Geology of the Paria Northwest quadrangle Kane County, Utah

The Paria Northwest Quadrangle, referred to as the Paria area, is located in semiarid to arid plateau and canyon country at the southwest corner of the Kaiparowits region in Kane County, Utah. The historic towns of Paria and Adairville are located on the north and south edges of the area respectively.

G EOLOGY O F THE PARIA NORTHWEST NORTlftlEST QUADRANGLE QUADRANGLE GEOLOGY OF KA NE COUN TY', UTAH UTAH KANE COUNTY, by by R o n a l d Clyde C l y d e Blakey Blakey Ronald A thesis A t h e s i s subm s u b mitted i t t e d to t o th t h ee faculty f a c u l t y of of the t h e University University of of Utah U t a h in i n partial p a r t i a l fulfillment f u l f i l l m e n t of of the t h e requirements requirements f o r tthe h e degree d e g r e e of of for Mas M a ster t e r of of Science Science ~ Depar D e p a r tment t m e n t of of Geolog'J Geology University U n i v e r s i t y of of Utah Utah August A u g u s t 1970 19?0 This Thesis for the }�ster of Science Degree by Ronald C. Blakey has been approved June 1970 �d� Chairman, Reader, Supervisory Corr�ittee Supervisory Committee , Reader, Supervisory Committee l:!e.�.. -.� , ajor Department � " .. . ,:. UNivt..RSUY Ut U i An Ub'WitS ACKNOHLEDGMENTS ACKNOWLEDGMENTS Thanks T h a n k s aare r e due d u e tto o tthose h o s e who helped h e l p e d in i n any way with w i t h the the p r e p a r a t i o n of of this t h i s report. report. preparation Dr. Wm. Lee Stokes D r . Wm. S t o k e s served s e r v e d as a s chairman c h a i r m a n for f o r my supervisory supervisory committee c o m m i t t e e and and gave g a v e much advice a d v i c e and and many hours h o u r s of of consultation. consultation. Drs. D r s . R. A. Robison R o b i s o n and H. D. Goode served s e r v e d as a s readers r e a d e r s on the the committee c o m m i t t e e and and also a l s o provided p r o v i d e d numerous n u m e r o u s suggestions. suggestions. Dr. D r . Stokes S t o k e s and Mr. A. E. Thompson Thompson provided p r o v i d e d access a c c e s s to t o notes, notes, m a n u s c r i p t , sections, s e c t i o n s , and photographs p h o t o g r a p h s of of material m a t e r i a l not n o t yet y e t published published a manuscript, h e San R a f a e l Group. Group. on tthe Rafael t a h State S t a t e Geological G e o l o g i c a l and Mineralogical M i n e r a l o g i c a l Survey Survey The U Utah furnished f u r n i s h e d a well w e l l llog e g and loaned l o a n e d drafting d r a f t i n g equipment. equipment. Special S p e c i a l tthanks h a n k s are a r e expressed e x p r e s s e d tto o my wife w i f e Dee who aaccompanied c c o m p a n i e d me each e a c h day d a y in i n the t h e field f i e l d and typed t y p e d the t h e manuscript. manuscript. iii iii CONTENTS CONTENTS PPage age ACKJ.1'OhTLEDGMENTS ACKNOWLEDGMENTS iii iii T.LT-,U STRA.T IONS ILLUSTRATIONS vii vii ABSTRACT INTRODUCTION INTRODUCTION ix ix I . of work work PPurpose u r p o s e of methods FField ield m ethods work PPrevious revious w ork I1 I1 . . . . . 1* 3 GEOGRAPHY 3 Location L ocation . . . . . . . . . History and nnomenclature H i s t o r y and omenclature Climate, and w water C l i m a t e , vvegetation, e g e t a t i o n , and a t e r supply supply . . . . . . . . Flora F l o r a and and fauna fauna Ro ads * • « . . . . . . . « » . > . . . . . . . . . . Roads ECO[lU[ftY Scenery iicunouiy , . . . « » • . . . • > . . . . . . . . . . • Movie S c e n e r yHaking Movie Making STR..4.TIGRAPHY STRATIGRAPHY . . . . Sub S u bssurface u r f a c e stratigraphy stratigraphy Rocks exposed R o c k s e x p o s e d at a t the t h e surface surface Permian System Permian . . . . . Ka:Lbnb K a i b a b Formation Formation • Perm.ian P e r m i a n Triassic T r i a s s i c boundary boundary Trias T r i a s s ic i c System , M oenkopi Forma Moenkopi F o r m ation t i o n •. LOhH': Lowerr Red Hemhcr Member Virg V i r g in i n Limt!stolLC Limestone 3 6 ( . . . . . . . . . . . . 13 . . . . . . . . 13 20 20 ^0 20 24 ^4 1 3 1 3 J . . . . . . . . . . . . •. . . . . 25 . . . . . . . . . . . . Ncm ber Member . . . . . . . . r.liddle d Hember. M i d d l e B.e Red Member. Shnabka.i.b S h n a b k a i b Nel!lber Member Upper Upper Red Feed He:nber Member Dep D e posit.ional o s i t i o n a l environments environments . . . . . . . . Sub·-Chinle S u b - C h i n l e uunconfo n c o n f ormity r m i t y ,. . . . . . . . . . . Chinle Formation • C h i nSh i e inarump F o r m a t i Member on , . . „ , . . . „ Shinarurap . . . . . . . or- ButMember te Mejnber Hon:lt M o nr iified t o r B uForest t t e Member , Pet Member P e t r Rock i f i e d Membe F o r er. s t Member . . . 0\·11 Owl Rock Member. . . . . . . . Depositional environments DepositIonal environments iv iv 3 3 6 77 8' 99 10 11 -0 , . . » » . . . . . . . . . . . . . . . . . . . . . . . 25 ^5 27 ^7 29 29 31 *32^ 35 -* 36^ 37 ^7 38 QO 3 3 3 3 39 41^ 44' 3 l rl 47 ^4 t.8 4 7 ^ PPage age STRATIGfu\PHY--Continued STRATIGRAPHY—Continued Glen Canyon Group Group • • • • G l e n Canyon 51 • • 51 W i n g a t e SSandstone andstone . . • . • . • 52 Hingate • • • • Hoenave FFormation Moenave ormation . . . • • • • 54 Dinosaur Canyon Member • • D i n o s a u r Canyon Member . . . . • . 55 Hember • • • • SSpringdale p r i n g d a l e SSandstone a n d s t o n e Member • 57 Depositional D e p o s i t i o n a l eenviror~ents nvironments 59 • • • 59 Kayenta K a y e n t a FFormation ormation • • • • • 60 Triassic and JJurassic Systems . . . . . . 64 T r i a s s i c and urassic S y s t e m s .• Navajo N a v a j o SSandstone andstone • • • • 64 • 64 System .• .• . • . •. • • • • • • • • • • • • • • 70 JJurassic u r a s s i c System Tongues Navajo and C Carmel T o n g u e s of tthe he N a v a j o and a r m e l • • · . . . . 70 Ho11o~,," Tongue .• .• . • . • . • . . JJudd udd H o l l o w Tongue · . . . • 71 Thousand Pockets Tongue T housand P o c k e t s Tongue • .• . . . 73 Depositional D e p o s i t i o n a l eenvironments nvironments . • • • 73 San R Rafael Group • • • • • San a f a e l Group • • 74 Cannel FFormation Carmel o r m a t i o n ,• • • • • • • • • • • • • • • 75 Paria River Member .• .• . . . . . . . . . . .77 P aria R i v e r Member 77 white W h i t e sandstone s a n d s t o n e ffacies acies • • 79 • 79 'V-linsor Hember Wins o r Member 81 • 81 Depositional D e p o s i t i o n a l environments environments . . . . • . • . • . •. • 85 Entrari8. • • • • • . . . . . . . . . • 87 E n t r a d a Sandstone Sandstone 87 G u n s i g h t.. Dutle B u t t e Member Gunsigiti l'fetI11j~l" • • • • • • •• 88 C a n n o n v i l l e Member Cannonville Hember • • • • • . • . •. .• . • 8899 Escalante E s c a l a n t e Hember Member • • • , •. .' 90 D e p o s i t i o n a l enviroll.lnents environments . 95 Depositional • • •• Sub-Cretaceous unconformities • • • • • 96 Sub-Cretaceous unconformities . . . Creataceous • • • • • • 98 C r e a t a c e o u s System System Dakota. Formation Formation • • • • " • • , 9988 Dakota T r o p i c Shale Shale , • • • • • • 105 Tropic • • • • • • • 105 S t r a i g h t Cliffs C l i f f s FOlTilation Formation 108 Straight • • • • • • • ,108 T i b b e t Canyon Hemb(~r Member • • 109 Tlbbet • • .109 H o l l o w Member . . .• .• . • . • . • . • . •. • ,109 .109 Smoky HolJow John • • • • • .110 J o h n Henry Hember Member 110 Drip .112 D r i p Tank Member • • • • • 112 Depositional D e p o s i t i o n a l environments environments . . . • • • • • .113 113 Tertia~y .114 T e r t i a r y anJ and Quatenary Q u a t e n a r y deposits deposits . . . . . . . . ,114 Tertiary-Quaternary T e r t i a r y - Q u a t e r n a r y COJ.l:slotiwrate-Conglomerate— Parum!eaf) P a r u n w e a p (?) ( ? ) Forrnati:.m Formation , 115 • • .US Terrace T e r r a c e and. and pediTaent p e d i m e n t rlepo3:i.ts deposits 116 ·116 L a n d s l i d e Dud and talus t a l u s depos:i.ts d e p o s i t s and and !"BndsJ.:i.cie Toreva-blocLs Toreva-blocks . , .us - -118 A l l u v i a l fan f a n deposits deposits . ·119 .119 Alluvial • • • • • Fluvial F l u v i a l deposits d e p o s i t s •. .• .• . • . • . • • • • • • .119 • .119 wied •• • • • • • _ • • -120 Wind deposits deposits »120 or STRUCTURE •• .... 121 • • • • • ·121 Folding Folding .121 • • • • .121 vv PPage age STRUCTURE--Continued STRUCTURE—Continued East Kaibab um.,arp E ast K a i b a b unwarp East Kaibab monocline E ast K aibab m onocline Basin PParia a r i a PPlatform-Kaiparowits latform-Kaiparowits B asin FFaulting aulting Valley FFivemile ivemile V a l l e y ffault a u l t zzone one Cockscomb ffault Cockscomb a u l t ssystem ystem . . . . . . . Road C Creek Road r e e k ffaults aults JJoints oints Slumping Slumping Periods of ddeformation P e r i o d s of eformation Pre-Dakota P r e - D a k o t a ddeformation eformation Post-Dakota P o s t - D a k o t a ddeformation eformation . Causes of ddeformation C a u s e s of eformation GEOMORPHOLOGY GE0M0RPH0L0GY 121 121 122 122 124 124 125 125 126 129 130 131 131 132 132 133 137 . . . . 139 139 . . . . . Physiographic P h y s i o g r a p h i c features features . . . . . 139 144 Geomorphic history Geomorphic h i s t o r y 144 HINERAL RESOURCES 146 MINERAL RESOURCES 146 Gold Gold Mercury Manganese M ercury Copper M anganese Uranium Copper Coal U ranium Building materials Coal Building materials STI~\TIGRAPRIC 145 1l~6 . . . . . . . . . . . . . . SECTIONS SIRATIGRAPRIC SECTIONS REFERE~CE S , 146 146 145 , . . . . . . . CITED 146 147 147 148 148 149 149 150 150 152 152 166 REFERENCES CITED 166 VITA 172 VITA 172 vi vi ILLUSTRATIONS Page Page F igures Figures 55 1. 1. Index I n d e x map of of Paria Paria ••••••• 2. 2. Photograph P h o t o g r a p h of of Road Creek C r e e k Badlands Badlands . . . . . . . . 12 12 3. 3. Photograph P h o t o g r a p h of of San Rafael R a f a e l Group in i n West Cove. Cove . . . 12 12 4. 4. Chart C h a r t of of previous p r e v i o u s and ppresent r e s e n t correlation correlation . . . . 15 1^ 5. 5. Columnar Columnar section s e c t i o n of of subsurface s u b s u r f a c e rocks rocks 16 16 6. 6. Photographs P h o t o g r a p h s of of Kaibab K a i b a b Formation F o r m a t i o n in i n Sand Sand Gulch G u l c h .••. 12 7. 7. P h o t o g r a p h of of Lower Lower Red and Virgin V i r g i n Members of Photograph Members of Moenkopi Formation •••• Moenkopi F o r m a t i o n • 12 ..... 12 34 34 34 34 3lf 34 42 2 34 34 8. 8. Photograph of Cockscomb near Paria 9. Photograph of channel in Shinarump 10. Photograph of Gingham Skirt Butte II. Sketch shmving "double Shinarump" 12. 12. Photosraph of Cockscomb looking north 13. 13. Photograph of Navajo Sandstone in Catstairs P h o t o gCanyon r a p h of• N • a •v a j•o • S •a n •d s t•o n e i n C a t s t a i r s • • • 67 14. 14. Canyon , . 6 7 P h o t o g r a p h of of Canuel-Navajo C a r m e l - N a v a j o Tongues T o n g u e s in in Photograph Catstairs • • • . . . . . . • . •. • 67 C a t s t a i r s Canyon Canyon 9. 10. 11. P h o t o g r a p h of Cockscomb n e a r P a r i a P h o t o g r a p h of c h a n n e l i n S h i n a r u m p P h o t o g r a p h of Gingham S k i r t B u t t e . . . . . . . ..... . . . . . . . S k e t c h showing " d o u b l e S h i n a r u m p " 4 . P h o t o g r a p h of Cockscomb l o o k i n g n o r t h . . . . . . 15. 15. Phot P h o t oograph g r a p h of of Paria P a r i a River R i v e r Member of of Cantlel Camel Formation F o r m a t i o n in i n Hest West Cove •. .• .• .• . • . • . • . • . •. .. • 67 16. 16. S e c t i o n Sllo'\'ling s h o w i n g "nnoorth-south r t h - s o u t h relationsi1ips relationships Seetioll 17. of San Rafael Group • • • • • of San R a f a e l Group . . . . . . . . . . . . • • 82 82 Photograph of Carmel and Entrada in West Cove •• 67 17. P h o t o g r a p h of C a r m e l and E n t r a d a i n West Cove . . 67 18. 18. Section shovling east-,vest relationships S e c t i oSan n showing e a s t - w e s t r e l a t i o• n •s h •i p •s • • • • • 90 Rafael Group 19. San R a of f a e lEntrada Group Sandstone . . . . . • . • 92 90 Photograph in l-Jest Cove 120. 9. P h o t o g r a p h of of E n t r a d a Sandstone S a n d s t o n e in i n West Cove . • 92 Photograph Entrada Cottom'lOod 20. Creek • • ... •• .. • • • • • • • .. .. • 92 P h o t o g r a p h of E n t r a d a Scradstone i n C o t t o n w o o d vii Creek . . . . . . . . . . . . . . . . . . . 92 vii Illustrations—Continued Illustrations--Continued Page Page F igures Figures 221. 1. Sketch S k e t c h sshowing h o w i n g Sub-Dakota S u b - D a k o t a uunconformities nconformities 222. 2. Photograph P h o t o g r a p h of of Cretaceous C r e t a c e o u s strata s t r a t a in i n Cottonwood Cottonwood Canyon Canyon. • • • • • • • • • 223. 3. ' 99 . . . 92 Section S e c t i o n of of Dakota D a k o t a Formation F o r m a t i o n showing s h o w i n g cyclic cyclic sedimentation 103 sedimentation 2/.. 24. 2S. 25. 103 Photograph of southern end of Brigham Plains P h o t o g r a p h of s o u t h e r n end of B r i g h a m P l a i n s . 92 92 Diagram shmving migration of environments D i a g r aacross m s h o wParia i n g m i area g r a t i o n• of • • e •n v•i r o• n m • e•n t s across Paria area . . . . . . 134 134 1. 1. L a t e Permian P e r m i a n tthrough hrough M iocene S t r u c t u r a l Events Events Late Miocene Structural 135 135 1. 1. G e o l o g i c map of P a r i a NH NW Quadrangle Quadrangle Geologic of Paria 22.. Structural S t r u c t u r a l sections sections • 3. 3. Structural Paria ~M S t r u c t u r a l map of of P aria N W Quadrangle Quadrangle • 4. 4. Physiographic of P Paria P h y s i o g r a p h i c ffeatures e a t u r e s of a r i a area area Table Table Plates Plates viii viii IIn n pocket pocket pocket . ·. IInn pocket pocket . · IInn pocket . . . . . pocket · IInn pocket ABSTRACT The P Paria a r i a Northwest N o r t h w e s t Quadrangle, Q u a d r a n g l e , referred r e f e r r e d to t o as a s tthe h e Paria Paria a r e a , is i s located l o c a t e d in i n semiarid s e m i a r i d to t o arid a r i d plateau p l a t e a u and canyon c a n y o n ccountry o u n t r y aatt the the area, southwest County, Utah. s o u t h w e s t corner c o r n e r of of the t h e Kaiparowits K a i p a r o w i t s rregion e g i o n in i n Kane C ounty, U tah. The h i s t o r i c towns t o w n s of of Paria P a r i a and Adairville A d a i r v i l l e are a r e located l o c a t e d on h e nnorth o r t h and historic on tthe s o u t h edges e d g e s of of the t h e area a r e a respectively. respectively. south I n f o r m a t i o n on subsurface s u b s u r f a c e sedimentary s e d i m e n t a r y rrocks o c k s rranging a n g i n g iin n age age Information from Precambrian P r e c a m b r i a n to t o Permian P e r m i a n was obtained o b t a i n e d chiefly c h i e f l y from from aan n electric electric from l o g of of the t h e Kaibab K a i b a b Gulch G u l c h #1 # 1 well w e l l located l o c a t e d jjust u s t off o f f tthe h e southwest s o u t h w e s t corner corner log of the t h e map. map. of of these t h e s e rrocks o c k s correlate c o r r e l a t e readily readily w i t h tthe h e Grand Most of with Canyon exposures. exposures. Canyon Rocks exposed Middle e x p o s e d in i n the t h e area a r e a rrange a n g e in i n age a g e from from M i d d l e Pel~ian Permian t o Late L a t e C:Lt::taceous C r e t a c e o u s and repl-eSeL1~ r e p r e s e n t a w-id8 w i d e v&ric~y v a r i e t y of of ccontir:.er.tal o n t i n e n t a l ane and to marine m a r i n e environments; e n v i r o n m e n t s ; their t h e i r total t o t a l aggregate a g g r e g a t e tthickness h i c k n e s s iis s aabout b o u t 6400 C400 feet. feet. a i b a b Formation F o r m a t i o n of of Permian P e r m i a n age a g e \-JaS was deposited d e p o s i t e d iin n a shallow shallow The K Kaibab s e a that t h a t transgressed t r a n s g r e s s e d into i n t o the t h e area a r e a from from the t h e southeast. southeast. sea The PermianPermian- T r i a s s i c unconformity u n c o n f o r m i t y hhas a s very v e r y little l i t t l e relief; r e l i e f ; it i t is is m a r k e d by thin Triassic marked by a thin yellow m u d s t o n e of of uuncertain n c e r t a i n affinities. affinities. yellmif mudstone Moenkopi F o r m a t i o n of of The l1oenkopi Formation E a r l y Triassic T r i a s s i c age a g e consists c o n s i s t s of of five f i v e members deposited d e p o s i t e d iin n a vvariety a r i e t y of of Early c o n t i n e n t a l and marine m a r i n e envii-orunents. environments. continental F o r m a t i o n is i s entirely e n t i r e l y continental. continental. Formation L a t e Triassic T r i a s s i c Chinle Chinle The Late R e l i e f of of up to t o 80 e e t iis s seen seen Relief 30 ffeet bbetween e t w e e n the t h e Moenkopi and Chinle C h i n l e Formatiolls F o r m a t i o n s where w h e r e the. t h e fluvial f l u v i a l Shinarump Shinarump Member of of tthe he C h i n l e is i s ppresent. resent. l1ember Chinle t h r e e uupper p p e r members the The three melllbers of of the C h i n l e form form colorful c o l o r f u l badlands b a d l a n d s and steep s t e e p slopes s l o p e s at a t tthe h e foot f o o t of the Chirile of the Cockscomb. Cockst2ornb. t h i n (60 feet f e e t or o r less) l e s s ) edge e d g e of of the t h e Wingate W l n g a t e Sandstone, Sandstone, A thin DC ggenerally e n e r a l l y aabsent b s e n t iin n ssouthwestern outhwestern U t a h , eextends x t e n d s aas s ffar ar w e s t aas s tthe h e Paria Paria Utah, west area. area. The ffluvial Moenave and and K Kayenta form much much of of the The l u v i a l Moenave a y e n t a FFormations o r m a t i o n s form the massive of tthe were by westward m a s s i v e ccliff l i f f of h e Cockscomb; bboth oth w e r e ddeposited e p o s i t e d by westward had ssources and east. fflowing l o w i n g rrivers i v e r s tthat h a t had o u r c e s iin n hhighlands i g h l a n d s tto o tthe h e ssouth o u t h and east. massive Navajo Sandstone The uusually sually m a s s i v e ccliff-forming liff-forming N avajo S a n d s t o n e of of Triassic and JJurassic and jjointed T r i a s s i c ((?) ? ) and u r a s s i c aage g e iis s hhighly i g h l y faulted f a u l t e d and o i n t e d iin n the the Paria P a r i a area. area. The tthickness of tthe The h i c k n e s s of h e uunit n i t iis s nnot o t determinable d e t e r m i n a b l e hhere e r e but but iis s estimated e s t i m a t e d tto o be 1800 ffeet. eet. be 1800 E x t e n s i v e tonguing t o n g u i n g bbetvJeen e t w e e n tthe h e Navajo Navajo Extensive and Carmel Formations Carmel F o r m a t i o n s iis s eexposed x p o s e d along a l o n g tthe h e bback a c k of of tthe h e Cockscomb. The JJudd Hollow Tongue of of tthe \,'est and the udd H o l l o w Tongue h e Carmel C a r m e l originates o r i g i n a t e s from from tthe he w e s t and the Thousand Tongue of Navajo from tthe Thousand Pockets P o c k e t s Tongue of the the N a v a j o originates o r i g i n a t e s from h e eeast. ast. a r e probably p r o b a b l y shallOlv shallow m a r i n e and beach-tidal b e a c h - t i d a l flat f l a t deposits. deposits. are marine Bo B o'tth h The Carmel and E n t r a d a Formations F o r m a t i o n s are a r e eeach a c h divided d i v i d e d iiuto n t o tthree h r e e members. members. Carmel Entrada Both were Both w e r e deposited d e p o s i t e d in i n complex complex environments e n v i r o n m e n t s th t h a tt ,,,ere w e r e dominantly dominantly marine m a r i n e or o r aqueous a q u e o u s to t o the t h e nnorth o r t h and contin c o n t i n en e n tal t a l tto o the t h e ssouth o u t h and complexly c o m p l e x l y interfingered i n t e r f i n g e r e d in i n tthe h e Paria P a r i a area. area. m a j o r unconfoIT.lity u n c o n f o r m i t y representing r e p r e s e n t i n g much of of the t h e Late L a t e Jur;;lssic Jurassic A major separates s e p a r a t e s the t h e Entrada E n t r a d a and the t h e Dakota D a k o t a Formations. Formations. Major Major uplifts uplifts took west t o o k place p l a c e to t o the the w e s t and most m o s t of of the t h e Cr C r eta e t a cceous e o u s clastics e l a s t i c s came from from t h a t di d i r~ec e c ttlon. ion. that C r etaceous e t a c e o u s Dakota D a k o t a Format F o r m a t i oon n is i s continental c o n t i n e n t a l at at The Cr the t h e b::lse b a s e an andd marine m a r i n e at a t the t h e top; t o p ; se'leral s e v e r a l coal c o a l depa d e p os:tts s i t s are a r e located l o c a t e d in in it. it. T r o p i c Shale S h a l e 'vas was deposi d e p o s i tte e dd in i n s hallo", h a l l o w seas s e a s that t h a t transgressed transgressed The Tropic t h e east. east. from the S t r a i g h t Cliffs C l i f f s contains c o n t a i n s considerable c o n s i d e r a b l e coal c o a l several several The Straight miles m i l e s east e a s t of the t h e area. area. U n c o n s o l i d a t e d fluvial, f l u v i a l , alluvial, a l l u v i a l , and arid eolian e o l i a n deposits d e p o s i t s are are Unconsolidated widespread. widespread. These T h e s e deposits d e p o s i t s are a r e plL)cenc, p l i o c e n e , Pleis P l e i s ttocene, o c e n e , and Recent R e c e n t in I n age. age, x The sedimentary s e d i m e n t a r y rocks r o c k s of of the t h e P;:n:ia P a r i a area a r e a hhave a v e been b e e n displaced displaced by t h e East E a s t Kaibab K a i b a b monocline m o n o c l i n e and the t h e regional r e g i o n a l tilting t i l t i n g and uplift uplift by the of the t h e Colorado C o l o r a d o Plateau. Plateau. of S t r u c t u r a l relief r e l i e f is i s over o v e r 7000 feet f e e t and and Structural s e v e r a l faults f a u l t s have h a v e displacements d i s p l a c e m e n t s of of 1000 or o r more feet. feet. several major The major f o l d i n g took t o o k place p l a c e at a t tthe h e close c l o s e of of the t h e Cretaceous C r e t a c e o u s bbut u t some of of the the folding f a u l t i n g may bbe e Miocene. Miocene. faulting The Faria P a r i a area a r e a has h a s undergone u n d e r g o n e a long l o n g complex complex history h i s t o r y of of g e o m o r p h i c development. development. geomorphic t h e four f o u r streams s t r e a m s that t h a t cross c r o s s the t h e East East Of the K a i b a b Uplift U p l i f t in i n its i t s 200 mile m i l e length, l e n g t h , two cross c r o s s the t h e Paria P a r i a area; area; Kaibab b o t h have h a v e apparently a p p a r e n t l y bbeen e e n superimposed s u p e r i m p o s e d from from the t h e Pliocene-Pleistocene Pliocene-Pleistocene both s t r e a m levels l e v e l s as a s shown by b y the t h e gravels g r a v e l s and alluvial a l l u v i a l fans. fans. stream l1uch Much prospecting p r o s p e c t i n g has h a s taken t a k e n place p l a c e in i n the t h e Paria P a r i a area. area. mercury, m e r c u r y , and uuranium r a n i u m hhave a v e bbeen e e n sought s o u g h t without x ^ i t h o u t success. success. Gold, Gold, A small small aoandoned a b a n d o n e d copper c o p p e r mine m i n e is i s locateu l o c a t e d in i n the t h e Navaj N a v a j o0 Sar,dstoH2. Sandstone. The m a i n economic e c o n o m i c aspect a s p e c t of of the t h e Paria P a r i a area a r e a in i n the t h e future f u t u r e will w i l l probably probably main be scenery s c e n e r y and tourism. tourism. xi INTRODUCTION P u r p o s e ·of of ~lork work Purpose The ppurpose u r p o s e of of tthis h i s work work is i s to t o describe d e s c r i b e a measured m e a s u r e d section section and pprovide r o v i d e a map of of an a n aggregation a g g r e g a t i o n of of Pennian P e r m i a n and and Hesozoic Mesozoic continental marine c o n t i n e n t a l and m a r i n e sedimentary s e d i m e n t a r y rocks r o c k s exposed e x p o s e d along a l o n g tthe h e flank f l a n k of of the t h e East E a s t Kaibab K a i b a b monocline m o n o c l i n e in i n southern s o u t h e r n Utah. Utah. Incidental I n c i d e n t a l to t o this t h i s the the g e c m o r p h o l o g y and structure s t r u c t u r e were w e r e also a l s o studied. studied. geomorphology F i e l d methods methods Field Host Most of of the t h e field f i e l d work work was done d o n e during d u r i n g the t h e summer of of 1969. 1969. Stratigraphic S t r a t i g r a p h i c sections s e c t i o n s were w e r e measured m e a s u r e d with w i t h tap t a p e ,, Brunton B r u n t o n compass, c o m p a s s , and and hand level. hand level. Contacts were Contacts w e r e plotted p l o t t e d in i n the t h e field f i e l d on aerial a e r i a l photographs photographs and ttransferred r a n s f e r r e d tto o the t h e base b a s e map by careful c a r e f u l inspection i n s p e c t i o n of of key k e y reference referenc ppoints. oints. f o r m a t i o n s were w e r e s a~lpled m p l e d and described d e s c r i b e d in i n the t h e field f i e l d and and The formations s e l e c t e d s aamples m p l e s were w e r e later l a t e r examined e x a m i n e d with w i t h a binocular b i n o c u l a r microscope. microscope. selected P r e v i o u s ~vork work Previous The earliest e a r l i e s t geologic g e o l o g i c \vork work done d o n e in i n the t h e area a r e a ~lCls was by the t h e Powell, Powell D u t t o n , and Wheeler W h e e l e r surveys s u r v e y s .. Dutton, I n 1871 1 8 7 1 Powell, P o w e l l , during d u r i n g his h i s second s e c o n d trip trip In tthrough h r o u g h the t h e Colorado C o l o r a d o canyons, c a n y o n s , l ee fft t the t h e Colorado C o l o r a d o near n e a r Crossing C r o s s i n g of of the the F a t h e r s and made a ttraverse r a v e r s e through t h r o u g h the t h e Paria P a r i a area. area. Fathers I n 1872 L. H. H, In M arshall r s h a l l of of tthe he W h e e l e r survey s u r v e y made a topog t o p o g raphic r a p h i c ttraverse r a v e r s e from from Ma Wheeler J o h n s o n Creek C r e e k to t o Paria P a r i a and then t h e n on Johnson t o Gl G l een n Canyon. Canyon. to I n 1872-73 1872-73 In A, H. Thompson of the t h e Powell P o w e l l survey s u r v e y locat l o c a t eed d tthe h e Utah-Arizona U t a h - A r i z o n a boundary boundary A. Thomp son of and b a s e line l i n e survey s u r v e y for f o r topographic t o p o g r a p h i c maps publi p u b l i sshhe e dd by the and made a base by the S, Geological G e o l o g i c a l Survey. Survey. U. S. I n 1875 E. E. E* Howell H o w e l l ppublished u b l i s h e d a report report In 2 d e a l i n g partly p a r t l y with w i t h the the V e r m i l i o n Cliffs. Cliffs. de.aling Vermilion was the t h e first f i r s t \vorker worker He Has t o establish e s t a b l i s h a stratigraphic s t r a t i g r a p h i c sequence s e q u e n c e for f o r the t h e Paria P a r i a area a r e a and to to to d e s c r i b e the t h e structure. structure. describe A d d i t i o n a l works w o r k s by o w e l l and Thompson Thompson on on the t h e East E a s t Kaibab Kaibab Additional by H Howell M o n o c l i n e are a r e incorporated i n c o r p o r a t e d in I n Dutton D u t t o n (1880). (1880). Monocline 1.Ja1cott W a l c o t t (1890), ( 1 8 9 0 ) , Lawson Lawson (1913), ( 1 9 1 3 ) , and Noble N o b l e (1927) ( 1 9 2 7 ) have h a v e \vritten written with ppapers a p e r s dealing dealing w i t h the t h e Paria P a r i a area a r e a and iimmediate m m e d i a t e surrounding s u r r o u n d i n g areas areas b u t the t h e first f i r s t modern m o d e r n investigation i n v e s t i g a t i o n was by by H. E. Gregory. Gregory. but first The first c o m p l e t e geologic g e o l o g i c map of of tthe h e Paria P a r i a area a r e a (1:250,000) ( 1 : 2 5 0 , 0 0 0 ) is i s included i n c l u d e d in in complete tthe h e map of of the t h e Kaiparo K a i p a r o ..wlits i t s rregion e g i o n (Gregory ( G r e g o r y and and Moore, M o o r e , 1931). 1931). U n f o r t u n a t e l y the t h e papers p a p e r s by Gregory G r e g o r y (1948, ( 1 9 4 8 , 1950) 1950) and and Baker, B a k e r , Dane, Dane, Unfortunately R e e s i d e (1947) are a r e marred m a r r e d by b y miscorrelations m i s c o r r e l a t i o n s chiefly c h i e f l y involving involving and Reeside tthe h e relation r e l a t i o n of of the t h e San Rafael R a f a e l Group of of south,(Testern s o u t h w e s t e r n Utah U t a h with with c o r r e s p o n d i n g rocks r o c k s of of the t h e Escalante E s c a l a n t e area. area. corresponding T h e s e miscorrelations miscorrelations These a r e currently c u r r e n t l y being b e i n g corrected c o r r e c t e d (Stokes ( S t o k e s and Thompson, 1969; 1 9 6 9 ; Thompson Thompson are S t o k e s , in i n press). press). and Stokes, Seve S e v eral r a l recent r e c e n t stratigraphic s t r a t i g r a p h i c ppapers a p e r s refer r e f e r tto o tthe h e Paria Paria s e c t i o n and and establish e s t a b l i s h a correlation c o r r e l a t i o n system; s y s t e m ; Babenroth B a b e n r o t h and Strahler Strahier section ( 1 9 4 5 ) discuss d i s c u s s tthe h e geomorphology g e o m o r p h o l o g y and and structure s t r u c t u r e of of the t h e East E a s t Kaibab Kaibab (1945) m onocline. mono.-:line. A l t h o u g h nonE n o n e of of hhis i s pa p a pers p e r s deals d e a l s so s o lely l e l y with w i t h the t h e Paria Paria Although a r e a , McKee h a s done d o n e much significant s i g n i f i c a n t ',",ork work in i n nnorthern o r t h e r n Arizona A r i z o n a and and m:ea, HcKee has a d j a c e n t Utah. Utah. .::djacent GEOGRAPHY Location Location The pParia Northwest aria N o r t h w e s t quadrangle, q u a d r a n g l e , rreferred e f e r r e d to t o hereafter h e r e a f t e r as as the t h e Paria P a r i a area, a r e a , is i s located l o c a t e d in i n central c e n t r a l Kane County, C o u n t y , south-central south-central Utah, U t a h , near n e a r the t h e \oJ·estern w e s t e r n edge e d g e of of the t h e Colorado C o l o r a d o Plateau. Plateau. The area a r e a lies lies at a t the t h e southern s o u t h e r n foot f o o t of of tthe h e High High Plateaus, P l a t e a u s , tthe h e eastern e a s t e r n edge e d g e of of the the Kaiparowits K a i p a r o w i t s region, r e g i o n , and and tthe h e northern n o r t h e r n edge e d g e of of the t h e Grand Grand CanyonCanyonKaibab K a i b a b Upwarp region. region. The area a r e a is i s uninhabited--Kanab u n i n h a b i t e d — K a n a b is i s 40 miles miles to t o the t h e west, w e s t , Cannonville, C a n n o n v i l l e , Henrieville, H e n r i e v i l l e , and and Tropic T r o p i c are a r e about a b o u t 35 35 miles miles to Marina Page t o the t h e north, n o r t h , and liJahweap Wahweap M a r i n a and P a g e are a r e about a b o u t 35 miles m i l e s to to the t h e southeast s o u t h e a s t in i n Arizona. Arizona. Two abandoned a b a n d o n e d settlements, s e t t l e m e n t s , Paria P a r i a (or (or Pahreah--pah, P a h r e a h — p a h , water; w a t e r ; rreah, e a h , deer) d e e r ) and Adairville A d a i r v i l l e are a r e on the the northern-most n o r t h e r n - m o s t and southern-most s o u t h e r n - m o s t extremities e x t r e m i t i e s of of tthe h e quadrangle quadrangle respectively r e s p e c t i v e l y (fig. ( f i g . 1). 1). H i s t o r y and Ncimenc1atlire Nomenclature Hisf.oE.L f o l l o w i n g account a c c o u n t is is m a i n l y after a f t e r Gregory G r e g o r y and Moore Moore The following mainly ( 1 9 3 1 , p. p . 30). 30). (1931, Paria, P a r i a , the t h e oldest o l d e s t settlement s e t t l e m e n t in i n south-cen s o u t h - c e n t ral r a l Utah, U t a h , has h a s aa llong o n g and and colorful c o l o r f u l history. history. Es must E s calante c a l a n t e in i n 1777 m u s t havE: h a v e crossed c r o s s e d the the Faria P a r i a River R i v e r nnear e a r hhere e r e because b e c a u s e to t o tthe h e north n o r t h and south s o u t h it i t :1.s i s entrenched entrenched i n deep, d e e p , nerrO"l n a r r o w canyons. canyons. in pass p a s s through t h r o u g h tthe h e area a r e a .. He was He~vas u n d o u b t a b l y the t h e first f i r s t Caucasian C a u c a s i a n to to undoubtably Navajos Nomadic N a v a j o s and a n d Piutes P i u t e s and possibly p o s s i b l y the the a n c i e n t "cliff " c l i f f dwellers d w e l l e r s "ll favored f a v o r e d tthe h e area a r e a as a s a temporary temporary more ancient stopover. stopover. f i r s t explore e x p l o r e r ss of of southern s o u t h e r n Utah U t a h including i n c l u d i n g Hamblin, Hamblin, The first 44 P o w e l l , Marshall, M a r s h a l l , and A. H. Thompson Thompson camped camped here. here. powell, The first f i r s t settlement s e t t l e m e n t was made by Peter P e t e r Shurtz S h u r t z in i n 1865 at a t Rock Rock House, H o u s e , 2 miles m i l e s below b e l o w the t h e Cockscomb (fig. ( f i g . 1) on the t h e Paria P a r i a River. River. d r i v e n away bby y Navajos N a v a j o s the t h e following f o l l o w i n g year, y e a r , but b u t returned r e t u r n e d with with He was driven f a m i l i e s in i n 1871; 1 8 7 1 ; in i n 1873 Adairville A d a i r v i l l e was loca l o c a tted e d further f u r t h e r down down 6 families stream. stream. I r r i g a t i o n ditches d i t c h e s were w e r e dug and several s e v e r a l years years w i t h good good Irrigation with c r o p s followed; f o l l o w e d ; bbut u t by by 1878 irrigation i r r i g a t i o n problems p r o b l e m s had h a d forced f o r c e d all a l l the the crops f a m i l i e s of of bboth o t h settlements s e t t l e m e n t s to t o relocate r e l o c a t e at a t the t h e present p r e s e n t site s i t e of of families P a r i a , above a b o v e the t h e Cockscomb, w h i c h was first f i r s t settled s e t t l e d in i n 1874. 1874. Paria, which By 1884 the members of t h e ppopulation o p u l a t i o n included i n c l u d e d 107 resident r e s i d e n t members of the t h e Mormon church c h u r c h plus p l u s transient t r a n s i e n t cattlemen c a t t l e m e n and Piutes. Piutes. The prosperity p r o s p e r i t y of of Paria P a r i a came to t o a sudden s u d d e n end. end. In I n 1884 and and 1885 severe mose s e v e r e winter w i n t e r storms s t o r m s and summer floods f l o o d s \>'ashed w a s h e d away m o s t or of ehe che arable a r a b l e lands l a n d s cconverting o n v e r t i n g the t h e narrow n a r r o w stream s t r e a m channel c h a n n e l into i n t o a broad b r o a d wa~h wash that t h a t often o f t e n extended e x t e n d e d from from wall w a l l to t o wall w a l l in i n the t h e canyon. canyon. As recent r e c e n t as a s the t h e late l a t e 1920's 1 9 2 0 * s a few families f a m i l i e s rreturned e t u r n e d during during the nm., the t h e growing g r o w i n g season s e a s o n to t o harvest h a r v e s t meager m e a g e r lands, l a n d s , but b u t now t h e townsite townsite i s uuninhabited--disturbed n i n h a b i t e d — d i s t u r b e d only o n l y by the t h e tourist, t o u r i s t , an a n occasional o c c a s i o n a l rancher, rancher, is o r perhaps p e r h a p s a movie m o v i e crew. crew. or A few acres a c r e s of of private p r i v a t e land l a n d nnear e a r Adairville Adairville a r e irrigated i r r i g a t e d and support s u p p o r t a small s m a l l he h e rrd d of of cattle. cattle. are Geographic G e o g r a p h i c names are a r e linportant i m p o r t a n t in i n an a n area a r e a and save s a v e words words \when ..hen describing d e s c r i b i n g locations l o c a t i o n s .. The Paria North<;.;rest Paria N o r t h w e s t quadrangel q u a d r a n g e l base b a s e map contains c o n t a i n s some of of the t h e important i m p o r t a n t place p l a c e llames names but b u t many landmarks l a n d m a r k s are are nnot o t labeled. labeled. The f011m.,ing f o l l o w i n g names are a r e added a d d e d in i n this t h i s report r e p o r t and their their sou:rces, s o u r c e s , where w h e r e known, aare r e given. given. Road Creek, C r e e k , Shurtz S h u r t z Gorge, G o r g e , and and Robinson R o b i n s o n Creek C r e e k appear a p p e a r on Gregory's G r e g o r y * s map ((1948). 1948). Par. P a r ii aa and Cottom-lOad Cottonwood F i g u r e 1.--Index 1 . - - I n d e x map of h e Paria P a r i a area. area. P h o t o g r a p h is i s of of a rrelief e l i e f model model Figure of tthe Photograph Visi National Recreation iin n the the V i s i t oor r Center C e n t e r of of Glen G l e n Canyon Canyon N ational R e c r e a t i o n Area. Area. 1) Calico Paria River, C a l i c o But B u t te, t e , 2) Hackberry H a c k b e r r y Canyon, 3) P aria R i v e r , 4) 4 ) Road Creek, Creek, 5) Gingham Gingham Skirt Gorge, S k i r t Butte, B u t t e , 6) Cottonwood C o t t o n w o o d Creek, C r e e k , 7), 7 ) , Shurtz Shurtz G o r g e , 8) Rush Beds, Creek, Rockhouse Valley, B e d s , 9) Cockscomb, 10) Robinson Robinson C r e e k , 11) Rockhouse V a l l e y , 12) RockRockMesa , 13) Brigham Brigham Plains, Fivemile hhouse o u s e Mesa, P l a i n s , 14) Sand Sand Gulch, G u l c h , 15) F i v e m i l e Mountain, Mountain, 16) FFivem i v e mii 1e l e Vaalley, l l e y , 17) Notch Notch Canyon, 18) The Slot, S l o t , 19) Catstairs Catstairs Canyon, 20) West Cove, 21) East Adairville 23) West E a s t Cove, 22) A d a i r v i l l e Canyon, 23) Clark nch, 24) U. S. Highway C l a r k Be Bench, Highway 89. 89. ,6 Canyon were xv ere left l e f t off o f f the t h e original o r i g i n a l U. S. S, Geological G e o l o g i c a l Survey S u r v e y base base Canyon T map. Host Most of of tthe h e roads r o a d s are a r e ne~v new and hhave a v e been b e e n located l o c a t e d approximately approximately and labeled me; l a b e l e d by m e ; this t h i s applies a p p l i e s also a l s o to t o the t h e movie m o v i e set s e t situated s i t u a t e d near near the t h e mouth m o u t h of of Road Creek. Creek. Gingham Skirt S k i r t Butte B u t t e is i s apparently a p p a r e n t l y aa l o c a l tern. term. local The ffollmving o l l o w i n g key key landforms l a n d f o r m s have h a v e been b e e n given g i v e n original o r i g i n a l names names in i n this t h i s rreport; e p o r t ; Rockhouse R o c k h o u s e Mesa, M e s a , Rockhouse R o c k h o u s e Canyon, C a n y o n , Adairv~lle A d a i r v i l l e Canyon, Canyon Notch N o t c h Canyon, C a n y o n , and The Slot. Slot. C l i m a t e , V e g e t a t i o n , and W a t e r Supply Supply Climate,Vegetatiort,artdWater From the t h e sparse s p a r s e amount amount of of climatic c l i m a t i c data d a t a available, a v a i l a b l e , it i t is is apparent a p p a r e n t that t h a t the t h e Paria P a r i a area a r e a lies l i e s in i n the t h e transition t r a n s i t i o n zone z o n e between between arid a r i d and and semi-arid s e m i - a r i d climate c l i m a t e (approximately ( a p p r o x i m a t e l y 9 inche i n c h e s of of rainfall r a i n f a l l per per yyear) e a r ) and also a l s o bbetween e t w e e n the t h e sub-tropical s u b - t r o p i c a l and and temperate t e m p e r a t e zones z o n e s (8 or or more months m o n t h s above a b o v e 50 degrees d e g r e e s Farenheit). Farenheit). Paria's P a r i a ' s annual a n n u a l rainfall rainfall o v e r five f i v e yyears e a r s (1895-1899) ( 1 8 9 5 - 1 8 9 9 ) averaged a v e r a g e d 8.45 8 , 4 5 inches i n c h e s with w i t h a maximum over max:L-rrum of 1 4 . 0 9 inches i n c h e s and and a minimum of 4.85 4 , 8 5 inches i n c h e s (Gregory ( G r e g o r y and Moore, M o o r e , 1931, 1931, 14.09 minimum of p , 16). 16). p. No data d a t a are a r e available a v a i l a b l e for f o r t eempe m p eraturz r a t u r e but b u t extr e x t r apolating apolating from nearby n e a r b y ttowns o w n s and correcting c o r r e c t i n g for f o r elevation e l e v a t i o n the t h e avera.ge a v e r a g e annual annual from ttemperature e m p e r a t u r e is i s pr p r oobably b a b l y be b e tt\>Jeen w e e n 52 aud and 56 degrees. degrees. a r e hot-hot Summers are g e n e r a l l y 10 tto o 20 days d a y s exce e x c e eed d 100 degre d e g r e e ss each e a c h ye y e aar r (Gregory ( G r e g o r y and and generally M o o r e , 1931? 1931> p. p . 22). 22). Hoore, W i n t ers e r s may be b e mild m i l d one o n e yyear e a r and severe severe Ttlint tthe h e nnext e x t but b u t snow seldom s e l d o m r eemains m a i n s on the t h e ground g r o u n d more m o r e than t h a n a day d a y or or two after a f t e r a storm. storm. Sunshine S u n s h i n e is i s tthe h e one dependable d e p e n d a b l e element e l e m e n t of of the t h e climate. climate. The a r e a rec.eiv r e c e i v ees s approxima a p p r o x i m ately t e l y 80 to t o 90 percent p e r c e n t of of possible p o s s i b l e sunshine sunshine area 7 annually. annually. On tthe h e contrary c o n t r a r y rainfall r a i n f a l l is i s sporadic. s p o r a d i c . One thirty-minute thirty-minute downpour an eentire downpour may give g i v e tthe h e area a r e a its i t s entire e n t i r e r a infall i n f a l l for f o r an n t i r e month month o r even e v e n a season. season. or L o n g , steady s t e a d y rrains a i n s are a r e rare r a r e and and even e v e n iin n winter winter Long, pprecipitation r e c i p i t a t i o n lasting l a s t i n g more m o r e than t h a n 24 hours h o u r s is i s uncommon. O f t e n in in Often s p r i n g , summer, and autumn autumn rain r a i n can c a n be b e seen s e e n falling f a l l i n g from clouds spring, from clouds o n l y to t o evaporate e v a p o r a t e before b e f o r e rreaching e a c h i n g tthe h e ground. ground. only Surface S u r f a c e water w a t e r is i s meag m e a ger. er. The Paria River Paria R i v e r flows f l o w s yyear e a r round, round, tthough h o u g h short s h o r t sections s e c t i o n s may be b e dry d r y at a t the t h e surface s u r f a c e much of h e yyear e a r due due of tthe to removed for t o water w a t e r removed f o r irrigation i r r i g a t i o n and underg u n d e r g rround o u n d flowage f l o w a g e iin n tthe h e river river bbed. ed. S e v e r a l springs s p r i n g s are a r e located l o c a t e d a short s h o r t distance d i s t a n c e uupstream p s t r e a m from from Several tthe h e mouth mouth of of Cottonwood Cottonwood Canyon Canyon but b u t during d u r i n g tthe h e summer summer m o n t h s , this this months, w a t e r seeps s e e p s underground u n d e r g r o u n d b eeff oore r e rreaching e a c h i n g the t h e Paria Paria R i v e r .. water River Several Several s e e p s occur o c c u r in i n the t h e Hoenkopi Moenkopi Formation F o r m a t i o n in i n the t h e slot-like s l o t - l i k e tribut:aries tributaries seeps n o r t h of of Road Creek C r e e k but b u t the t h e quantity q u a n t i t y of of w a t e r involved i n v o l v e d is is north water insignificant. insignificant. Because and much of of the B e c a u s e tthe h e area area, is i s extremely e x t r e m e l y ~.,e w ell l l drained d r a i n e d and the s u r f a c e is i s bedrock, b e d r o c k , water w a t e r runs r u n s off off and does d o e s not n o t soak s o a k iin n oor r pond surface e v e n during d u r i n g heavy h e a v y rain. rain. even Flora. F l o r a artd and ·FaUIl§!. Fauna The vegetation Paria of tthe v e g e t a t i o n of of tthe he P a r i a area a r e a is i s typical t y p i c a l of h e Upper Sonoran S o n o r a n and Transition T r a n s i t i o n Zones. Zones. the t h e so-called s o - c a l l e d pygmy forest. forest. The cornman and pinyon-common trees t r e e s aare r e jjuniper u n i p e r and pinyonOther O t h e r corr~on common pplants l a n t s aare r e tthe h e cliffrose, cliffrose, gray Brigham g r a y sage, s a g e , r aa bbbit b i t bbrush, r u s h , black b l a c k brush, brush, B r i g h a m tea, t e a , and and numerous numerous annuals a n n u a l s (Gregory, ( G r e g o r y , 19l1.8~ 1 9 4 8 , pp.. 217). 217). A fe,., few cottom-lOads c o t t o n w o o d s aand n d willows willows (planted Paria River ( p l a n t e d by the t h e Normon Mormon pioneers,!) p i o n e e r s ? ) grow grox^ along a l o n g the the P aria R i v e r and 8 Cottonwood Canyon; C a n y o n ; tamarack t a m a r a c k or o r salt s a l t cedar c e d a r grows g r o w s in i n profusion p r o f u s i o n along along cottonwood p a r t s of of the t h e Paria Paria R i v e r flood f l o o d pplain. lain. parts River v a r i o u s photographs photographs The various p r e s e n t a good good picture p i c t u r e of of the t h e flora. flora. present f a u n a of of tthe h e Paria P a r i a area a r e a is i s rrepresentative e p r e s e n t a t i v e of of the t h e high high The fauna desert. desert. S p a r s e vvegetation e g e t a t i o n ,, little l i t t l e water, w a t e r , and harsh h a r s h cl~~ate c l i m a t e account account Sparse ffor o r many species s p e c i e s bbut u t few individuals. individuals. include a Common mammals include w i d e varie v a r i e tty y of of m i c e , rats, r a t s , and other o t h e r small s m a l l rodents, r o d e n t s , rabbits, r a b b i t s , deer, deer, wide mice, c o y o t e s , and and bbats. ats. coyotes, tthrough h r o u g h tthe h e area. area. B i r d s are a r e not n o t abundant a b u n d a n t but b u t many species s p e c i e s pass pass Birds o t i c e a b l e ones o n e s include i n c l u d e hawks, h a w k s , vultures, vultures, More nnoticeable m a g p i e s , rravens, a v e n s , sHallows, s w a l l o w s , and an occasional o c c a s i o n a l roadrunner. roadrunner. magpies, Reptiles R e p t i l e s include i n c l u d e nume n u m erous r o u s lizards l i z a r d s but b u t contrary c o n t r a r y tto o public public opinion t T..JO were o p i n i o n rattlesnakes r a t t l e s n a k e s are a r e rare--only r a r e — o n l y two w e r e seen s e e n during d u r i n g a summer season, s e a s o n , bbut: u t cdution c a u t i o n is i s still s t i l l nnecessary e c e s s a r y .. Three T h r e e unpleasC'.nt unpleasant a r t h r o p o d s — b l a c k widow spiders, s p i d e r s , scorpions s c o r p i o n s ,, and wasps w a s p s constitute c o n s t i t u t e aa arthropods--black d e f i n i t e threat t h r e a t to t o man and are a r e espe e s p e ci c i a lly l l y abundant a b u n d a n t nnear e a r ttrash r a s h barrels barrel definite and "rater. water. Roads Although A l t h o u g h the t h e Paria P a r i a area a r e a is i s generally g e n e r a l l y uninhab u n i n h a b it i t eed d Hilderness w i l d e r n e s s, tthe h e area a r e a is is w e l l served s e r v e d by roads. \vell by roads. S, 89 loops l o o p s thro!.lgh t h r o u g h the the U. S. s o u t h w e s t e r n quarte q u a r t e rr of of the t h e map area a r e a and then t h e n parallels p a r a l l e l s the t h e southern southern southwestern boundary. boundary. The Paria P a r i a Road, R o a d , a good good dirt d i r t road r o a d ,, leaves l e a v e s High\vay Highway 89 at at tthe h e ",estern w e s t e r n edge e d g e of of the t h e map and provides p r o v i d e s access a c c e s s to t o the t h e 'vest-central west-central part p a r t of of tthe h e area. area. A n o t h e r good good dirt d i r t road, r o a d , the t h e COttOIlVlOOd C o t t o n w o o d Canyon Canyon Another Road, leaves l e a v e s U. U, S. S, 89 a few few miles m i l e s east e a s t of of the t h e Paria Paria R i v e r but b u t enters enters River the t h e map ar.ea a r e a south s o u t h of of Brigham Brigham Plains P l a i n s and then t h e n follmvs f o l l o w s the t h e Paria Paria 9 R i v e r and Cottonwood C o t t o n w o o d Creek C r e e k nnorthward. orthward. River Old Paria Paria R o a d , now The Old Road, j e e p trail, t r a i l , parallels p a r a l l e l s Road Creek C r e e k and provides p r o v i d e s access a c c e s s to t o the the a jeep n o r t h w e s t part p a r t of of the t h e map area. area. northwest 4 - w h e e l - d r i v e vvehicle e h i c l e ccan a n easily easily A 4-wheel-drive n e g o t i a t e tthe h e Paria P a r i a River R i v e r bed bed and provide p r o v i d e access a c c e s s tto o tthe h e nnorth o r t h and and negotiate c e n t r a l sections s e c t i o n s of of the t h e area. area. central r i g h a m Plains P l a i n s jjeep e e p ttrail r a i l climbs climbs The B Brigham tthe h e KaiparoHits K a i p a r o w i t s Plateau P l a t e a u opposite o p p o s i t e Hackberry H a c k b e r r y Creek C r e e k and r o v i d e s an an and pprovides a v e n u e to t o the t h e Brigham Brigham Plains. Plains. avenue S e v e r a l parts p a r t s of of tthe h e oold l d Kanab-Glen Kanab-Glen Several Canyon High\vay Highway are a r e still s t i l l usable u s a b l e and are a r e useful u s e f u l in i n West Canyon West Cove and F i v e m i l e Valley. Valley. Fivemile S e v e r a l other o t h e r jjeep e e p ttrails r a i l s lead l e a d iinto n t o tthe h e short short Several c a n y o n s on tthe h e west w e s t side s i d e of of the t h e Cockscomb and aabandoned b a n d o n e d ppaths a t h s used used canyons i n construction c o n s t r u c t i o n of of pmver power lines l i n e s are a r e convenient c o n v e n i e n t hhiking i k i n g trails. trails. in Economy The economy Utah economy of of central c e n t r a l Kane County, County, U t a h iis s at a t present present completely c o m p l e t e l y unsupported u n s u p p o r t e d by pennanent p e r m a n e n t industry i n d u s t r y and and is i s totally totally d e p e n d e n t on natural n a t u r a l resources. resources. dependent M i n i n g hhas a s been b e e n ffairly a i r l y active, active, Mining though t h o u g h sporadic s p o r a d i c since s i n c e pioneer p i o n e e r days. days. Prospects P r o s p e c t s ,, cclaL~s, l a i m s , and d e s e r t e d mines m i n e s dot d o t the t h e area; a r e a ; deposits d e p o s i t s of of gold, g o l d , mercury) m e r c u r y , manganese, manganese, deserted c o p p e r , uranium, u r a n i u m , vanadium, v a n a d i u m , coal, c o a l , and bbuilding u i l d i n g materials materials w e r e the the copper, ~lere g o a l s of of these t h e s e ventures. ventures. goals At present p r e s e n t none n o n e of of the t h e aabove b o v e are are e c o n o m i c a l l y feasible f e a s i b l e to t o mine m i n e (with ( w i t h the t h e possible p o s s i b l e exception e x c e p t i o n of economically of some r o a d bbuilding uilding m a t e r i a l s ) although a l t h o u g h tthe h e new Kaiparowits Kaiporowits C o a l Project Project road materials) Coal c u r r e n t l y unde:nvay u n d e r w a y ,viII w i l l uundoubtedly n d o u b t e d l y provide p r o v i d e a great g r e a t economic e c o n o m i c boost boost currently t o the t h e eastern e a s t e r n part p a r t of of Kane County C o u n t y in i n tthe h e near n e a r future. future. to p r e s e n t economy economy of of the t h e area a r e a consists c o n s i s t s of t o c k raising raising, The present of sstock tourism, t o u r i s m , and and u\ovie m o v i e making, making. Host of the Most of of the t h e area a r e a at a t tthe h e ffoot o o t of the 10 10 V e r m i l i o n Cliffs C l i f f s is i s Bureau B u r e a u of of Land Management-controlled M a n a g e m e n t - c o n t r o l l e d grazing grazing Vermilion land of the l a n d ~.,here w h e r e nnumerous u m e r o u s sheep s h e e p and cattle c a t t l e graze g r a z e throughout t h r o u g h o u t much of the yyear. ear. S°iLnerjL The scenery mainstay s c e n e r y of of southern s o u t h e r n Utah U t a h is i s indirectly indirectly a m a i n s t a y of of the t h e economy. Kane County by three C o u n t y is i s surrounded s u r r o u n d e d on four f o u r sides s i d e s by three National Area N a t i o n a l Parks P a r k s and a National N a t i o n a l Recreation Recreation A r e a and and tthe h e ttowns o w n s of of Kanab and Ht. on tourist Mt. Carmel C a r m e l Junction J u n c t i o n are a r e highly h i g h l y dependent d e p e n d e n t on tourist trade. trade. The Paria P a r i a area a r e a contains c o n t a i n s scenery s c e n e r y that t h a t is i s representative r e p r e s e n t a t i v e of of the ~.,ho1e. t h e pplateau l a t e a u country c o u n t r y as as a w hole. Because B e c a u s e 14 fonnations f o r m a t i o n s aare r e exposed exposed across and no a c r o s s a strip s t r i p 7 miles m i l e s wide, w i d e , the t h e llandforms a n d f o r m s change c h a n g e rrapidly a p i d l y and single, s i n g l e , spectacular s p e c t a c u l a r type t y p e of of landform l a n d f o r m dominates d o m i n a t e s the t h e aarea; r e a ; tthe h e scenery scenery depends and tthe d e p e n d s on the t h e geologic g e o l o g i c fonnations, f o r m a t i o n s , the t h e structure, s t r u c t u r e , and h e rrate a t e of of erosion. erosion. Thus in where i n the t h e north~.,est n o r t h w e s t corner c o r n e r of of the t h e map area area w h e r e the the rocks Ilioenkopi and r o c k s are a r e nearly n e a r l y horizontal h o r i z o n t a l and erosion e r o s i o n is i s rapid, r a p i d , tthe h e Moenkopi C h i n l e Formations F o r m a t i o n s h aave v e been b e e n deeply d e e p l y dissected d i s s e c t e d into i n t o nnarrow a r r o w sslot l o t canyons canyons Chinle r o l l i n g interfluves. interfluves. and rolling movie The walls w a l l s surrounding s u r r o u n d i n g Paria P a r i a and and all an abandoned abandoned m o v i e set s e t at at the t h e foot f o o t of of Gingham Gingham Skirt S k i r t Butte B u t t e are a r e eroded e r o d e d into i n t o spectacularly spectacularly c o l o r e d cliffs; c l i f f s ; brick-red b r i c k - r e d siltstones s i l t s t o n e s of Moenkopi aare r e ooverlain v e r l a i n by colored of Moenkopi y e l l o w Shinarump, S h i n a r u m p , the t h e multi-colored m u l t i - c o l o r e d and banded b a n d e d Chinle, C h i n l e , and h e deep deep yellow and tthe v e r m i l i o n - c o l o r e d Glen G l e n Canyon Group ( fig f i g ,. 2). 2). venil:l1ion-c:010red The Cockscomb is i s created c r e a t e d from from dipping d i p p i n g strata s t r a t a of of tthe h e East East Kaibab K a i b a b monocline. monocline. The deep Glen d e e p ve v e rJ.:::ailion m i l i o n rocks r o c k s of of tthe he G l e n Canyon Canyon Group hhave a v e been b e e n eroded e r o d e d into i n t o a rr'.gged r a g g e d ,, rrooster o o s t e r comb-like c o m b - l i k e rridge i d g e cut cut il by numerous n u m e r o u s box canyons c a n y o n s with w i t h abundant a b u n d a n t pinyon p i n y o n and jjuniper u n i p e r trees. trees. The Paria P a r i a River R i v e r cuts c u t s through t h r o u g h this t h i s structure s t r u c t u r e exposing e x p o s i n g the t h e steeply steeply d i p p i n g , multi-colored m u l t i - c o l o r e d sandstones s a n d s t o n e s and siltstones. siltstones. dipping, Cottonwood C o t t o n w o o d Canyon Canyon is i s a colorful c o l o r f u l strike s t r i k e valley v a l l e y Hhere where s t e e p l y dipping d i p p i n g Entrada E n t r a d a Sandstone S a n d s t o n e has h a s been b e e n fashioned f a s h i o n e d into I n t o castles castles steeply inarets. and m minarets. A few few m i l e s north n o r t h of of the t h e Paria P a r i a area a r e a contrasting c o n t r a s t i n g red red miles h i t e beds b e d s of of tthe h e Carmel C a r m e l and cream cream bbeds e d s of of the t h e Entrada E n t r a d a have have and w white b e e n tilted t i l t e d on end and and llocally o c a l l y overturned o v e r t u r n e d to t o form form a uniquely uniquely been t w i s t e d hogback. hogback. twisted U n f o r t u n a t e l y much of of the t h e scenery s c e n e r y in i n Cottonwood Cottonwood Unfortunately Canyon is i s spoiled s p o i l e d by t h e careless c a r e l e s s pplacement l a c e m e n t of of two sets s e t s of of highhighCanyon by the v o l t a g e po",er power lines. lines. voltage West Cove dominates of the d o m i n a t e s the t h e scenery s c e n e r y of t h e southern s o u t h e r n part p a r t of the t h e map area. area. The colorful c o l o r f u l red, r e d , white, w h i t e , and and brmm brown Carmel C a r m e l is i s capped capped bby y the t h e massive m a s s i v e white w h i t e cliffs c l i f f s of of the t h e Entrada. Entrada. The vvalley a l l e y is i s wide w i d e to to t h e south s o u t h where w h e r e the t h e Entrada E n t r a d a dips d i p s gently, g e n t l y , but b u t narrows n a r r o w s quickly q u i c k l y to to the t h e north n o r t h where w h e r e bboth o t h formations f o r m a t i o n s dip d i p steeply s t e e p l y tto o the t h e east e a s t (fig. ( f i g . 3). 3). the Movie Haking Making The scenery s c e n e r y of of the t h e Paria P a r i a ar a r eeaa hhas a s bbeen e e n used u s e d as a s a background background in i n many movies. movies. The varied v a r i e d llandforms a n d f o r m s plus p l u s the t h e rapid r a p i d change c h a n g e in in scenery widely s c e n e r y easily e a s i l y afford a f f o r d the t h e illusion i l l u s i o n of of w i d e l y separated s e p a r a t e d areas. areas. Several S e v e r a l feature f e a t u r e movies m o v i e s as a s ",ell w e l l as a s numerous n u m e r o u s television t e l e v i s i o n shows have have bbeen e e n filmed f i l m e d in i n this t h i s area. area. The economy economy of of Kanab has h a s received r e c e i v e d aa major m a j o r bboost o o s t from from the t h e movie m o v i e industry. industry. -Figure F i g u r e 2. 2 . ---Road - R o a d Creek C r e e k Badlands B a d l a n d s with w i t h Calico C a l i c o Butte Butte in Figure i n middle m i d d l e distance. distance. F i g u r e shows entire entire Triassic T r i a s s i c section s e c t i o n and a n d East E a s t Road Creek C r e e k fault. fault. See pplate 1 for explanation of symbols. late f o r e x p l a n a t i o n of s y m b o l s . F i g u r e 3. 3.— S a n Rafael R a f a e l Group in i n West Cove looking looking Figure --San north Kaibab n o r t h along a l o n g East East K a i b a b monocline. monocline. Figure 6( - -Kalbab Forn~tion (Beta Member) in Sand Gulch. Figure 7. --Lower Red and Virgin Members of Moenkopi Formation south of Road Creek. STRATIGRAPHY The stratigraphy s t r a t i g r a p h y of of the t h e Paria P a r i a area a r e a may be b e considered c o n s i d e r e d under under e a d i n g s — r o c k s in i n the t h e subsurface s u b s u r f a c e and and rrocks o c k s exposed e x p o s e d at a t the the two hheadings--rocks surface. surface. I n f o r m a t i o n on the t h e subsurface s u b s u r f a c e formations f o r m a t i o n s came chiefly chiefly Information from an an electric e l e c t r i c log l o g of of the t h e Tidewater T i d e w a t e r Oil O i l Company Kaibab K a i b a b Gulch G u l c h #1 #1 from jjust u s t off o f f the t h e map area a r e a to t o the t h e south,v-est. southwest. of tthis h i s section s e c t i o n can can Most of r e a d i l y bbe e correlated c o r r e l a t e d '-lith w i t h the t h e Grand Grand Canyon Canyon exposures. exposures. readily The rocks were r o c k s seen s e e n at a t tthe h e surface surface w e r e measured m e a s u r e d where w h e r e exposures exposures and accessibility a c c e s s i b i l i t y were w e r e best. best. The formations f o r m a t i o n s were w e r e also a l s o studied s t u d i e d at at several s e v e r a l places p l a c e s along a l o n g strike s t r i k e to t o detect d e t e c t possible p o s s i b l e facies f a c i e s and and thickness thickness chang e s . changes. Figure F i g u r e 4 shows previous p r e v i o u s and and ppresent r e s e n t correlations c o r r e l a t i o n s for f o r the the Paria P a r i a area a r e a involving i n v o l v i n g rocks r o c k s exposed e x p o s e d at a t the t h e surface. surface. SUBSURFACE STRATIGRAPHY Rocks that t h a t underlie u n d e r l i e tthe h e Paria P a r i a area a r e a range r a n g e in i n age a g e from from Precambrian P r e c a m b r i a n to t o Permian P e r m i a n (fig. ( f i g . 5). 5). A well w e l l drilled d r i l l e d in i n section s e c t i o n 34, 34, T 42S., 4 2 S . , R 2W. 2W. has h a s penetrated p e n e t r a t e d the t h e upper u p p e r Precambrian P r e c a m b r i a n rocks, r o c k s , and most most of of the t h e subsurface s u b s u r f a c e stratigraphy s t r a t i g r a p h y discussed d i s c u s s e d in i n this t h i s ppaper a p e r is i s based b a s e d on on rrecords e c o r d s of of that t h a t vJell. well. Although A l t h o u g h much of of the t h e terminology t e r m i n o l o g y uused s e d here here is i s from from tthe h e Grand Grand Canyon, C a n y o n , several s e v e r a l formations f o r m a t i o n s are a r e present p r e s e n t here here tthat h a t are a r e not n o t present p r e s e n t there) t h e r e , and several s e v e r a l names are a r e brought b r o u g h t in i n from from the ~nd southeastern t h e eastern e a s t e r n Gre G r e at a t Basin, B a s i n , south,,,,estern s o u t h w e s t e r n Colorado C o l o r a d o and s o u t h e a s t e r n Utah. Utah In I n addition a d d i t i o n several s e v e r a l formations f o r m a t i o n s are a r e much thicker t h i c k e r in i n the t h e Paria P a r i a area area tthan h a n at a t their t h e i r type t y p e sections s e c t i o n s tn i n the t h e Grand Grand Canyon. Canyon. 13 14 14 The ooldest l d e s t rrocks o c k s ppenetrated e n e t r a t e d aare re w h i t e qquartzites u a r t z i t e s aassigned s s i g n e d to to white tthe h e Shinumo uartzite. Shinumo O Quartzite. T h e s e aare r e ooverlain v e r l a i n by e q u e n c e of varicolored These by a ssequence of varicolored ssoft o f t sstrata trata w i t h a few h i t e ssandstones a n d s t o n e s and i m y bbeds e d s aassigned s s i g n e d to to with few w ~"hite and llimy tthe h e Chuar h e Grand eries. Chuar Group Group of of tthe Grand Canyon Canyon SSeries. B o t h tthe h e Shinumo Both Shinumo and Chuar re L ate P r e c a m b r i a n and e r e deposited d e p o s i t e d iin n a north-south-trending north-south-trending Chuar aare Late Precambrian and w were geosyncline. geosyncline. Cambrian were ,,,ere C a m b r i a n strata strata w e r e deposited d e p o s i t e d in i n seas s e a s tthat hat w e r e time time ttransgressive r a n s g r e s s i v e sso o tthe h e deposits d e p o s i t s aare re E a r l y and and M i d d l e Cambrian C a m b r i a n in i n the the Early Middle Grand Canyon and M Middle and Late Cambrian Canyon rregion e g i o n and i d d l e and Late C a m b r i a n eastward. eastward. Cambrian The bbasal asal C a m b r i a n formation f o r m a t i o n iis s tthe h e Tapeats T a p e a t s Sandstone, S a n d s t o n e , aa q u a r t z i t i c sandstone s a n d s t o n e which w h i c h is i s locally l o c a l l y arkosic. arkosic. quartzitic common and conglomerates c o n g l o m e r a t e s occur o c c u r locally. locally. G l a u c o n i t e bbeds e d s are are Glauconite The Tepeats T a p e a t s grades g r a d e s into I n t o and and intertongues Angel i n t e r t o n g u e s with w i t h the t h e Bright Bright A n g e l Shale, S h a l e , a grayish-green g r a y i s h - g r e e n lii.i. m iC&CCCUS caceous shale s h a l e with w i t h intercalated i n t e r c a l a t e d sandstone s a n d s t o n e and limestone l i m e s t o n e units. units. As the the Cambrian seas s e a s transgressed t r a n s g r e s s e d eastward, e a s t w a r d , a thick t h i c k carbonate c a r b o n a t e deposit, d e p o s i t , the the Cambrian F o r m a t i o n s , was laid l a i d dO'Nn. down. Muav and Lynch Formations, D u r i n g the t h e interval i n t e r v a l of During t h e Ordovician, O r d o v i c i a n , Silurian, S i l u r i a n , and early e a r l y Devonian D e v o n i a n a period p e r i o d of of erosion e r o s i o n and and the n o n - d e p o s i t i o n took t o o k place. place. non-deposition O r d o v i c i a n or o r Silurian S i l u r i a n rocks r o c k s are are No Ordovician r e c o g n i z e d on the t h e Colorado C o l o r a d o Plateau. Plateau. recognized Several S e v e r a l hundr h u n d r eed d feet f e e t of of Upper Devonian D e v o n i a n rocks r o c k s T."ere w e r e deposited deposited in i n the t h e Paria P a r i a area. area. A basal b a s a l \-7hite w h i t e sandstone s a n d s t o n e and dolomite d o l o m i t e sequence, sequence, the t h e McCracken Fonnation F o r m a t i o n or o r Hember, Member, is i s overlain o v e r l a i n by a light-brovm light-brown dolomite, d o l o m i t e , the t h e Temple Butte B u t t e or o r Elbert E l b e r t Formation. Formation. Rocks equivale~t e q u i v a l e n t to to the t h e Ouray Limestone L i m e s t o n e thin t h i n across a c r o s s the t h e Kaibab K a i b a b Uplift U p l i f t and are a r e not n o t present present in i n the t h e Paria P a r i a area. area. (Lessentime, ( L e s s e n t i m e , 1969, 1 9 6 9 , p. p . 103). 103). Previous Workers I This Paper Drip Tonk M Straight Straight Cliffs Ciiffj John Henry M S5 Ss Smoky Hollow M JHbbet Canyon^ M Tropic Sh Tropic Sh Dakota F-i Etetlantt M. Cannonvilje M Gunsight Butte M Wi Fm Winsor AA ~ ~ E Curtis fm Entrada Ss Carmel Fm Navajo N ovajo Ss Ss whits ss f River M Pa. ..... <.J Thousand Pockets Ton Jydd Hollow Ton Navajo Navajo S5 Ss r---------- ~------- Tod i I to Fm Wingate Ss Upper S3S Petrified F o' est M Kay en to F| Springda'e Ss M Dinosaur Canyon M Owl Rock M Petrified Fores * M Shjna rvm p___ Co£Q Upper Red M_ Shnabkaib M Shnabkaib M Middle Red M Middle Red M lower Red M Virgin Is M Lower Red M I t kaibab Fni U . Kaibab ~_„—™ J .21 t_ . I F i g u r e J u - - D i a g rram a m s h o w i n g pprreevvi o u s a n d p r e s e n t l y p r o p o s e d c o r r e l a t i o n o f t h e P a r i a a r e a . Huiibers r e f e r t o p a g e s i n t e x t w h e r e o l d c o r r e l a t i o n s a r e d i s c u s s e d ,. i1); p . .10?.? 2) p . S l j 3 ) . 8 l | 10 p . 8 7 ; SO p . ? 6 | 6 ) p . 6 0 j 7) p . 5 7 j 8) p .•Sli: ^ l i s 9$J n . 2 t i . t p 1 I n d i v i d e d (1140* )* Muav-Lynch uundivided (1140'); 1 Kuav-Lynch T-—r I J Ezra J llieht-tan i g h t - t a n tto o brown brown llimestone i m e s t o n e aand n d ddolomite olomite w ith m i n o r ssaridstone a n d s t o n e and and with minor ssllty i l t y shales. shales. j T.—T i, i . ~J J j L 7 zZ 1I I I I tT T J 1 <<! ffi I 1 CD ~ < ~ O I l -1- - -I- 1—r I I 1-"15 . -L-,'" r_i"T.rxE Bri Ang She B r i gght ht A n ge l S h . ((330'); 330*)j g r:l.'e e eenish'~gray n i s h - g r a y ssi i Iltstone t s lone aand n d ssha h a lly y sandstone sandstone w i t h ssubordlnate u b o r d i n a t e sandstone sandstone with aand n d limestone. limestone. white own \~ ...... ' ' ~:., / '- Tapeats T a p e a t s Ss. S s . ((280); 280)* w h i t e tto o ppale-red a l e - r e d t oo br brown ——rrr'q uuartzitic a r t z i t i c s a n ddss tt oonne e w i t h a few s h a l y silt s i l t *.. with fel,' shaly . .. .. .. ..~ : ~. stone s t o n e beds. beds. t~~ ---- r----- - ---------------------- -------------------------------------.Z -=--=-:-::: Z - - - -.:?:' <! ~~-::~-= < . - - - -_7" 0:: ::-: ~ :~~ Chuar C h u a r Group (l120'); (1120')| vvaa ricolored r i c o l o r e d siltstone s i l t s t o n e with with int contains i n t eerbedded r b e d d e d white w h i t e sandstone; sandstone• c o n t a i n s a few few limestone l i m e s t o n e beds. beds. [l) t::...- ----- I _ -'--,--.,:. ~ i-=-c.=: <! Ii~£rr­ U o r.-:- . _7.:= UJ Hi ~:---:-:-:_~~ 0:: --'-- ~[~~~ a.. -.-CL u.. ----- W UJ ..=--=-~ -_'-.-:-~":7 n. ~~-_- ~~:1 :J -.. .. -:-::. -:-: ------------'--------_. _-------------'.. ~. to ...... ' \. _::0::.' S h i .. : .. 1r);j nShinumo u m o QU-1rtzi Q u a r t z i te t e U00 (100**) w h ite t e quartz q u a r t z ii tte e <• wh! WWvVvvvVw - - - _._ ---_._ --------------------------------------------------Figure F i g u r e 55 ..... . — Cen€!r,dlz G e n e r a l i z ee dd (~olu:nn column, of of ss ub u bc·ur s u r fi.1Ce f a c e st s t ~r.atD. r a t a in i n the t h e Pa P arla r i a area. area. K a i b a b Fm, herty m a s s i v e yyellow e l l o w limestone limestone Kaibab Fm . (250'+) (250'+-);; ccherty ll'ilssive and ssandy and a n d y dolomite. dolomite. . ·~::i·, Toroweap Fm. Fro. ((480'); Toroweap 480'); llight-colored i g h t - c o l o r e d ssandy a n d y carbonate carbonate sequence with bedded gypsum, andyrite, chert, s e q u e n c e w i t h b e d d e d gypsum, a n d y r i t e , chert, wMmmtim aand n d rred e d beds b e d s .• .. .. isrr.nt : .... :,.;'.:. --_. - . - - - _. <> A ... ............. . ;. :". :" ": ; . : •• : 0. ~.~ Hermit F::n. ((740'); H e r m i t Fm. 740')? iinterbedded n t e r b e d d e d bbrick r i c k -..rred e d tto o orange orange ssandstone a n d s t o n e aand n d siltstone. siltstone. XL HI Q. Supai-Esplanade, Queantoweap-Cednr S upai-Esplanade, Q u e a n t o w e a p - C e d a r Mesa undivided undivided ((810'); 310*); iinterbedded n t e r b e d d e d ppale-orange a l e - o r a n g e sandstone sandstone aand n d rred e d ssilty i l t y shale. shale. SXZZ gg:t"een r e e n mudstone mudstone -~- ~:.. ,/./ ' ~" p a 1l eeeOr<lnge - o r a n g e sancistone sandstone .:---::::..::~:. ./ .</ w ~;hite-to pale-orange h i t e t o p a l e - o r a n g e cchert h e r t yy sandstone sandstone ", :-:::~: / / ::':: \:':-:}.:'/ // ~-'- ,~. y .' ':'.' -? ,.-----------P a k o o n (O:~ephant E l e p h a n t Canyon) Canyon) Fin. 0 * ); ); Pakoon Fm. ( 770' . :.' / ~~:.J;:::::: .. .... / t a n limestone limestone tan aand n d ppink i n k ,_<lndstone. sandstone. C a l l v i l l e (Hermosa ( H e n n o s a )) uith w i t h basal b a s a l " ~lo M o1a~-type" l a s - t y p o " (210'); (210*)j s a n d y cherty, c h e r t y , tan t a n limestone l i m e s t o n e with w i t h limes l i m e s ttone o n e breccia; breccia* sandy mUdstone whit rred ed m u d s t o n e and and w h i t ee sandstone s a n d s t o n e at a t the t h e base. base, \ Red\ola Ls. Redw a ll ll L s , (750'); (750')» nlnssive ttan an m a s s i v e llimesto i m e s t o nne e and and dolomite. dolomite. -~~L~ -- ---- ---- Temple Butte B u t t e ( :J.b6:':) E l b e r t ) ·.r w ith i t h bC) b a ~tl. s a l~_ NcCracke McCrackenn SS S s ,t (WO'); (ISO*) *. ~t::?~~: ::. 'fempl{~ t a n!~ dolomite d o l o m i t e wIth w i t h i nnterbe<:!ded t e r b e d d e d Hh:ite w h i t e ssaandstone n d s t o n e ..— Orf~~r,:,.': ta - e specially s p e c i a l l y n car e a r the t h e base b a s e •, _ - --- - - ---- - ---- . Figure g u r e 5.--Continued. 5. —Continued. 18 is M i s s i s s i p p i a n seas s e a s ccovered o v e r e d most m o s t of of tthe he C o l o r a d o Plateau P l a t e a u and and Nississippian Colorado d e p o s i t e d the t h e Redwall Redwall L imestone. deposited Linlestone. e d w a l l is i s a llight-tan i g h t - t a n and and The R Redwall g r a y linlestone l i m e s t o n e and dolomite; d o l o m i t e ; tthe h e name ii.s s dderived e r i v e d from h e red r e d stain stain gray from tthe that w a s h e s down from from overlying o v e r l y i n g rred e d bbeds e d s iin n tthe he G r a n d Canyon. Canyon. that washes Grand During D u r i n g tthe he P Pennsylvanian, e n n s y l v a n i a n , seas s e a s ttransgressed r a n s g r e s s e d from from the the washed down do,vn from from hhighlands nnorthwest o r t h w e s t and cclastic l a s t i c deposits d e p o s i t s \\rashed i g h l a n d s tto o the the east; e a s t ; tthe h e rresulting e s u l t i n g stratigraphy s t r a t i g r a p h y iis s characterized c h a r a c t e r i z e d bby y numerous n u m e r o u s lateral lateral changes. changes. The bbasal Pennsylvanian asal P e n n s y l v a n i a n ddeposit e p o s i t ooriginated r i g i n a t e d aas s a "terra " t e r r a -rossa" -rossa soil s o i l on Hississippian M i s s i s s i p p i a n carbonates; c a r b o n a t e s ; this t h i s unit u n i t may bbe e ccorrelative o r r e l a t i v e with with the Holas F FO:L'1llation Four Corners t h e Molas o r m a t i o n of of tthe he F our C o r n e r s region. region. This T h i s is i s overlain overlain by a sequence and llight s e q u e n c e of of cherty c h e r t y carbonate, c a r b o n a t e , rred e d shale, s h a l e , and i g h t sandstone sandstone t h a t is i s pprobably r o b a b l y correlative correlative w i t h the t h e Callville Callville F o r m a t i o n of western that with Formation of \.;restern Utah and the t h e Hermosa Hermosa Formation F o r m a t i o n of s o u t h e a s t e r n Utah. Utah. Utah of southeastern Permian most complex of of all The P e r m i a n is i s perhaps p e r h a p s tthe he m o s t complex a l l systems s y s t e m s in in t h e southern s o u t h e r n Colorado C o l o r a d o Plateau P l a t e a u region. region. the S h a l l o w seas s e a s ppersisted e r s i s t e d to to Shallow tthe h e north n o r t h and and west w e s t bbut u t a complex complex of of m i x e d and continental c o n t i n e n t a l envirorunent environment mixed p r e v a i l e d to t o tthe h e east e a s t and south. prevailed and south. C o n s e q u e n t l y a complex terminology Consequently complex terminology hhas a s bbeen e e n deveJ.oped, d e v e l o p e d , and g r e e m e n t on w h i c h , pparticularly a r t i c u l a r l y iin n transition transition and aagreement ,.,hich, a r e a s , iis s far f a r from from bbeing e i n g complete. complete. areas, B a s a l Permian P e r m i a n rocks r o c k s correlate correlate w i t h tthe he P akoon F o r m a t i o n of Basal Hith Pakoon Formation northwestern Arizona of the northwestern A r i z o n a and the t h e Elephant E l e p h a n t Canyon Canyon Formation F o r m a t i o n of the Canyonlands Utah. C a n y o n l a n d s area a r e a of of U tah. These T h e s e rocks r o c k s consist c o n s i s t of of light-brown light-brown limestone marine l i m e s t o n e and and pi p i nnk k s'_ s aun,dstone d s t o n e and and are are m a r i n e iin n origin. origin. This T h i s sequence sequence- by a ccomplex of redbeds iis s ovel~lain o v e r l a i n by o m p l e x clastic c l a s t i c iinterval n t e r v a l of r e d b e d s c.onsisting c o n s i s t i n g of of siltstone s i l t s t o n e and and san s a n dstone. dstone. In Grand Canyon I n tthe h e eastern e a s t e r n Grand Canyon aarea r e a equivalent equivalent 19 19 r o c k s bbelong e l o n g to t o the t h e Supai Supai F o r m a t i o n but b u t to t o tthe h e northwest n o r t h w e s t tthe h e Supai Supai rocks Formation i n t e r t o n g u e s with w i t h a more m o r e sandy s a n d y section, s e c t i o n , the t h e Esplanade E s p l a n a d e and Queantoweap intertongues and Queantoweap Formations, Hesa and Organ Rock Hembers F o r m a t i o n s , and to t o the t h e nnorth o r t h the t h e Cedar C e d a r Mesa O r g a n Rock Members of of the t h e Cutler C u t l e r Formation F o r m a t i o n are a r e recognized. recognized. The Paria m~ Paria N W quadrangle quadrangle is names can i s in i n this t h i s ttransition r a n s i t i o n area a r e a and so s o any or o r all a l l of of these t h e s e names can be applied more a p p l i e d until until m o r e detailed d e t a i l e d subsurface s u b s u r f a c e work is i s ddone. one. Bissell Bissell (1969) gives g i v e s a good good summary summary of of the t h e relations r e l a t i o n s of of tthe h e aabove b o v e formations. formations. The uppermost System ccan u p p e r m o s t three t h r e e formations f o r m a t i o n s of of the t h e Permian P e r m i a n System a n be be d i r e c t l y correlated c o r r e l a t e d with w i t h the t h e Grand Grand Canyon Canyon section. section. directly Hermit The Hermit F o r m a t i o n is i s a thick t h i c k sequence s e q u e n c e of of brick-red b r i c k - r e d sandstone, s a n d s t o n e , siltstone, siltstone, Formation s i l t y shale s h a l e that t h a t was most m o s t like l i k e lly y deposited d e p o s i t e d on on a ccoastal o a s t a l plain plain and silty ( B i s s e l l , 1969, 1 9 6 9 , pp.. 142-143). 142-143). (Bissell, I t is i s overlain o v e r l a i n by o m p l e x carbonate, carbonate, It by a ccomplex g y p s u m - a n h y d r i t e , chert, c h e r t , and and sandstone s a n d s t o n e sequence, s e q u e n c e , tthe h e Toroweap Toroweap gypsum-anhydrite, Formation. Formation. The Toroweap was deposited d e p o s i t e d in i n a fluctuating, f l u c t u a t i n g , restricted restricted sea. sea. The yyoungest o u n g e s t Permian P e r m i a n formation f o r m a t i o n and and oldest o l d e s t uunit n i t eexposed x p o s e d at at the t h e surface s u r f a c e in i n tthe h e Paria P a r i a area a r e a is i s tthe h e Kaibab K a i b a b Formation. Formation. Only the Only the upper and tthis u p p e r half h a l f of of the t h e Kaibab K a i b a b is i s exposed e x p o s e d at a t tthe h e surface s u r f a c e and h i s is is described d e s c r i b e d in i n detail d e t a i l in i n tthe h e next n e x t section. section. The lmver of the l o w e r ppart a r t of the Kaibub Formation Kaibab F o r m a t i o n Is i s sandy s a n d y dolomite d o l o m i t e and sandstone. sandstone. This T h i s sandstone sandstone is Hembers of i s pprobably r o b a b l y correlative c o r r e l a t i v e with w i t h the t h e DeChelly D e C h e l i y and \{]:lite W h i t e Rim Members of t h e Cutler C u t l e r Formation; F o r m a t i o n ; it i t is i s pprobably r o b a b l y a shallow s h a l l o w marine m a r i n e and and beach beach the deposit. deposit. 20 20 ROCKS EXPOSED AT THE SURFACE Pennian P e r m i a n System System The PPennian form one one of e r m i a n rrocks o c k s of of tthe h e Grand Grand Canyon Canyon rregion e g i o n form of the Lower and Middle Permian of tthe world t h e classical c l a s s i c a l Lower and M iddle P e r m i a n sections s e c t i o n s of he w o r l d both both from from tthe h e standpoint s t a n d p o i n t of of paleontology p a l e o n t o l o g y and eexcellent x c e l l e n t eexposures. xposures. A A thumb-shaped of Permian t h u m b - s h a p e d outcrop o u t c r o p pattern p a t t e r n of P e r m i a n rrocks o c k s eexposed x p o s e d iin n the t h e Kaibab Kaibab uplift and along East Kaibab monocline u p l i f t and a l o n g the the E ast K aibab m o n o c l i n e rreaches e a c h e s up into i n t o Utah Utah e x t e n d s as a s far f a r nnorth o r t h as a s the t h e Paria Paria N orthwest Q u a d r a n g l e where where and extends Northvlest Quadrangle t h e y form form most m o s t of of F ivemile M o u n t a i n (pl. ( p i . 1). 1). they Fivemile Mountain Only by McKee (1938, Only the t h e Kaibab K a i b a b Formation F o r m a t i o n as a s ddefined e f i n e d by ( 1 9 3 8 , pp.. 12) 12) i s exposed e x p o s e d iin n the t h e mapped area. is mapped area. Formations Form~tions entire K a i b a b and and Toroweap Toroweap The entire Kaibab and a r t of of tthe h e Rennit Hermit F o r m a t i o n are a r e ppresent r e s e n t at a t the the aDd ppart Formation surface 6 m i l e s tto o tthe h e ssouth o u t h iin n K a i b a b Gulch G u l c h (now B u c k s k i n Gulch Gulch surface miles Kaibab Buckskin most m aps). on most maps). I t should s h o u l d bbe e It n o t e d , however, h o w e v e r , tthat h a t bboth o t h the the noted, Photogeologic Northwest P h o t o g e o l o g i c Map of of tthe h e Paria Paria N o r t h w e s t Quadrangle, Q u a d r a n g l e , Kane County, County, Utah (Mcqueen (McQueen and a y , 1958), 1 9 5 8 ) , and and the t h e Geologic G e o l o g i c Map of of Southwestern Southwestern Utah and R Ray, Utah show the Toroweap FFonnation Gulch. Utah (Hintze, ( H i n t z e , 1963) 1963) show t h e Toroweap o r m a t i o n in i n Sand Sand G ulch, A A c l o s e comparison c o m p a r i s o n bbetween e t w e e n tthe he m e a s u r e d section s e c t i o n of of Sand Sand Gulch G u l c h (this (this close measured ppaper) a p e r ) with w i t h tthe h e type t y p e section section m e a s u r e d by Noble N o b l e ((1927) 1 9 2 7 ) shows that m.easured S110v7S that tthe h e bbasal a s a l 100 1.00 to t o 150 150 feet f e e t of of tthe h e Kaibab K a i b a b (as ( a s rredefined e d e f i n e d bby y HcKee) McKee) are are n o t exposed e x p o s e d in i n Sand Sand Gulch. Gulch, not K a i b a b Formation Formation Kaibab D a r t o n (1910) ( 1 9 1 0 ) named n a n e d the t h e Kaibab Kaibab L i m e s t o n e for f o r rrocks o c k s exposed exposed Darton Limestone t h e Kaibab K a i b a b Plateau P l a t e a u of of northern northern A r i z o n a , and and N o b l e (1927) ( 1 9 2 7 ) proposed proposed on the Arizona, Noble 21 21 m e a s u r e d a type t y p e section s e c t i o n iin n K aibab G ulch. and measured Kaibab Gulch. McKee (1938) ( 1 9 3 8 ) divided divided the K aibab L i m e s t o n e into i n t o the t h e Kaibab K a i b a b and and Toroweap Toroweap Formations. Formations. the Kaibab Limestone The K Kaibab Formation aibab F o r m a t i o n is i s extensively e x t e n s i v e l y eexposed x p o s e d at a t the t h e Grand Grand »" and H Hurricane Cliffs, Mogollon Canyon, Grand Grand Wash and urricane C liffs, M o g o l l o n Rim, Circle Circle Cliffs, Rafael of the Little C l i f f s , San R a f a e l Swell, S w e l l , and and pparts a r t s of the L i t t l e Colorado C o l o r a d o River River Valley. Valley. In Kaibab Formation widely I n the t h e Paria P a r i a area a r e a the the K aibab F o r m a t i o n is is w i d e l y exposed exposed on F Fivemile Mountain. ivemile M ountain. The yellow y e l l o w and and ggray r a y limestone l i m e s t o n e is i s in i n sharp sharp contrast of tthe Formation. c o n t r a s t tto o tthe h e rred e d siltstone s i l t s t o n e of h e Moenkopi Moenkopi F ormation. The upper upper ppart a r t of of the the K aibab F o r m a t i o n is i s vvery e r y resistant r e s i s t a n t tto o erosion e r o s i o n and and Kaibab Formation conforms of tthe Kaibab conforms tto o tthe h e structure s t r u c t u r e of he K a i b a b uuplift. plift. Nume~ous consequent Numerous consequent g u l c h e s hhave a v e cut c u t into i n t o the t h e dipslope d i p s l o p e of of this t h i s resistant r e s i s t a n t uupper p p e r unit unit gulches e x p o s i n g tthe h e older o l d e r uunits n i t s of t h e fformation. ormation. exposing of the Sand G u l c h has h a s cut cut Sand Gulch t h r o u g h tthe h e northern n o r t h e r n eedge d g e of of Fivemile Fivemile M o u n t a i n and and exposes e x p o s e s over o v e r 150 150 through Mountain f e e t of of tthe h e alternating a l t e r n a t i n g hard h a r d and s o f t strata s t r a t a that t h a t compose compose the the feet and soft Formation. Kaibab Formation. In Kaibab I n Sand Gulch G u l c h the the K a i b a b is i s divisible d i v i s i b l e into i n t o four f o u r dist.inct distinct units u n i t s on tthe h e bbas a s iis s of of llandforms; a n d f o r m s ; tthe h e two uuppermos p p e r m o s t units u n i t s are are Alpha Hember and and tthe pprobably r o b a b l y correlative c o r r e l a t i v e with w i t h McKee's McKee*s A l p h a Member h e two Jm.;rermost lowermost ul~nits n i t s aar2 r e pprobably r o b a b l y equivalent e q u i v a l e n t to t o his h i s Be B e ta t a }Iember, Member, Only Only ppart a r t of of tthe h e Beta B e t a Member is i s exposed e x p o s e d iin n tthe h e Paria P a r i a area. area. o l d e s t eexposed x p o s e d uunit n i t is i s a llimy, i m y , cherty, c h e r t y , extremely e x t r e m e l y resistant resistant The oldest s a n d s t o n e tthat h a t £O).:1:1S f o r m s a lledge e d g e and a r r o w ccanyon a n y o n in i n tthe h e bbottom o t t o m of sandstone and nnarrmV' Sand Gulch Gulch (Fig. ( F i g . 6). 6). Sand n i t is i s composed composed of of ll-to-3 - t o - 3 foot f o o t beds b e d s that that The uunit c o n t a i n abundant a b u n d a n t chert c h e r t and and iron-'rich i r o n - r i c h nnodules; o d u l e s ; numerous numerous contain poorly poorly 22 ppreserved r e s e r v e d fossils f o s s i l s aare r e associated associated w i t h these t h e s e nodules. nodules. \.Jith About About 16 f e e t of h i s uunit n i t are a r e exposed e x p o s e d iin n Sand Sand Gulch. Gulch, feet of tthis The ssteep \o7a1ls of m mas t e e p llower ower w a l l s aare r e composed composed of a ssive, s i v e , yellow, yellow, c h e r t y , ffossiliferous o s s i l i f e r o u s llimestone. imestone. cherty, The cchert h e r t ooccurs c c u r s in i n beds, beds, l e n s e s , nnodules, o d u l e s , and and stringers s t r i n g e r s and and iis s ooften f t e n ccovered overed w i t h impressions impressions lenses, Hith of of delicate d e l i c a t e bbryozoans, r y o z o a n s , corals, c o r a l s , and and sponges. sponges. The fevl few bbedding e d d i n g planes planes in weather i n the t h e uunit nit w e a t h e r as a s nnotches, o t c h e s , lledges, e d g e s , oor r ccaves a v e s in i n tthe h e otherwise otherwise uunbroken n b r o k e n cliffs. cliffs. N e a r tthe h e ttop o p the t h e uunit n i t becomes ess m a s s i v e and and Near becomes lless massive forms and cliffs. forms lledges e d g e s and cliffs. The entire e n t i r e uunit n i t is i s 88 ffeet e e t thick. thick. Alpha Member of Kaibab Formation of two The A l p h a Member of tthe he K aibab F o r m a t i o n cconsists o n s i s t s of distinct \o7eak, d i s t i n c t uunits; n i t s ; tthe h e llower o w e r uunit n i t iis s a w e a k , wavy bbedded e d d e d yellm-l yellow limestone \o7ith and sand. l i m e s t o n e about a b o u t 30 ffeet e e t tthick, hick, w i t h considerable c o n s i d e r a b l e silt s i l t and sand. T h i s uunit n i t c.:mtains c o n t a i n s bboth o t h bedded b e d d e d and and nnodular o d u l a r chert, chert, This The bedding Th~ wavy HiWy beddi.ng i s quite q u i t e distinct d i s t i n c t and and iis s due iin n ppart a r t tto o ripple r i p p l e laminations, l a m i n a t i o n s , though though is of tthe h e "waves" " w a v e s " aare r e several s e v e r a l ffeet e e t llong o n g with w i t h amplitudes a m p l i t u d e s of to some of of 6 to inches. 8 inches. Most of of the t h e limestone l i m e s t o n e beds b e d s are a r e 6 feet f e e t thick t h i c k and are are Host s e p a r a t e d by chert c h e r t bbeds, e d s , silt s i l t bbeds, e d s , oor r distinct d i s t i n c t wavy bbedding e d d i n g planes. planes. separated of tthe h e llin"ty i m y bbeds e d s ccontain o n t a i n eenough n o u g h sand s a n d tto o bbe e classified c l a s s i f i e d as as Some of sandstones. sandstones. The sand s a n d is i s very v e r y fine f i n e and and aalmost l m o s t ppure ure w h i t e "lith w i t h 'o7hite x^hite \o7hite mica he m a j o r accesso a c c e s s o rry y .. mica tthe major T h i s uunit n i t forms f o r m s a stepped s t e p p e d ccliff l i f f or or This r u b b l e - c o v e r e d slope. slope. "Cubble-covered The uupper p p e r 30 ffeet e e t of of tthe he A l p h a Member c o v e r s about a b o u t 90 Alpha Hember covers ppercent e r c e n t of h e ttotal otal K a i b a b ooutcrop u t c r o p aarea r e a .. of tthe Kaibab T h i s cap c a p rrock o c k of the This of the Kaibab F Formation medium·- tto o r m a t i o n iis s a mediumo tthick--bedded, h i c k - b e d d e d , deep·-yello~", deep-yellow, ccross-lwllinated r o s s - l a m i n a t e d limestone Limestone w i t h no cchert h e r t and o n l y vvery e r y poorly poorly w'ith and only 23 p r e s e r v e d fossils. fossils. preserved t h i c k n e s s of of the t h e bedding b e d d i n g vvaries. aries. The thickness Some beds beds a p p e a r to t o bbe e massive, m a s s i v e , but b u t when ttraced r a c e d along a l o n g strike,weather s t r i k e , w e a t h e r into into appear b e d s about a b o u t a foot f o o t thick. thick. beds f e e t tthick. hick. feet Most of tthe h e beds b e d s are a r e bbetween e t w e e n 1I and M ost of and 4 T h i s is i s the t h e only o n l y unit u n i t of of the t h e Kaibab K a i b a b tthat h a t contains contains This a b u n d a n t cross c r o s s llaminations a m i n a t i o n s and and intraclasts i n t r a c l a s t s (ripped-up, ( r i p p e d - u p , semisemiabundant c o n s o l i d a t e d intra-fonnational intra-formational m a t e r i a l rredeposited e d e p o s i t e d by currents). consolidated material by currents). n i t weathers w e a t h e r s into i n t o slabby s l a b b y cliffs. cliffs. The uunit Most Most of of the t h e limestone l i m e s t o n e of of tthe h e Paria P a r i a area a r e a ccan a n bbe e classified classified as -this a s microsparite m i c r o s p a r i t e ((Folk, F o l k , 1959, 1 9 5 9 , p. p . 32) 3 2 ) -— t h i s is i s substantiated s u b s t a n t i a t e d by Brown (1969, ( 1 9 6 9 , pp.. 171). 171). The u pppe p e r ppart a r t of of the the A l p h a Member is Alpha Member is intramicrite. intramicrite. On tthe FOTIl1ation h e bbasis a s i s of of numerous n u m e r o u s fossils, f o s s i l s , the t h e Kaibab Kaibab F o r m a t i o n is is equivalent San Andres e q u i v a l e n t to t o the t h e Leonard L e o n a r d Formation F o r m a t i o n of of West Texas, T e x a s , tthe h e San Andres Limestone L i m e s t o n e of of New Mexico, M e x i c o , tthe h e lm'ler l o w e r part p a r t of of the t h e Phosphoria-Park Phosphoria-Park City C i t y of of the t h e northern n o r t h e r n int i n t eerrmount m o u n t aain i n region, r e g i o n , and a n d several s e v e r a l Middle Middle Pennian e, 1938, P e r m i a n formations f o r m a t i o n s of of southern s o u t h e r n Arizona A r i z o n a (McKe (McKee, 1 9 3 8 , pp.. 169-176). 169-176). Fossils F o s s i l s found f o u n d in i n the t h e Paria P a r i a area a r e a include: include: Brachiopods Brachiopods Peniculauri P e p i q u i a u r i ss bassi bassi P;~tus P r o d u c t u s CD'i'Z;.y';c-lostus) ( P i c t y o c l o s t u s ) occ O c ci dental:Ls identalls Echinauris subhorrida E c h i n a u r i s s u b h o r r i d a ----Koslowskia K o s l o w s k i a meridionalis meridional1s Bryozoans Bryozoans Fenestrate F e n e s t r a t e forms forms Massive M a s s i v e fonns forms Pe P e lecypod l e c y p o d fragmen f r a g m e nts ts Crinoid C r i n o i d co c olumnals lumnals -------- The Kaibab by shal.lo K a i b a b Formation F o r m a t i o n ~"as was deposi.ted d e p o s i t e d by s h a l l o wt,,, sseas e a s that that trans t r a n s ggres r e s ssed e d from from the t h e southeast. southeast. Duri:c.g D u r i n g mos m o s t of of tthe h e Kaibab Kaibab deposition r e between Lees Ferry &nd the d e p o s i t i o n the t h e shoreline s h o r e l i n e lay l a y some.,,,,he somewhere between L ees F e r r y and the 24 Monument ~lonument upwarp. up_varp. B e t a Member d e p o s i t e d ina i n a sstanding t a n d i n g sea sea The Beta Nember was deposited with w i t h minor m i n o r regressions, r e g r e s s i o n s , especially e s p e c i a l l y nnear e a r the t h e eastern e a s t e r n sshore h o r e (McKee, p . 13; i 3 ; Brown, 1969, 1 9 6 9 , pp.. 171). 171). 1938, p. b u n d a n t sandstone s a n d s t o n e and The aabundant siltstone l-fuite s i l t s t o n e are a r e pprobably r o b a b l y related r e l a t e d to, t o , and derived d e r i v e d from, f r o m , tthe he W h i t e Rim and DeChelly D e C h e l l y Sandstone S a n d s t o n e Members of of the t h e Cutler C u t l e r Formation F o r m a t i o n --both •—both continental c o n t i n e n t a l and marine(?) m a r i n e ( ? ) equivalents e q u i v a l e n t s of of the t h e Kaibab K a i b a b iin n tthe h e eastern eastern p l a t e a u country. country. plateau The Alpha A l p h a Member was deposited d e p o s i t e d bby y a regressing r e g r e s s i n g ssea e a (McKee, 1 9 3 8 , p. p . 13; 1 3 ; Brown, Erown, 1969, 1 9 6 9 , p. p . 171). 171). 1938, c r o s s laminations, l a m i n a t i o n s , intraclasts, intraclasts The cross t h i n n e r bbeds e d s show that t h a t increasing i n c r e a s i n g energy e n e r g y was aassociated ssociated w i t h this this and thinner with regression. regression. C o n s e q u e n t l y fossils f o s s i l s are a r e poorly p o o r l y ppreserved, r e s e r v e d , or o r rrare, a r e , or or Consequently both. both. Permian-Triassic P e r m i a n - T r i a s s i c Boundary Boundary Wherever Wherever the t h e Kaibab K a i b a b Formation F o r m a t i o n is i s ppresent r e s e n t iin n southern s o u t h e r n Utah Utah and nnorthern Arizona, orthern A r i z o n a , the t h e Permian-Triassic P e r m i a n - T r i a s s i c bboundayy o u n d a r y ii.s s generally generally sharp s h a r p and easily e a s i l y rrecognized. ecognized. In I n tthe h e Lees L e e s Ferry F e r r y area a r e a llocal o c a l scouring scouring to ~vere t o depths d e p t h s as a s much as a s 25 feet feet w e r e seen s e e n (Phoenix, ( P h o e n i x , 1963, 1 9 6 3 , pp.. 13). 13). Davidson Cliffs D a v i d s o n (1967, ( 1 9 6 7 , p. p . 13-15) 1 3 - 1 5 ) rreports e p o r t s that t h a t in i n the t h e Circle Circle C l i f f s area area the t h e Kaibab K a i b a b is i s locally l o c a l l y absent a b s e n t beca b e c a uuse s e of of Late L a t e Permian P e r m i a n and Early Early T r i a s s i c erosion. erosion. Tr-iassie Where erosion e r o s i o n surfaces s u r f a c e s are a r e indistinct, i n d i s t i n c t , sharp s h a r p color color l i t h o l o g i c chang::::s changes m a r k the t h e contact. contact. and lithologic mark However, iin n tthe he Z ion However, Zion and a r e a s where w h e r e the t h e TimpO\\1e Timpoweap Member of of the t h e Moenkopi Moenkopi F o r m a t i o n is is Kanab areas ap i1ember Formation p r e s e n t the t h e bboundary o u n d a r y is i s oft o f t eenn difficult d i f f i c u l t tto o establish e s t a b l i s h on physical present on physical e v i d e n c e and paleontological p a l e o n t o l c g i c a l cr:itel'ia c r i t e r i a are a r e needed. needed. evidence IIn n tthe h e PParia a r i a aarea r e a tthe h e PPermian-Triassic e r m i a n - T r i a s s i c bboundary o u n d a r y iis s obvious obvious from i s t a n c e bbecause e c a u s e of h a r p ccolor o l o r cchange h a n g e and contrasting from a ddistance of a ssharp and contrasting llithologies. ithologies. sseen. een. At l o s e iinspection n s p e c t i o n a 33-- tto o 55-foot - f o o t ttransition r a n s i t i o n zzone o n e is is At cclose T h i s uunit n i t iis s a yyellow, ellow, m o t t l e d , llimy, i m y , ssilty, i l t y , ffissile, i s s i l e , crumbly crumbly This mottled, m udstone. mudstone. The o w e r ccontact ontact w i t h tthe he K a i b a b iis s nnot ot w e l l eexposed x p o s e d but but The llOvler with Kaibab well iis s uusually s u a l l y a rrubble-covered u b b l e - c o v e r e d ssurface--the u r f a c e — t h e rrelief e l i e f iis s lless e s s tthan h a n several several ffeet e e t and r o b a b l y iis s nnearly e a r l y pplanar. lanar. and pprobably C o n g l o m e r a t e was nnot o t evident. evident. Conglomerate p p e r ccontact ontact w i t h tthe h e Lower of tthe h e Moenkopi Formation The uupper with Lower Red Red Member Hember of Moenkopi Formation iis s m o t t l e d and r a d a t i o n a l , and t fforms o r m s a sinuous s i n u o u s ccontact ontact w h a mottled and ggradational, and iit \-lii tth rrelief e l i e f of of several s e v e r a l ffeet. eet. A g a i n cconglomerates o n g l o m e r a t e s aare r e nnot o t present. present. Again T h i s uunit n i t hhas a s tthe h e color c o l o r of of tthe he K a i b a b bbut u t tthe h e llithology i t h o l o g y is is This Kaibab s i m i l a r tto o tthat h a t of of tthe he M oenkopi. similar Moenkopi. The uunit n i t is i s discontinuous d i s c o n t i n u o u s locally locally for wherever Kaibab-Moinkpi f o r a few few feet f e e t bbut ut w h e r e v e r tthe he K a i b a b - M o i n k p i contaci: c o n t a c t is i s well well exposed it i t is i s present. present. exposed The significance s i g n i f i c a n c e of of this t h i s unit u n i t is i s nnot o t clear. clear. It I t may represent represent the t h e final f i n a l fe f e aather t h e r edge e d g e of of the t h e Timpoweap Member of of tthe h e Moenkopi Moenkopi which which pinches p i n c h e s out o u t jjust u s t a few miles m i l e s v!est w e s t of of the t h e Paria P a r i a River, R i v e r , or o r it i t may be be the t h e result r e s u l t of of the t h e reduction r e d u c t i o n of of iron I r o n by hydrocarbons h y d r o c a r b o n s causing c a u s i n g a color color change from from r eedd to t o yellow. yellow. Without W i t h o u t fossil f o s s i l evidence e v i d e n c e or o r a more detailed detailed study, s t u d y , definite d e f i n i t e conclusions c o n c l u s i o n s can c a n not n o t be b e made. made, Triassic T r i a s s i c .System System Noenkopi Moenkopi Formation Formation Moenkopi F o r m a t i o n of of Ea E arly r l y and i-fiddle M i d d l e (?) ( ? ) Triassic T r i a s s i c age age The N :oe nkopi Formation was named i.)y by 1iard Ward (1901, ( 1 9 0 . 1 , p. p . 403) fo f o r~c r oocks c k s exposed e x p o s e d in i n the t h e valley v a l l e y of of 26 t h e Little L i t t l e Colorado Colorado R i v e r nnear ear M oenkopi, A rizona. the River MOenkopi, Arizona. I t is i s a wedgewedgeIt shaped shaped deposit d e p o s i t that t h a t thickens t h i c k e n s from from a feather f e a t h e r edge e d g e in i n eastern-most eastern-most Utah to t o almost a l m o s t 2000 feet f e e t in i n the t h e St. S t . George, G e o r g e , Utah, U t a h , area. area. East E a s t of the t h e Colorado C o l o r a d o River R i v e r the t h e Moenkopi Moenkopi is i s dominantly d o m i n a n t l y red r e d continental continental siltstone s i l t s t o n e and sandstone. sandstone. West of of the t h e Colorado C o l o r a d o River R i v e r the t h e grain g r a i n size size f i n e r and continental c o n t i n e n t a l rrocks o c k s interfinger i n t e r f i n g e r with w i t h marine m a r i n e rocks rocks becomes finer westward. westward. and limestone l i m e s t o n e become increasingly i n c r e a s i n g l y more m o r e abundant abundant Gypsum and i n southern s o u t h e r n Nevada Nevada most m o s t of of the t h e Hoenkopi Moenkopi is i s marine. marine. and in source The source of the t h e clastics e l a s t i c s in I n the t h e Moenkopi r o b a b l y were w e r e tthe h e Ancestral A n c e s t r a l Rockies Rockies of Moenkopi pprobably e a s t w a r d and tthe h e Mogollon M o g o l l o n Highlands H i g h l a n d s southward. southward. eastward (McKee, 1954) 1954) In the Hoenkopi I n the t h e Paria P a r i a area a r e a the. Moenkopi Formation F o r m a t i o n unconformably unconformably overlies o v e r l i e s the t h e Kaibab K a i b a b Formation F o r m a t i o n and uunconformably n c o n f o r m a b l y underlies u n d e r l i e s tthe h e Chinle Chinle Formation. Formation. The ooutcrop u t c r o p of of the t h e formation f o r m a t i o n cconforms o n f o r m s to t o the t h e structure structure of the t h e Kaibab K a i b a b upwarp-u p w a r p — the t h e broad b r o a d outcrop o u t c r o p ppattern a t t e r n iin n the t h e northwest northwest of corner c o r n e r of of the t h e map area a r e a abruptly a b r u p t l y nnarrows a r r o w s along a l o n g tthe h e flank f l a n k of of the the uplift. uplift. t o t a l thickness t h i c k n e s s of of tthe h e Hoenkopi Moenkopi Formation F o r m a t i o n on the the The total northwest n o r t h w e s t part p a r t of of the t h e map area a r e a is i s 760 feet. feet. The Hoenkopi Format:1on Moenkopi F o r m a t i o n of of the t h e Paria P a r i a area a r e a lies l i e s in i n the t h e zone zone of interfingering i n t e r f i n g e r i n g marine m a r i n e and non-marine n o n - m a r i n e rocks. rocks. of resulting The resulting complex lithology l i t h o l o g y consists c o n s i s t s of of siltstone, s i l t s t o n e , sandstone, s a n d s t o n e , shaly s h a l y mudstone, muds t o n e , complex l i m e s t o n e , and ggypsum. ypsum. limestone, The definitions d e f i n i t i o n s of of the t h e five f i v e members of of the the F o r m a t i o n of of the the P a r i a area a r e a are a r e based b a s e d on lithology l i t h o l o g y and and Moenkopi Formation Paria e n v i r o n m e n t (marine ( m a r i n e versus v e r s u s ttidal i d a l fla f l a tt). ). environment a r e , in in The members members are, a s c e n d i n g order, o r d e r , the t h e Lower Lower Red Member, Virgin Virgin L i m e s t o n e Member, Member, ascending Limestone Middle Red Member, S h n a b k a i b Member, Upper Red Hember. Member. Hember, and Upper 11iddle Nember, Shnabkaib 27 The age a g e of of tthe h e Moenkopi Moenkopi Formation F o r m a t i o n is i s bbased a s e d on tthe h e ammonite ammonite T r i o l i t ees s ,, w h i c h hhas a s bbeen e e n found f o u n d iin n tthe he V irgin L i m e s t o n e Member in i n the the '!!iolit which Virgin Lilllestone S t . George G e o r g e area. area. St. T h i s ammonite ammonite is i s a guide g u i d e tto o tthe h e uupper p p e r ppart a r t of of the the This T r i a s s i c (Poborski, ( P o b o r s k i , 1954, 1 9 5 4 , pp.. 993). 993). Lower Triassic B e c a u s e of of this t h i s Repenning Repenning Because e t h e r s (1969 pp.. B13) state s t a t e that t h a t the t h e uupper p p e r members of the the and others members of M i d d l e Triassic. Triassic. Moenkopi may be be Middle Member Lower Red Hember The Lower of tthe Moenkopi FFormation Lower Red Member of h e Moenkopi o r m a t i o n (Huntington (Huntington and Goldthwait, G o l d t h w a i t , 1903, 1 9 0 3 , pp.. 48) 4 8 ) is i s rrecognized e c o g n i z e d oonly n l y iin n southwestern s o u t h w e s t e r n Utah Utah and northwestern where n o r t h w e s t e r n Arizona Arizona w h e r e it i t uunconformably n c o n f o r m a b l y overlies o v e r l i e s tthe h e Kaibab Kaibab Formation; west Member of F o r m a t i o n ; further further w e s t it i t overlies o v e r l i e s the t h e Timpoweap Member of the the Moenkopi F Formation. ormation. The member member thickens t h i c k e n s tto o 310 feet f e e t nnear e a r St. S t . George George (Gregory ( G r e g o r y 1950, 1 9 5 0 , pp.. 660)-0 ) — the t h e gypsum gypsum ccontent o n t e n t also a l s o increases i n c r e a s e s in i n that that direction. direction. In Member unconformably I n the t h e Paria P a r i a area a r e a the t h e Lower Lower Red Member unconformably overlies Kaibab o v e r l i e s tthe he K a i b a b Formation F o r m a t i o n and cconformably o n f o r m a b l y (?) ( ? ) uunderlies n d e r l i e s the the V i r g i n Limestone L i m e s t o n e member. Virgin B o t h contacts c o n t a c t s are a r e rreadily e a d i l y recognizable recognizable Both a e r i a l photographs. photographs. on aerial The member i s 141 1 4 1 feet f e e t tthick h i c k and f o r m s ggentle, e n c l e , stepped stepped member is and forms s l o p e s and bbroad r o a d valleys v a l l e y s bbut u t llocally o c a l l y along a l o n g Road r e e k recent recent slopes Road C Creek s t r e a m rrejuvenation e j u v e n a t i o n hhas a s cut c u t sheeJ:." s h e e r cliffs c l i f f s iinto n t o tthe h e uunit n i t exposing exposing stream tthe h e intricate i n t r i c a t e bedding b e d d i n g (fig. ( f i g . 7). 7). The Lower Nember cconsists Lower Red Member o n s i s t s of of llight i g h t reddish-brown, reddish-brown, micaceous, with m i c a c e o u s , silty, s i l t y , thin-bedded t h i n - b e d d e d tto o fissile f i s s i l e ; silty s i i t y shale shale w i t h interinter­ bedded sandstone bedded s a n d s t o n e and and rripple i p p l e mark m a r k eed d s i lltstone. tstone. The lower l o w e r 6lf 64 feet f e e t of of 28 28 the with t h e member are a r e eentirely n t i r e l y siltstone s i l t s t o n e and mudstone mudstone w i t h no sand s a n d units units present. present. T h i s unit u n i t is i s ripple-marked, r i p p l e - m a r k e d , micaceous, m i c a c e o u s , and vvery e r y thin thin This bedded--it bedded i t forms f o r m s gentle g e n t l e slopes s l o p e s and and occasional o c c a s i o n a l low steps. steps. Stewart Stewart and others o t h e r s (1959, ( 1 9 5 9 , p. p . 542) 5 4 2 ) report r e p o r t that t h a t on an a n average a v e r a g e the t h e finerfinergrained g r a i n e d units u n i t s of of the t h e Moenkopi Formation F o r m a t i o n have h a v e angular a n g u l a r grains g r a i n s and aa high h i g h ppercentage e r c e n t a g e of of feldspar, f e l d s p a r , and and should s h o u l d be b e classified c l a s s i f i e d as a s arkose. arkose. At 6/. 64 feet f e e t above a b o v e the t h e bbase, a s e , the t h e first f i r s t ppoorly o o r l y sorted, s o r t e d , angular, angular, thin-bedded, t h i n - b e d d e d , rripple-laminated i p p l e - l a m i n a t e d silty s i l t y sandstone s a n d s t o n e appears. appears. Beds of sandstone s a n d s t o n e fonl form conspicuous c o n s p i c u o u s ledges l e d g e s and low cliffs c l i f f s on the t h e otherwise otherwise gentle g e n t l e slope, s l o p e , and and they t h e y increase i n c r e a s e in i n thickness t h i c k n e s s and number number towards t o w a r d s the the top t o p of of tthe h e member. These T h e s e beds b e d s are a r e generally g e n e r a l l y 1 to t o 4 feet f e e t thick t h i c k but but some are a r e almost a l m o s t 10 feet f e e t thick t h i c k and according a c c o r d i n g to t o Stewart S t e w a r t and others others ( 1 9 5 9 , p. p . 542), 5 4 2 ) , on the t h e average a v e r a g e are a r e also a l s o arkoses. arkoses. (1959, The upper u p p e r 18 feet f e e t consists c o n s i s t s of of limy, l i m y , sandy, s a n d y , lighter-colored, lighter-colored, t h i n - tto o medium-bedded m e d i u m - b e d d e d siltstone siltstone w i t h numerous n u m e r o u s sedimentary s e d i m e n t a r y structures. structures. thinVlith Asymmetric rripple i p p l e marks, m a r k s , interference i n t e r f e r e n c e ripple r i p p l e marks, m a r k s , small s m a l l load l o a d casts, casts, Asymmetric complex cross c r o s s l aaminations, m i n a t i o n s , and and cut c u t and fill f i l l structures s t r u c t u r e s are a r e common. complex T h i n - b e d d e d as a s well w e l l as a s cross--cutting c r o s s - c u t t i n g gypsum gypsum iis s present. present. Thin-bedded T h i s unit unit This i s gradational g r a d a t i o n a l "lith w i t h tthe h e overlying o v e r l y i n g Virgin V i r g i n Limestone L i m e s t o n e and forms f o r m s a steep, steep, is l e d g y , light-colored l i g h t - c o l o r e d slope. slope. 1edgy, The sedimentary Hember clearly s e d i m e n t a r y structures s t r u c t u r e s of of the t h e Lower Lower Red Member clearly indicate i n d i c a t e increasing i n c r e a s i n g energy e n e r g y from from bottom b o t t o m to t o top. top. Thin T h i n horizontal horizontal bedding b e d d i n g and ripple r i p p l e marks m a r k s at a t ·tt hhe e bottom b o t t o m of of tthe h e member member give g i v e way to to load more l o a d casts, c a s t s , scour s c o u r marks, m a r k s , complex complex cross c r o s s laminations, laminations, m o r e complex complex r i p p l e marks, m a r k s , larger l a r g e r grain g r a i n size s i z e and and tthicker h i c k e r bbedding, e d d i n g , althoug a l t h o u g hh the the ripple 29 t h i c k e s t bbeds e d s in i n tthe h e entire e n t i r e member member are a r e only o n l y several s e v e r a l iinches n c h e s thick. thick. thickest The rresistant e s i s t a n t sandstones, s a n d s t o n e s , often o f t e n ttraceable r a c e a b l e for f o r several several miles, m i l e s , form form key k e y bbeds e d s in i n the t h e ootherwise t h e r w i s e ggentle e n t l e sloping s l o p i n g surface s u r f a c e of of the t h e Lower Red Member. from butte Many of of tthese h e s e bbeds e d s can c a n be b e ttraced r a c e d from butte to western t o butte b u t t e and are a r e uuseful s e f u l rreference e f e r e n c e pplanes l a n e s in i n the the w e s t e r n ppart a r t of of t h e map area. area. the No fossils f o s s i l s were w e r e found f o u n d in i n the t h e Lower Lower Red l1ember Member bbut u t jjust u s t west west of and overlies of the t h e mapped mapped aarea r e a it i t uunderlies n d e r l i e s and o v e r l i e s marine m a r i n e llimestone i m e s t o n e that that contain Early Early c o n t a i n an E a r l y Triassic T r i a s s i c fauna, f a u n a , so s o tthe h e age a g e is is E a r l y Triassic. Triassic. The Lower Formation Lower Red Hember Member of of tthe h e Moenkopi Moenkopi F o r m a t i o n is i s probably probably equivalent e q u i v a l e n t tto o tthe h e llower o w e r siltstone s i l t s t o n e member member tthat h a t is i s present p r e s e n t in i n the the Monument Valley of southeastern Utah, V a l l e y area a r e a and and pparts a r t s of southeastern U t a h , bbut u t it i t is is older Hoenkopi F FOHudtion r.'.03t o l d e r tthan h a n tthe h e bbasal a s a l uunits n i t s of of tthe h e Moenkopi o r m a t i o n in in m o s t cf of Arizona Mexico (Repenning and oothers, A r i z o n a and New Mexico ( R e p e n n i n g and t h e r s , 1969, 1 9 6 9 , pp.. B5). B5). Virgin V i r g i n L.i..mest6neHember L i m e s t o n e Member The V Virgin of the Moenkopi F Formation i r g i n Limestone L i m e s t o n e Member of t h e Moenkopi o r m a t i o n was first by Reeside and B Bassler Poborski f i r s t named by R.eeside and a s s l e r ((1.922, 1 9 2 2 , pp., 660); 0); P o b o r s k i (1954, (1954, pp.. 974) raised r a i s e d it i t tto o formational f o r m a t i o n a l status s t a t u s and c h aanged n g e d the t h e sta,tUG s t a t u s of of and ch Moenkopi from tthe h e Moenkopi from formation f o r m a t i o n tto o group. group. Because widerallging B e c a u s e of of w ide ranging regional r e g i o n a l implications, i m p l i c a t i o n s , tthis h i s s uugg g g est e s t iion o n hhas a s ggenerally e n e r a l l y nnot o t been been followed. followed. The V Virgin of the i r g i n Lline L i m estone s t o n e iis s treated t r e a t e d as a s a member of the Moenkopi iin Moenkopi n this t h i s report. report. V i r g i n Limes L i m e s tone t o n e Hember Member is i s rrecognized e c o g n i z e d in i n soutluvestern southwestern The Virgin Utah Arizona Eas Kaibab Utah afl.d and northern northern A r i z o n a ,lest w e s t of of tthe he E ast K a i b a b Monocline M o n o c l i n e aud and tthickens h i c k e n s from from 12 feet f e e t in i n the t h e Faria P a r i a a.:rrrea e a to t o about a b o u t 200 ffeet e e t in i n the the . , 30 ~o St r e a ((Porborski, P o r b o r s k i , 11954, 9 5 4 , pp.. 9975). 75). St. George George aarea IIn n tthe he S t . George George St. and r e a s a ddistinct i s t i n c t uunconformity n c o n f o r m i t y iis s ppresent r e s e n t aat t tthe h e base base and Zion Zion aareas ((Porborski, P o r b o r s k i , 11954; 954; G r e g o r y , 1950) u t iin n tthe h e PParia a r i a aarea r e a tthe h e contact contact Gregory, 1950) bbut iis s ttransitional r a n s i t i o n a l ((?) ? ) aas s ddescribed e s c r i b e d iin n tthe h e ppreceding r e c e d i n g sections. sections. Virgin Limestone Member lies IIn n tthe h e PParia a r i a aarea r e a tthe he V irgin L i m e s t o n e Member lies conformably L01.;er and and M Nidd1e Red Members Hembers of of the c o n f o r m a b l y bbetween e t w e e n tthe h e Lower i d d l e Red the Moenkopi ormation. Moenkopi FFormation. B o t h ccontacts o n t a c t s aare r e somewhat r a n s i t i o n a l but but Both somewhat ttransitional viewed h o r t ddistance i s t a n c e tthe h e ccolor o l o r and i t h o l o g i c differences differences viewed from from a sshort and llithologic aare r e vvery e r y ssharply h a r p l y ddefined. efined. The V i r g i n iis s oonly n l y 12 ffeet e e t tthick h i c k on Virgin tthe he w e s t e r n ppart a r t of of tthe h e map area, a r e a , hhowever, o w e v e r , iit t iis s rreadily e a d i l y mappable mappable western bbecause e c a u s e of of tthe h e land l a n d forms f o r m s iit t ccrea r e a tte e s ;; iit t is is a m e s a - c a p p i n g unit unit mesa-capping on tthe h e extreme extreme w e s t eedge d g e of h e map a r eea a and o g b a c k - f o r m e r to to wes of tthe and a hhogback-former tthe h e south s o u t h iin n F i v e m i l e Valley. Valley, Fivemile Member i ss a tthinThe Virgin V i r g i n Limestone L i m e s t o n e Member h i n - tto o medium-bedded, medium-bedded, y e l l o w , sandy s a n d y l iime m e stone, s t o n e , and bblue-gray, lue-gray, m i c a c e oous u s siltstone. siltstone. yellow, micace Some of with of tthe h e siltstone s i l t s t o n e bbeds e d s show no react r e a c t iion o n at a t all all w i t h acid a c i d and and therefore t h e r e f o r e have h a v e little l i t t l e or o r no lime l i m e cont c o n t ent. ent, Almost A l m o s t all a l l beds b e d s are are l e n t i c u l a r and individual i n d i v i d u a l beds b e d s are a r e not n o t traceable t r a c e a b l e for f o r more m o r e tban t h a n aa lenticular few yards. yards. fe\v The siltstone s i l t s t o n e is i s interb i n t e r b eedded d d e d thr t h r ooughout u g h o u t the t h e unit. unit. Ti18 v a r i e t y of of s e ddimentary i m e n t a r y structures s t r u c t u r e s a r ee present p r e s e n t throughout throughout A variety t h e member i nncluding c l u d i n g l eenticular n t i c u l a r bedding b e d d i n g ,, wavy bedding, b e d d i n g , minor minor the l o w - a n g l e cro c r o ss s s laminations, l a m i n a t i o n s , ripple r i p p l e marks m a r k s (more abundant a b u n d a n t on on low-angle s i l t s t o n e than t h a n limestone), l i m e s t o n e ) , and a number of of small s m a l l cut-·and-fill cut-and-fill siltstone c h a n n e l stru s t r u cctures t u r e s .. channel moderate m o d e r a t e ene e n ergy r g y .. a b o v e point p o i n t to t o an a n aqueous a q u e o u s enviromnent e n v i r o n m e n t of of The above .- 31 F o s s i l s aare r e llocally o c a l l y nnumerous u m e r o u s in i n the the V irgin L i m e s t o n e Member, Member, Fossils Virgin Limestone i n the t h e ppurer u r e r limestone l i m e s t o n e units u n i t s nnumerous u m e r o u s small, s m a l l , bbroken, r o k e n , poorly poorly and in _ j and uunidentifiable n i d e n t i f i a b l e sshell h e l l rremains e m a i n s ccan a n bbe e sseen e e n on close preserved, and on close c p r v e ( p }ffciIz> t-,L " y observation. Similar fossils have been found in the St. George area observation. Similar f o s s i l s have been found i n t h e S t . George area and the few that could be identified were mostly long-ranging, littleand t h e few t h a t c o u l d b e i d e n t i f i e d were m o s t l y l o n g - r a n g i n g , little- studied forms of slight stratigraphic value (Poborski, 195 1f, s t u d i e d forms of s l i g h t 1954, p . 9 9 1 - stratigraphic value (Poborski, p. 991- 992). Significant fossils were found in the St. George area that 992). Significant f o s s i l s were found i n t h e S t . George a r e a that can be used to date the Virgin. Tirolites spinosus as well as can be u s e d t o d a t e t h e V i r g i n . Tirolites spinosus as w e l l as (?)Cordillerites and (?)Hungarites were found by Poborski (1954, p. C ? ) C o r d i l l e r i t e s and ( ? ) H u n g a r i t e s w e r e f o u n d by P o b o r s k i (1954, p . 993); these arrmonites are characteristic of the Tirolites zone which 9 9 3 ) ; t h e s e a m m o n i t e s a r e c h a r a c t e r i s t i c of t h e T i r o l i t e s zone which is in the upper part of the Lower Triassic sequence of North America. i s i n t h e u p p e r p a r t of t h e Lower T r i a s s i c s e q u e n c e of N o r t h A m e r i c a . This zone is found in the upper part of the Thaynes Formation of This zone i s f o u n d I n t h e u p p e r p a r t of t h e T h a y n e s F o r m a t i o n of northern Utah (Poborski, 1954, p. 993; Smitlt, 1969 p. Ill). The n o r t h e r n Utah ( P o b o r s k i , The 1954, p . 993; Smith, 1969 p . 1 1 1 ) . Virgin Limestone Member is probably equivalent to part of the lower V i r g i n L i m e s t o n e Member i s p r o b a b l y e q u i v a l e n t t o p a r t of t h e lower siltstone member of the Hoenkopi Formation of the Honument Valley s i l t s t o n e member of t h e Moenkopi F o r m a t i o n of t h e Monument V a l l e y area and adjacent southeastern Utah, but equivalent beds are absent a r e a and a d j a c e n t s o u t h e a s t e r n Utah, but equivalent beds are absent in most of the N2vajo country (Reppening and others, 1969, p. B5). i n most of t h e N a v a j o c o u n t r y ( R e p p e n i n g and o t h e r s , 1969, p . B5). Middle Member Mid d1e Red Memb er Miiddl~ d d l e Red Member is i s similar s i m i l a r tto o tthe h e Lmver Lower Red Hember Member but but The H. contains c o n t a i n s more gypsum. It westward I t tthickens hickens w e s t w a r d to t o over o v e r 500 500 feet f e e t in in southwestern U t a h (Gregory, ( G r e g o r y , 1950, 1 9 5 0 , pp., 60) "ihe w h ere r e some local l o c a l limestone limestone southwestern Utah i s found. found. is i d d l e Red Member g e n e r a l l y recognized r e c o g n i z e d wherever w h e r e v e r the the The M Nidale Hember i ss generally Virgin L i m e s t o n e Member i s present. present. Virgin Limestone Member is IIn n the t h e l?aria P a r i a Clrea a r e a the t h e Hiddle M i d d l e Red Member cconformably o n f o r m a b l y overlies overlies the· Hember. t h e Shnabka.ib S h n a b k a i b Member. Both B o t h bboundaries o u n d a r i e s are a r e readily r e a d i l y rrecognized e c o g n i z e d by sharp sharp 32 o l o r chang c h a n ges. es. color The member is i s 344 ffeet e e t thick t h i c k in i n tthe h e northwest n o r t h w e s t corner corner of f the t h e map along a l o n g Road Creek C r e e k ,.,here w h e r e it i t forms f o r m s undulating u n d u l a t i n g hills h i l l s and 0 valleys where v a l l e y s except except w h e r e rrejuvenating e j u v e n a t i n g streams s t r e a m s hhave a v e cut c u t sheer s h e e r cliffs cliffs and canyons. canyons. Lithologically Lower Red L i t h o l o g i c a l l y tthe h e member member is i s similar s i m i l a r tto o the t h e Lower Red Member. Generally G e n e r a l l y iit t iis s a fissilef i s s i l e - to t o tthin-bedded h i n - b e d d e d reddish-brown reddish-brown shaly with s h a l y mudstone m u d s t o n e and and siltstone siltstone w i t h interbedded i n t e r b e d d e d poorly p o o r l y sorted sorted micaceous mudstone m i c a c e o u s sandstones s a n d s t o n e s and and thin t h i n bbeds e d s of of bblue-green lue-green m u d s t o n e associated associated with w i t h bedded bedded gypsum. Some bbeds mottled e d s are are m o t t l e d and massive. massive. Many seeps seeps of of the \vhere of water w a t e r are a r e found found in i n tthe h e nnorthwest o r t h w e s t area a r e a of t h e map w h e r e steep, steep, narrm-1 narrow canyons c a n y o n s have h a v e cut c u t iinto n t o the t h e ggypsiferous y p s i f e r o u s beds. beds. wide A w i d e vvariety a r i e t y of of rripple i p p l e marks, m a r k s , rripple i p p l e laminations, l a m i n a t i o n s , and and scour luarks marks aa;:e r e found f o u n d in i n tthe h e membe!.". member. scour a r e also a l s o present. present. are L o c a l cut-And-fill c u t - a n d - f i l l channels channels Local A l t h o u g h most m o s t of of tthe h e iindividual n d i v i d u a l bbeds e d s are a r e less l e s s than than Although s e v e r a l inches i n c h e s thick t h i c k some of h e bblue-green l u e - g r e e n cclaystone l a y s t o n e and and gypsum several of tthe l a y e r s are a r e persistent. persistent. layers No fossils Middle f o s s i l s hhave a v e bbeen e e n found f o u n d iin n the the M i d d l e Red Member but but P o b o r s k i (1954) (1954) bbelieves e l i e v e s it i t may bbe e Middle Middle T riassic. Poborski Triassic. I t iis s physically physically It continuous w i t h the t h e lower l o w e r ppart a r t of of tthe he W a p a t k i Member of of tthe h e Moenkopi Moenkopi continuous with Hapatki F o r m a t i o n of of tthe he L i t t l e Colorado C o l o r a d o River River V a l l e y (Repenning ( R e p e n n i n g and and others, others, Formation Little Valley 1969, p. B8). , B 8). p §,hnabkaibHenlber Shnabkaib Member L i k e other o t h e r members of of tthe h e Moenkopi Moenkopi F o r m a t i o n the t h e Shnabkaib Shnabkaib Like Fonnation Member (Reeside and B Baassler, westward ( R e e s i d e and s s l e r , 1922, 1 9 2 2 , pp.. 60) tthickens hickens w e s t w a r d and and attains Utah a t t a i n s a tthick11c h i c k n e scls s of of 376 feet f e e t nnear e a r St. S t . George, George, U t a h (Gregory, ( G r e g o r y , 1950, 1950, 33 p 60). 60). p. i t is ggenerally e n e r a l l y nnot o t rrecognized e c o g n i z e d eeast a s t of Paria. It of Paria. i s The nnarrow, a r r o w , curved c u r v e d outcrop o u t c r o p pattern p a t t e r n of of tthe h e Shnabkaib S h n a b k a i b lies l i e s at at the t h e foot f o o t of of tthe h e Cockscomb Cockscomb and and tthen h e n curves c u r v e s westvlard w e s t w a r d along a l o n g the the Vermilion V e r m i l i ° Cliffs. Cliffs. n II tt forms f o r m s low, l o w , rrolling, o l l i n g , banded b a n d e d hills h i l l s that t h a t support support little l i t t l e vegetation v e g e t a t i o n (fig. ( f i g . 8). 8). Loca L o c ally l l y in i n tthe h e nnorthwest o r t h w e s t ppart a r t of of the the map area a r e a south s o u t h of of Gingham Gingham Skirt S k i r t Butte, B u t t e , rejuvenated r e j u v e n a t e d streams s t r e a m s have h a v e cut cut s i n u o u s slot s l o t canyons c a n y o n s up to t o 100 feet f e e t deep d e e p and and only o n l y 4 tto o 6 feet f e e t wide. wide. sinuous The Shnabkaib by the S h n a b k a i b Hember Member is i s distinguished d i s t i n g u i s h e d by t h e amount amount of of bedded bedded i t contains. contains. gypsum it a s a l and upper u p p e r contacts c o n t a c t s are a r e defined d e f i n e d by by The bbasal t h e lowermost l o w e r m o s t and and uuppermost p p e r m o s t 5-foot 5 - f o o t gypsum bbeds e d s respectively respectively the ( s t r i k i n g on aerial a e r i a l photographs). photographs). (striking S h n a b k a i b Member is i s 164 feet feet The Shnabkaib t h i c k 1 mile m i l e south s o u t h of of the t h e movie m o v i e set. set. thick The Shnabkaib S h n a b k a i b Member is i s composed composed of of pale p a l e reddish-beown reddish-brown mudstone and siltstone s i l t s t o n e intercalated i n t e r c a l a t e d with w i t h light l i g h t bluish-gray b l u i s h - g r a y gypsum gypsum mudstone mudstone. and mudstone. e a t h e r e d outcrops o u t c r o p s these t h e s e alt2rnating a l t e r n a t i n g bands b a n d s are are 5 On w weathered t o 15 feet f e e t thick t h i c k bbut ut w h e r e rejuvenated r e j u v e n a t e d streruns s t r e a m s have h a v e exposed e x p o s e d the the to where rock, r o c k , these t h e s e tthick h i c k bbeds e d s can c a n be b e seen s e e n to t o consist c o n s i s t of of very v e r y intricately intricately stratified, s t r a t i f i e d , thin t h i n tto o fissile f i s s i l e beds. beds. The red r e d bands b a n d s are a r e comprised c o m p r i s e d of m u d s t o n e , siltstone, s i l t s t o n e , minor m i n o r sandstone s a n d s t o n e and thin t h i n beds b e d s of of gypsum gypsum and and the the mudstone, white w h i t e bands b a n d s consist: c o n s i s t : of of complexly c o m p l e x l y intercalated i n t e r c a l a t e d blue b l u e --green g r e e n mudstone m u d s t o n e and and n e a r l y ppure u r e (chemically) (chemically) w h i t e gypsum. gypsum. nearly Vlhite gypsum forms f o r m s tthe h e main main The gypsum cementing agent a g e n t in i n bboth o t h units. units. cementing The infrequ i n f r e q u eent n t ripple r i p p l e marks m a r k s and the t h e general g e n e r a l lack l a c k of of sedimentary sedimentary structures s t r u c t u r e s indicate i n d i c a t e that t h a t the t h e Shnabkaib S h n a b k a i b Membe Memberr 'I7a8 was deposited. d e p o s i t e d under u n d e r very very quiet q u i e t conditicns--this c o n d i t i o n s — t h i s is i s consistent c o n s i s t e n t "lith w i t h tthe h e pprecipitation r e c i p i t a t i o n of of gypsum. gypsum. F i g u r e 10.—Gingham S k i r t Butte. Butte, Figure lO.--Gingham Skirt Figure of Paria. F i g u r e 88.--Cockscomb . - - C o c k s c o m b ssouth o u t h of Paria. Figure Shinarump F i g u r e 99.--Channel . - - C h a n n e l in in S h i n a r u m p Member Member cut Moenkopi Formation. c u t in i n Moenkopi Formation. F i g u r e 12,—Cockscomb o o k i n g north north Figure l2.--Cockscomb llooking aalong long E ast K a i b a b monocline. monocline. East Kaibab 35 35 Shnabkaib Member ccan The S h n a b k a i b Member a n bbe e ttraced r a c e d ddirectly i r e c t l y iinto n t o tthe h e upper upper part of tthe Hupatki Member of of tthe Moenkopi FFormation Lees p a r t of he W u p a t k i Member h e Moenkopi o r m a t i o n aat t L e e s Ferry. Ferry. Smith ((1969, p. 111) Shnabkaib Hember iis Smith 1 9 6 9 , p« H I ) bbelieves e l i e v e s tthat h a t tthe he S h n a b k a i b Member s equivalent equivalent in age tto of tthe Thaynes Formation of tthe Salt i n a^e o tthe h e uupper p p e r ppart a r t of he T haynes F o r m a t i o n of he S a l t Lake Lake C i t y area. area. City were Paria No ffossils ossils w e r e ffound o u n d iin n tthe he P a r i a area. area. Upper Upper Red Member The Upper Upper Red Member of of tthe Moenkopi iis h e Moenkopi s rrecognized e c o g n i z e d wherever wherever t h e Shnabkaib Shnabkaib is i s present p r e s e n t and and tthis h i s includes includes m o s t of of ssouthvlest o u t h w e s t Utah Utah the most northern A rizona w e s t of of L e e s Ferry. Ferry. and northern Arizona west Lees The U p p e r Red Upper Red Member t h i c k e n s from from 99 feet f e e t in i n the the P a r i a area a r e a tto o 564 iin n ssouthwest o u t h w e s t Utah Utah thickens Paria ( G r e g o r y , 1950, 1 9 5 0 , p. p . 60). 60). (Gregory, In I n the t h e Paria P a r i a area a r e a the t h e Upper Upper Red Member is i s ggradational r a d a t i o n a i ~"ith with t h e Shnabkaib S h n a b k a i b Member and unconformably u n c o n f o r m a b l y underlies u n d e r l i e s the the S h i n a r u m p or or the Shinarump Monitor Butte B u t t e Members of of the t h e Chinle C h i n l e Formation. Formation. Monitor G e n e r a l l y tthe h e upper upper Generally p a r t of of the t h e member forms f o r m s a knobby k n o b b y cliff c l i f f and the t h e Imver l o w e r ppart a r t forms f o r m s aa part s t e e p slope. slope. steep Member i s composed composed of of two lithologic l i t h o l o g i c types. types. The Upper Red M ember is The lOvler l o w e r 70 to t o 80 feet f e e t of of the t h e formation f o r m a t i o n is i s very v e r y similar s i m i l a r to t o the the o t h e r red r e d members. members. other sandstone. some sandstone. T h i s is i s a ripple--marked, r i p p l e - m a r k e d , micaceous, m i c a c e o u s , silty s i l t y f>hale s h a l e with with This F l u t e casts c a s t s were w e r e ob o b served s e r v e d on some beds b e d s indicating indicating Flute s t r o n g current c u r r e n t action. action. strong m i n o r accessory, a c c e s s o r y , is i s both b o t h bedded bedded Gypsum, a minor f i l l s cross c r o s s cutting c u t t i n g veins v e i n s and decreases d e c r e a s e s upwards u p w a r d s in i n the t h e member. member. and fills t i p peer part p a r t of of the t h e Upper Red Member is i s a massive, m a s s i v e , poorly poorly The upp s o r t e d , silty, s i l t y m' micaceous, i c a c e o u s , fine-grained f i n e - g r a i n e d sandstone s a n d s t o n e (£ig. ( f i g , 9). 9), Sorted, T h i s deep deep This 36 3,6, red-brown n i t iis s much a r k e r tthan h a n tthe h e oother t h e r rred e d bbeds e d s iin n tthe h e Moenkopi red-brown uunit much ddarker Formation h i s iis s pprobably r o b a b l y due o llack a c k of ypsum. Formation and and tthis due tto of ggypsum. T h i s unit unit This forms i s t i n c t i v e kkey e y bbed e d tthat h a t iis s uuseful s e f u l iin n sseparating e p a r a t i n g the the forms aa ddistinctive Moenkopi he C hinle w h e r e tthe h e SShinarump h i n a r u m p iis s absent. absent. Moenkopi from from tthe Chinle where No ffossils o s s i l s hhave a v e bbeen e e n ffound o u n d iin n tthe h e Upper n the the Upper Red Red Member Member iin P a r i a aarea r e a bbut u t iin n tthe he L ittle C olorado R iver V a l l e y , small, small, Paria Little Colorado River Valley, uunidentifiable n i d e n t i f i a b l e bbivalves i v a l v e s hhave a v e bbeen e e n ffound o u n d iin n tthe h e llimesto i m e s t o nne e llenses e n s e s of of tthe he H o l b r o o k Member h i c h iis s tthe h e llateral a t e r a l eequivalent q u i v a l e n t of h e Upper Holbrook Member w which of tthe Upper Red Member R e p p e n i n g and t h e r s , 1969, 1969, P 9). Kember ((Reppening and oothers, P.. B B9). IIn n tthe h e same location, location, r e p t i l e and m p h i b i a n rremains e m a i n s hhave a v e aalso l s o bbeen e e n ffound. ound, reptile and aamphibian The aage g e of of the the Upper Red Member s Lower iddle T r i a s s i c and and uuntil n t i l paleontological paleontological Upper Hember iis Lower oorr M Middle Triassic e v i d e n c e is i s more ccomplete, o m p l e t e , the t h e exact e x a c t age a g e will w i l l remain r e m a i n iin n doubt. doubt. evidence Depositional D e p o s i t i o n a l Ertvironmertts Environments Rocks of of the t h e Hoenkopi Moenkopi Formation F o r m a t i o n of of the t h e Pa!:'ia P a r i a area a r e a are are transitional t r a n s i t i o n a l betwe'en b e t w e e n mostly m o s t l y marine m a r i n e rocks r o c k s to t o the t h e west w e s t and mostly mostly continental c o n t i n e n t a l rocks r o c k s to t o the t h e east e a s t and consequently c o n s e q u e n t l y were w e r e deposited d e p o s i t e d in i n aa v a r i e t y of of environments environments. variety a r e a was a shoreline s h o r e l i n e during d u r i n g much of of The area t h e Moenkopi deposition--all d e p o s i t i o n — a l l three t h r e e dominantly d o m i n a n t l y marine m a r i n e members, m e m b e r s , the the the Timpoweap, the t h e Virgin, V i r g i n , and the t h e Slmabkaib S h n a b k a i b pinch p i n c h out o u t or o r undergo u n d e r g o facies facies Timpo~-1eap, w i t h i n several s e v e r a l miles m i l e s of the t h e Paria P a r i a River. River. changes ~-lithin t h r e e red r e d members members are a r e dominantly d o m i n a n t l y tidal t i d a l flat f l a t deposits d e p o s i t s .. The three The LO\ver Lower Red Member Member \-1as was deposited d e p o s i t e d in i n aa transgressing t r a n s g r e s s i n g littoral l i t t o r a l envirenvir­ The onment. onment. The Virgin V i r g i n \vas was deposited d e p o s i t e d in i n aa shallo~'J s h a l l o w sea s e a in i n vlhich which deposition d e p o s i t i o n and and subsidence s u b s i d e n c e were w e r e very v e r y ss low l o w in i n the t h e Paria P a r i a area a r e a but b u t fairly fairly rapid p i d in i n ssouthern o u t h e r n Nevada. Nevada. r a The The Hiddle M i d d l e Red Red Nember Member was was deposi' d e p o s i t ed e d on on the the 37 dge of l u c t u a t i n g ssea e a iin n a ttidal i d a l fflat l a t eenvironment. nvironment. edge of a ffluctuating The Shnabkaib The Shnabkaib was marine-littoral ./as ddeposited e p o s i t e d iin n a sshallmv hallow m a r i n e - l i t t o r a l eenvironment n v i r o n m e n t dduring u r i n g aa time time of low eenergy. f vvery e r y low nergy. 0 The Upper Upper Red Red Member Member was vlas d deposited on tthe The e p o s i t e d on h e edge edge of a rregressing of tthe of e g r e s s i n g ssea; e a ; tthe h e kknobby n o b b y ssandstone a n d s t o n e aat t tthe h e ttop o p of h e member was ddeposited e p o s i t e d iin n a ffluvial l u v i a l complex. complex. S u b - C h i n l e Unconformity Unconformity Sub-Chinle T h r o u g h o u t tthe he C olorado P l a t e a u rregion egion a m a j o r unconformity unconformity Throughout Colorado Plateau major a t the t h e bbase a s e of he C hinle F ormation m a r k s a ggreat r e a t cchange h a n g e in in at of tthe Chinle Formation marks s e d i m e n t a t i o n , rrepresents e p r e s e n t s a ffair a i r pportion o r t i o n of e o l o g i c ttime, i m e , and sedimentation, of ggeologic r e f l e c t s pprofound r o f o u n d pphysiographic, h y s i o g r a p h i c , and e r h a p s cclimatic l i m a t i c changes. changes. reflects and pperhaps e x c e l l e n t rregional e g i o n a l ttreatment r e a t m e n t of of tthis h i s uunconformity n c o n f o r m i t y is i s ggiven i v e n in in An excellent Repenning and o t h e r s (1969, ( 1 9 6 9 , pp.. B13-BI5 B 1 3 - B 1 5). ). Repenning and others IIn n the the P a r i a area a r e a tthe h e unconformity u n c o n f o r m i t y is i s quite q u i t e obvious o b v i o u s where where Paria t h e white, w h i t e , massive, m a s s i v e , coarse, c o a r s e , sometimes s o m e t i m e s conglomeratic c o n g l o m e r a t i c Shinarump S h i n a r u m p has has the cut channels c h a n n e l s into i n t o the t h e red, r e d , fine-grained f i n e - g r a i n e d sands s a n d s and silts s i l t s of of the the cut ( f i g . 9). 9). Moenkopi (fig. C r e e k \vest w e s t of of the t h e movie m o v i e set, set, Along Road Creek c h a n n e l s at a t least l e a s t 50 and perhaps p e r h a p s over o v e r 80 feet f e e t deep d e e p are a r e cut c u t into i n t o the the channels Formation. Moenkopi Formation. l o c a t i o n (fig ( f i g .. 9) the t h e wall w a l l of of the t h e channel channel At one location i s so steep s t e e p that t h a t from from a distance d i s t a n c e if i f appears a p p e a r s to t o be b e a fault f a u l t .. is width The ,lidth of the t h e channel c h a n n e l cannot c a n n o t be determined d e t e r m i n e d due to t o a true t r u e fault f a u l t that t h a t cuts c u t s out out of t h e west w e s t edge e d g e of of the t h e channel. channel. the Where the t h e Shinarump S h i n a r u m p is i s absent a b s e n t the t h e unconformity u n c o n f o r m i t y is i s still still '.Jhere o b v i o u s although a l t h o u g h in i n places p l a c e s red r e d silts s i l t s of of the t h e Monitor M o n i t o r Butte B u t t e Hember Member obvious overlie o v e r l i e red r e d silts s i l t s of of the t h e Moe M o enkopi. nkopi. Gener<",lly G e n e r a l l y in i n the t h e above a b o v e case c a s e the the s a n d s t o n e is i s present p r e s e n t on top t o p of of the t h e Moenkopi and this t h i s bed bed knobby sandstone 38 38 nveniently m a r k s tthe h e uunconformity. nconformity. conveniently marks G enerally w h e r e tthe h e Shinarump Shinarump Generally where ig aabsent b s e n t a tthin h i n ddiscontinuous i s c o n t i n u o u s ssurface u r f a c e of n c o n s o l i d a t e d ppebbles e b b l e s and and is of uunconsolidated c o n c e n t r a t i o n s of e t r i f i e dd wood a r k tthe h e ssurface u r f a c e of h e unconformity. unconformity. concentrations of ppetrifie wood m mark of tthe C Chinle h i n l e Formation Formation The C hinle F o r m a t i o n ((Gregory, G r e g o r y , 11917, 9 1 7 , pp.. 443) 3 ) was or a Chinle Formation was named nroned ffor sequence of a r i g aatted ed m u d s t o n e s and a n d s t o n e s eexposed x p o s e d iin n tthe h e Chinle Chinle sequence of vvarig mudstones and ssandstones V a l l e y nnear ear C hinle, A rizona. Valley Chinle, Arizona. The ffo o rrnla m a tion t i o n ccan a n bbe e ttraced r a c e d directly directly along a ccontinuous o n t i n u o u s bband a n d of u t c r o p s from h e ttype y p e ssection e c t i o n iinto n t o the the along of ooutcrops f rom tthe P a r i a area. area. Paria Due tto o iits t s ggreat r e a t aareal r e a l eex x tent, tent, w i d e s p r e a d outcrops, o u t c r o p s , and and widespread uranium conten c o n t e n t, t , aa ggreat r e a t amount of literature l i t e r a t u r e is i s ddevoted e v o t e d to t o tthe h e Chinle Chinle uranium amount of Formation. Formation. C o n s e q u e n t l y much e r m i n o l o g y hhas a s bbeen e e n pproposed r o p o s e d ffor o r the the Consequently much tterminology v a r i o u s units. units. various T h i s ppaper a p e r follows f o l l o w s tthe h e ttermino e r m i n o llogy o g y pproposed r o p o s e d by Witkind This by Witkind and Thaden Thaden (1963), ( 1 9 6 3 ) , Ste,,,art S t e w a r t and o t h e r ss (1 ( 1 959), 9 5 9 ) , and and uused s e d by recent and and other by many many recent a u t h o r s in i n southeast s o u t h e a s t eern r n Utah U t a h and and northern n o r t h e r n Arizona. Arizona. authors In Paria I n the the P a r i a anrea r e a rrocks o c k s assigned a s s i g n e d to t o the t h e Chinle C h i n l e Formation Formation unconf o r m a b l y overli o v e r l i ee tthe h e Moenkopi Moenkopi Forma F o r m ation t i o n and unconform u n c o n f o r m aab b lly y underlie underlie unconformably the t h e Glen Cany,)n Canyon Group. Group. The Chinle C h i n l e forms f o r m s steep s t e e p ,, badland b a d l a n d slopes s l o p e s at a t the the f o o t of of the t h e Vermilion V e r m i l i o n Cl C l iff i f f ss and t hhe e Cockscomb. Cockscomb, foot t h e "squ " s q u aa~;r w skirts" skirts" At the ( t h e sloping s l o p i n g ,, banded b a n d e d sides s i d e s )) of of Gingham Skirt S k i r t Bu B utt te t e is i s perhap p e r h a p s the the (the i^est and most complete c o m p l e t e exposure e x p o s u r e of of the t h e Chinle C h i n l e Formation F o r m a t i o n in i n southHestern southwestern best ( f i . 10). 10). Utah (fig. g FOlt1." Four members of t hhe e Chinle C h i n l e Format F o r m a t ion i o n are a r e recogni r e c o g n i zzed e d and are are i n ascending a s c e n d i n g order o r d e r the t h e Shinarump S h i n a r u m p Hember, Member, Ho M onito n i t o r Butte B u t t e Henber, Member, in Petrifi.~d ? & t r : l f i e d Forest F o r e s t MCl'lber Member,, and O~d Owl Rock Hember Member.. 39 Shinarump Member - Conglomerate The Shinarump Shinarump C o n g l o m e r a t e ((Powell, P o w e l l , 1873, 1 8 7 3 , pp.. 458; 4 5 8 ; Gilbert, Gilbert, 1875 p* 176) was rreduced e d u c e d tto o a member of the t h e Chinle Chinle F o r m a t i o n by by 1875, p. 176) member of Formation Stewart (1957) (1957) and h e tterm e r m Shinarump S h i n a r u m p was also a l s o rrestricted e s t r i c t e d in i n parts parts Stewart and tthe of southeastern southeastern U t a h and t h e Moss Back Member ddefined. efined. of Utah and the Back Hember Rocks a s s i g n e d tto o tthe h e Shinarump S h i n a r u m p Member iin n tthe he P a r i a area a r e a ccan a n bbe e traced traced assigned Paria d i r e c t l y into i n t o tthe h e ttype y p e section s e c t i o n at a t tthe h e Shinarump S h i n a r u m p Cliff C l i f f ss a few miles directly fe'\v miles t h e southwest. southwest. to the Early were E a r l y geologists g e o l o g i s t s and explorers explorers w e r e immediately i m m e d i a t e l y aattracted t t r a c t e d to to t h i s peculiar peculiar w h i t e and and yyellow e l l o w sandstone s a n d s t o n e and c o n g l o m e r a t e that that this white and conglomerate c o n t a i n e d so many different different m i n e r a l s and and bbedding e d d i n g structures, s t r u c t u r e s , and and contained minerals p r o t r u d e d obviously o b v i o u s l y bbetween e t w e e n tthick h i c k eexposures x p o s u r e s of e d rrock. ock. protruded of rred Gregory Gregory 4 - 6 5 ) gives g i v e s a good e g i o n a l description d e s c r i p t i o n of h e Shb.arump Shinarump (1950, pp.. 664-65) good rregional of tthe r i e f aaccount c c o u n t of early w o r k e r s oopinions p i n i o n s as a s tto o origin. origin. and a bbrief of early vlOrkers Throughout Utah and nnorthern Arizona T h r o u g h o u t southern southern U t a h and orthern A r i z o n a tthe h e Shinarump Shinarump is and except i s amazingly a m a z i n g l y ppersistent e r s i s t e n t and e x c e p t for f o r sscattered c a t t e r e d llocal o c a l areas a r e a s of of non-deposition n o n - d e p o s i t i o n ((or, o r , less l e s s likely, l i k e l y , erosion e r o s i o n pprior r i o r tto o ooverlying v e r l y i n g Honitor Monitor Butte member of of tthe Chinle B u t t e deposition) d e p o s i t i o n ) is i s tthe h e bbasal a s a l member he C h i n l e Fonnation. Formation. In In the Paria NW the southern s o u t h e r n tthree h r e e qquarters u a r t e r s of of tthe he P aria N W qquo.drangie u a d r a n g l e a local l o c a l area area of of nondeposition n o n d e p o s i t i o n is i s seen s e e n .. Shinarump The S h i n a r u m p is i s ppresent r e s e n t only o n l y iin n tthe h e area area of the t h e movie s e t and P a r i a cemetery c e m e t e r y and n discontinuous d i s c o n t i n u o u s ooutcrops u t c r o p s in in of movie set and Paria and iin t h e extreme e x t r e m e nnorthHest o r t h w e s t corner c o r n e r of of tthe h e map area. area. the from 0 to t o 30 80 fe f e ee tt thick t h i c k in i n less l e s s tthan han a m ile, from mile. The Shinarump S h i n a r u m p ranges ranges The Shinarump S h i n a r u m p iis s aa TIle w h i t e to to b uff, m e d i u m - tto o ccoarse-grai o a r s e - g r a i nned e d ,, locally locally w e l l - s o r t e d sandstone sandstone buff, mediumwell-sorted White with sub-round s u b - r o u n d to t o sub-angular s u b - a n g u l a r vvitre-ouG i t r e o u s and f r o s t e d qquartz u a r t z grains. grains. with and frosted is m o s t l y ccalcite a l c i t e and and tthe h e semel s a n d is i s someHnat somewhat ffriable. riable. Cement is mostly A ffine i n e silt silt 40 t r i x coats coats m o s t of of tthe h e ggrains~ rains. aatrix most About e r c e n t of of tthe h e grains g r a i n s are are About 2 ppercent dark colored c o l o r e d chert c h e r t and r t z i t i c ggrains. rains. dark and qquuaartzitic S a m p l e s analyzed a n a l y z e d by Samples Stewart and others o t h e r s ((1959, 1 9 5 9 , pp.. 544) he P a r i a area a r e a show tthat h a t the the Stewart 544) from from tthe Paria Shinarump contains c o n t a i n s 70 ppercent e r c e n t qquartz, u a r t z , 14 ppercent e r c e n t ffeldspar, e l d s p a r , 1 percent percent Shinarump mica, and and 15 ppercent material. e r c e n t ttuffaceous uffaceous m aterial. w i l l be discussed d i s c u s s e d later. later. and will The latter l a t t e r is i s Significant significant The Shinarump S h i n a r u m p of he P a r i a aarea r e a is is of tthe Paria c l a s s i f i e d by S t e w a r t and and others o t h e r s (1959, ( 1 9 5 9 , pp.. 544) 544) as a s a ttuffaceous u f f a c e o u s feldfeldclassified Stewart s p a t h i c orthoquartzite. orthoquartzite. spathic S u b o r d i n a t e tto o tthe h e sandstone s a n d s t o n e aare r e bbeds e d s of of gray-green g r a y - g r e e n lenticular lenticular Subordinate ^rit. grit. g r a i n s range r a n g e up to t o one q u a r t e r iinch n c h in i n diameter. diameter. The grains one quarter Quartz Quartz g r a i n s are a r e smokey smokey and and many aare r e bbroken; roken; w h o l e ggrains r a i n s are a r e angular a n g u l a r to to grains whole rounded. rounded. The m a t r i x is i s a fine f i n e green g r e e n quartz q u a r t z ssand a n d tthat h a t ccomposes o m p o s e s 50 50 matrix p e r c e n t of of tthe h e uunit. nit. percent S c a t t e r e d l eenses n s e s of of brown c o n g lome l o m erate r a t e are are Scattered brmm cong d i s t r i b u t e d tthroughout h r o u g h o u t tthe h e Shinarump. Shinarump, distributed the Shinarump Where the. S h i n a r u m p is i s about a b o u t 40 feet f e e t tthick h i c k it i t forms f o r m s sheer, sheer, o v e r h a n g i n g cliffs c l i f f s (fig. ( f i g . 9) bbut ut w h e r e it i t is i s tthinner h i n n e r it i t forms forms overhanging where r e s i s t a n t rrauuded o u n d e d bbuttes u t t e s and ledges l e d g e s. resistant Honi Butte The uupper p p e r contact c o n t a c t with w i t h tthe he M o n itor tor B u t t e is i s ggradational r a d a t i o n a l and locally l o c a l l y is i s pp:rroobahly b a b l y int i n t eer r ttongu o n g u eed d .. Ev E v idence i d e n c e of of intertonguing i n t e r t o n g u i n g is is found in i n tth h ee nnorthlvest o r t h w e s t corner c o r n e r of h e map w h e r e Shinarump-type S h i n a r u m p - t y p e deposits deposits fcund of tthe \-lherc a r e repeated r e p e a t e d iin n tthe he M o n i t o r Bu B utte t t e (fig ( f i g .. 11). 11). arc Monitor The bbasal, a s a l , discontinuous discontinuous Shinarump Shinarump ggrades r a d e s uup~.;rards p w a r d s into i n t o bbentonitic e n t o n i t i c sandstone sandstone and m mudstone and udstone the \vhich the. Monitor M o n i t o r Butte Butte w h i c h aare r e aabout b o u t 80 tto o 100 feet f e e t thick. thick. of of These T h e s e are are Overlain by a coarse, o v e r l a i n by c o a r s e , chert-pebble c h e r t - p e b b l e cconglomerat o n g l o m e r a t ee and and sandstone s a n d s t o n e about about 20 to t o 30 30 ffe_et e e t tthO h,1.C i c kk,• T h i s ccong o n g lomer l o m e r a te t e is i s tthe h e coarsest c o a r s e s t conglc'merate conglomerate This 441 1 found in i n tthe he C h i n l e Formation F o r m a t i o n of of the the P a r i a area. area. found Chinle Paria C h e r t and Chert q u a r t z i t e ppebbles e b b l e s up tto o 1-1/2 1 - 1 / 2 iinches n c h e s iin n diameter d i a m e t e r are a r e scattered s c a t t e r e d in in a quartzite oarse, m o t t l e dd,, yyellow, e l l o w , ,,,hit w h i t e ,, and i n k ssandstone. andstone. coarse, mottle and ppink A n o t h e r 50 to to Another f e e t of of M onitor B u t t e tthen h e n conformably c o n f o r m a b l y ooverlies v e r l i e s tthe h e conglomerate. conglomerate. 100 feet Monitor Butte Large L a r g e ccarbonized a r b o n i z e d and ppetrified e t r i f i e d logs l o g s are a r e found f o u n d in i n the the c o n g l o m e r a t e along a l o n g ,vith w i t h hhe e aavy v y cconcentrations o n c e n t r a t i o n s of of jjarosite. arosite. conglomerate Many fragments of a r b o n and and jjarosite-impregnated a r o s i t e - i m p r e g n a t e d cconglomerate onglomerate w e r e tested tested fragments of ccarbon were for uranium u r a n i u m bbet u t no evidence e v i d e n c e of of rradioactive adioactive m a t e r i a l was ffound. ound. for material This This upper conglomerate c o n g l o m e r a t e iis s shown as a s a kkey e y bbed e d on tthe h e ggeologic e o l o g i c map. map. upper Sedimentary complex iin S e d i m e n t a r y structures s t r u c t u r e s aare r e qquite u i t e complex n tthe h e Shinarump. Shinarump. Lenticular L e n t i c u l a r bbedding e d d i n g iis s everywhe e v e r y w h e re r e ppresent r e s e n t although a l t h o u g h some of of tthe h e graygraygreen green conglomerates c o n g l o m e r a t e s are a r e ppee rsistent. rsistent. The uunit n i t is i s highly h i g h l y cross cross s t r a t i f i e d "lith w i t h tthe h e dominant d o m i n a n t ddips i p s tto o tthe h e nnorthwest. orthwest. stratified channeling w i t h i n tthe h e member a r e common. channeling within member are D i n s t e r n s and Diastems B e d d i n g iis s several s e v e r a l inches inches Bedding t h i c k at a t the t h e bbase a s e bbut u t becomes becomes m ore m a s s i v e ttowards o w a r d s tthe h e ttop. op. thick more massive The The l a r g e channels c h a n n e l s cut c u t in i n tthe h e Moenkopi Moenkopi ccontain o n t a i n ripped r i p p e d up ffragments r a g m e n t s of large the Hoenkopi, Moenkopi, bblue-green lue-green m u d s t o n e s , and c o n g l o m e r a t i c beds. beds. the mudstones, and a few few conglomeratic amount of of conglomerate c o n g l o m e r a t e and tthe h e size s i z e of of tthe h e pebbles p e b b l e s increases increases The amount i n tthe h e Shinarump S h i n a r u m p Member Member.• . upwards in o n l y fossil f o s s i l fr from he P a r i a aarea r e a is i s ppetrified e t r i f i e d wood, AraucariAraucariThe only om tthe Faria a r i z o n i c u m (Greg ( G r e g ory, o r y , 1950, 1 9 5 0 , pp.. 66; 66; D a u g h e r t y , 1941, 1 9 4 1 , pp.. 8). 8). o]tylon arizoniC".um Daugherty, ^~IOrtitor ^ ^ L ^ t Butte t ^ ^ i eNem B k ber ^I The Monitor Butte Thaden, Monitor B u t t e Member (n~itkind W i t k i n d and T h a d e n , 1963) 1963) is is recognized with Paria recognized w i t h some rres e s ee rrvations v a t i o n s iin n tthe he P a r i a aarea. rea. Generally G e n e r a l l y only only the Petrifie Forest Memb e rs are t h e Shinarump Shinarump and P e t r i f i e dd F o r e s t Members a r e recognized r e c o g n i z e d iin n southsouth- 120 100 80 MONITOR . 1-' :: :. 60 .....,._ ... "("' ~. 40 .. o '. . ,"",-. 1. ---:..:.... ~-~.::-.. - ." -- - ' ~-"r---. : '" r-- --=-_'y- __. . •. -..::..::::.:: <:",,",?: . BUTTE _# . -~"."" ~__!.._! '~ ,,""j' ••~~;-- _ . ... ~-:n-:3::::r~------ - . -c---- --I .. .,.,.•=.". .... .•.••. ..... •...,.; . ....~ ... : ~ ~~.~.. ; .~:; .... ~: - . ," .:~:;~~"" '" . ~ .. ',' . - :- . - .:. .~. :. :- .. .. ...: ~ .~ •• :i.: :.• ' ..~ ... :.• SHINAI!UMP _r.,,;.;,.... - ~.~,. r-...,.... ~ -. . -." .. .. .: - '." " ' ~ mee F i g u r e 11. 1 1 . -..SSketc k e t c hh shovi s h o w i ng n g re r e llatio a t i o nns s hhip i p of of ""do d o t.1 u ble" b l e " Shina S h i n a rruump m p iin n extre extrem Figure .. n o r t h w\lcst e s t co c o rner rner north toitguing b e t w e eenn tongu ing betwe o f ini:<"1.· of map ar a r ee a .. T s p robi"b r o b a b lly y eevidf~ v i d e n!1c c ee of inter' h i s iis of ers . Butt tthe h e Honi M o n itt or or B u t t ee aand n d Shimt S h i n a rruump m p Memb Members. 43 _ U tah. western Utah. e s < e r n At e e s FFerry, erry, P h o e n i x ((1963) 1 9 6 3 ) uuses s e s aan n iinformal n f o r m a l tern, tern, At L Lees Phoenix ""the t h e ssandstone a n d s t o n e and u d s t o n e uunit", n i t " , ffor o r rrocks o c k s aapproximately p p r o x i m a t e l y equivalent equivalent and m mudstone to he M onitor B utte. to tthe Monitor Butte. R e p e n n i n g and t h e r s ((1969, 1 9 6 9 , pp.. B18) t a t e that that Repenning and oothers B18) sstate t h i s uunit n i t iis s aabsent b s e n t aat t P a r i a ddue u e tto o iintertonguing ntertonguing w i t h tthe h e Petrified Petrified this Paria with F o r e s t Member. Forest However, n i t aabout b o u t 185 e e t tthick hick w i t h lithologic, lithologic, Hmvever, a uunit 185 ffeet with s t r a t i g r a p h i c , and o l o r ssimilarities i m i l a r i t i e s tto o tthe h e ttype ype M onitor B u t t e near near stratigraphic, and ccolor Monitor Butte a l l e y iis s eexposed x p o s e d aatt P aria. Monument V Valley Paria. S t e w a r t and t h e r s ((1959, 1 9 5 9 , p. p. Stewart and oothers e f e r s tto o tthis h i s uunit n i t aas s M onitor B u t t e and n aaddition, d d i t i o n , Davidson Davidson 546) rrefers Honitor Butte and iin (1967) rrecognises Monitor Butte Circle Cliffs which ecognises M onitor B u t t e iin n tthe he C ircle C l i f f s aarea, rea, w h i c h is is t h e closest closest C h i n l e ooutcrop u t c r o p tto o tthe h e nnortheast o r t h e a s t of Paria. the Chinle of Paria. r i t e r i a can c a n bbe e uused s e d iin n tthe he P a r i a aarea r e a aas s elsewhere elsewhere The same ccriteria Paria i n the t h e pplateaus l a t e a u s to t o separate s e p a r a t e tthe he M onitor B u t t e from h e Petrified Petrified in Monitor Butte from tthe F o r e s t (Stewart ( S t e x r a r t and t h e r s , 1959). 1959), Forest and oothers, M i c a , uusually s u a l l y rrere a r e iin n tthe h e Chinle, Chinle, Mica, i s abundant a b u n d a n t in i n the the M onitor B u t t e ; the t h e colors c o l o r s of he M o n i t o r Butte Butte is Monitor Butte; of tthe Monitor a r e gray, g r a y , green, g r e e n , pale p a l e ppinkish inkish w h i t e , and and grayish g r a y i s h bblue l u e iin n contrast contrast are white, t o the t h e vvivid i v i d red) r e d , ppink, i n k , ddeep e e p bblue l u e ,, purple p u r p l e and white xvhite exposed e x p o s e d in i n the the to o v e r l y i n g Petrified P e t r i f i e d Forest F o r e s t Member (fig ( f i g .. 10); 1 0 ) ; interbedded i n t e r b e d d e d sandstones sandstones overlying a r e the t h e main m a i n distinguishing d i s t i n g u i s h i n g feature f e a t u r e of of the t h e Monitor" M o n i t o r Butte B u t t e and they they are a r e usually u s u a l l y lenticular, l e n t i c u l a r , highly h i g h l y cro c r o sssbedded s b e d d e d ,) and sometimes s o m e t i m e s conglomeratic. conglomeratic are In I n the t h e northern n o r t h e r n ha h a llf f of of the t h e mapped area a r e a the t h e badland-forming bad-land-forming Monitor weell comb and is Monitor Butte B u t t e is is w l l ey' e x posed p o s e d at a t the t h e foot f o o t of of the t h e Cocks Cockscomb is approximately a p p r o x i m a t e l y 185 feet f e e t thick. thick. II t t is i s a bentonitic, b e n t o n i t i c , banded, b a n d e d , grayishgrayish- green, g r e e n , gray, g r a y , white, w h i t e , and bluish b l u i s h structureless s t r u c t u r e l e s s mudstone m u d s t o n e with w i t h gray g r a y to to White, w h i t e , interheded i n t e r b e d e d ,) cros c r o s s -lcmlinated, - l a m i n a t e d , l eenticularn t i c u l a r sandstone s a n d s t o n e and mudmudpebble p e b b l e conglomerate. conglomerate. The Monit M o n i t er o r Butte B u t t e has h a s many minor m i n o r or o r local local 44 44 l i t h o l o g i e s also. also. lithologies N e a r or o r at a t the t h e base b a s e is i s commonly commonly a rred, e d , ~icaceous micaceous Near s i l t s t o n e tthat h a t is i s probably p r o b a b l y derived d e r i v e d from from the t h e Hoenkopi Moenkopi Fonaation. Formation. siltstone Associated w i t h this t h i s unit, u n i t , especially e s p e c i a l l y where w h e r e the the S h i n a r u m p is i s present, present, Associated with Shinarump i t a ppale-red a l e - r e d to t o bbuff u f f quartz q u a r t z sandstone sandstone w i t h 5 ppercent ercent w h i t e mica, mica, it \.;rith white p e r c e n t chert c h e r t and and rock r o c k fragments f r a g m e n t s and a large l a r g e ppercentage e r c e n t a g e of of fine, fine, 15 percent s i l t y matrix. matrix. silty average m i n e r a l composition c o m p o s i t i o n of of tthe h e 110nitor M o n i t o r Butte Butte The average mineral i n the the P a r i a area a r e a is i s quartz q u a r t z 56 percent, p e r c e n t , feldspar f e l d s p a r 21 ppercent, ercent, m ica 3 in Paria mica p e r c e n t , and tuffaceous tuffaceous m a t e r i a l 20 percent p e r c e n t (Stewart ( S t e w a r t and t h e r s , 1959, 1959, percent, material and oothers, p . 546). 546). p. l a t t e r is i s quite q u i t e significant s i g n i f i c a n t and will w i l l bbe e discussed discussed The latter later. later. Sedimentary Hember include S e d i m e n t a r y structures s t r u c t u r e s of of the t h e Monitor M o n i t o r Butte B u t t e Member include lenticular l e n t i c u l a r bedding, b e d d i n g , low-angle l o w - a n g l e cross c r o s s laminations, l a m i n a t i o n s , and and intraformational intraformational and mud-pebble m u d - p e b b l e conglomerates c o n g l o m e r a t e s or o r rip-ups. rip-ups. The mudstone m u d s t o n e iis s structureless structureless and shows massive m a s s i v e post p o s t depositional-prelithification d e p o s i t i o n a l - p r e l i t h i f i c a t i o n sslumpages. lumpages. The membe:::member weathers w e a t h e r s into i n t o bbadlands a d l a n d s covered c o v e r e d with w i t h a frothy, f r o t h y , "popcorn" "popcorn" surface. surface. The resistant r e s i s t a n t sandstones s a n d s t o n e s form form ledges l e d g e s and and low low cliffs. cliffs. In Valley I n the t h e south s o u t h ppart a r t of of the t h e map area a r e a in i n Fivemile Fivemile V a l l e y the the Chinle C h i n l e "is i s poorly p o o r l y exposed e x p o s e d and is i s not n o t divided d i v i d e d on the t h e map oorr cross cross sections s e c t i o n s (pl. ( p i . 2). 2). Petrified P e t r i f i e d Forest F o r e s t Member The Petrified P e t r i f i e d Forest F o r e s t Member was named by by Gregory G r e g o r y ((1950, 1 9 5 0 , pp.. 667) 7) for f o r rocks r o c k s he h e describes d e s c r i b e s as as . . aa m a r v e l o u s assemblage a s s e m b l a g e of of shales, s h a l e s , soft s o f t sandstones, sandstones, " .••• marvelous weathered of calcareous w e a t h e r e d volcanic v o l c a n i c ashes, a s h e s , and and many kkinds i n d s of calcareous r o c k s colored c o l o r e d with w i t h bbands, a n d s , streak s t r e a k s, s , and iirregular r r e g u l a r blotches blotches rocks of yellow, y e l l o w , lavender, l a v e n d e r , ppurple, u r p l e , pink, p i n k , li.lac, l i l a c , aash s h ggray, r a y , and and of v a r i o u s shades s h a d e s of of red, r e d , blue. b l u e ,1 and brown. brown. T h e s e aarc r e the the various These 4S 45 most m o s t rrichly i c h l y colored c o l o r e d beds b e d s in i n Utah." Utah." s t a t e m e n t made in i n a land l a n d of of vivid v i v i d rocks r o c k s attests a t t e s t s to t o the the Such a statement s t r i k i n g color c o l o r of of tthe h e Petrified P e t r i f i e d Forest F o r e s t Member. striking s o , bbecause e c a u s e of Even so, i t s weak nature n a t u r e very v e r y few outcrops o u t c r o p s in i n the t h e Colorado C o l o r a d o Plateau P l a t e a u expose expose its e n t i r e member. the entire of the t h e finest f i n e s t exposures e x p o s u r e s occurs o c c u r s where w h e r e the the One of Paria R i v e r cuts c u t s through t h r o u g h the t h e Cockscomb at a t tthe h e tmvn town of of Paria, Paria, Paria River c o m p l e t e l y exposing e x p o s i n g the t h e entire e n t i r e Petrified P e t r i f i e d Forest F o r e s t Member (fig. ( f i g . 10). 10). completely S k i r t Butte, B u t t e , colorful c o l o r f u l banded b a n d e d "squaw " s q u a w skirts" s k i r t s " are a r e capped capped At Gingham Skirt t h e Glen Glen Canyoll Canyon Group. Group. by the Petrified F o r e s t forms f o r m s gullied gullied The Petrified Forest b a d l a n d s along a l o n g tthe h e Cockscomb Cockscomb and at a t tthe h e bbase a s e of of the t h e Vermilion V e r m i l i o n Cliffs. Cliffs. badlands S k i r t Butte B u t t e the t h e unit u n i t is i s approximately a p p r o x i m a t e l y 482 feet f e e t thick. thick. At Gingham Skirt a s e of of the t h e Petrified P e t r i f i e d Forest F o r e s t Member is i s pplaced l a c e d at a t the t h e ttop o p of of the the The bbase uppermost conglomeratic c o n g l o m e r a t i c sandstone s a n d s t o n e of of the the M o n i t o r Butte B u t t e Member which which uppermost Monitor a l s o coincides c o i n c i d e s TlIlith w i t h a change c h a n g e in i n color c o l o r from from greenish g r e e n i s h gray g r a y to t o the the also v i v i d colors c o l o r s described d e s c r i b e d above. above. vivid t o p is i s placed p l a c e d '.,here w h e r e bentonite bentonite The top i s either either m i n o r or o r absent a b s e n t as a s shown by the t h e lack l a c k of of a I!popcorn" "popcorn" is minor surface. surface. The Petrified P e t r i f i e d Forest F o r e s t Member is i s a complex, c o m p l e x , bentonitic, bentonitic, sandy mudstone m u d s t o n e and and siltstone. siltstone. The colorful, c o l o r f u l , horizontal h o r i z o n t a l bands b a n d s are are from from less l e s s than t h a n an a n inch i n c h to t o over o v e r 20 feet f e e t in i n thickness. thickness. Some are a r e very very p e r s i s t e n t over o v e r several s e v e r a l miles-m i l e s — others o t h e r s grade g r a d e llaterally a t e r a l l y into i n t o other other persistent c o l o r s , some aappea~: p p e a r tto o ppinch i n c h out, o u t , others o t h e r s are are m e r e l y streaks s t r e a k s or or colo:rs, merely i r r e g u l a r blotches. blotches. irregular T h e r e is i s no s atisfactory a t i s f a c t o r y explanation e x p l a n a t i o n for f o r this this There pbenomonon although a l t h o u g h bbentonitic e n t o n i t i c units u n i t s are a r e notorioLls n o t o r i o u s for f o r color color phenomonon banding. banding. Both the t h e 1Vinsor W i n s o r HembE:r Member of of the t h e Carmel C a r m e l Formation F o r m a t i o n and and the the Both 46 T r o p i c Shale S h a l e hhave a v e bbentonitic e n t o n i t i c color c o l o r bbaa nnding. ding. Tropic P h o e n i x (1963, ( 1 9 6 3 , pp.. 22) 22) Phoenix a p e s t s that t h a t tthese h e s e and o t h e r changes c h a n g e s in i n tthe he P etrified F o r e s t Member Suggests and other Petrified Forest SUg& are the results of subtle chemical changes in an othen-lise stable a r e t h e r e s u l t s of s u b t l e c h e m i c a l c h a n g e s i n an o t h e r w i s e stable and uniform depositional environment. and u n i f o r m d e p o s i t i o n a l environment. Several minor and peculiar lithologies are locally present S e v e r a l m i n o r and p e c u l i a r lithologies are locally in parts of the Pe trified Forest Hember. Minor lenses of i n p a r t s of t h e P e t r i f i e d Minor l e n s e s F o r e s t Member. present of conglomeratic sandstone and mud-pebble conglomera te are present and c o n g l o m e r a t i c s a n d s t o n e and m u d - p e b b l e c o n g l o m e r a t e a r e p r e s e n t and a resistant, ledge-forming silicified mudstone (once limestone ?) a r e s i s t a n t , l e d g e - f o r r a i n g s i l i c i f i e d m u d s t o n e ( o n c e l i m e s t o n e ?) about 6 feet thick forms a marker bed on the north s ide of Gingham about 6 f e e t t h i c k f o r m s a m a r k e r b e d on t h e n o r t h s i d e of Gingham Skirt Butte. Several other thin and discontinuous silicified beds Skirt Butte. S e v e r a l o t h e r t h i n and d i s c o n t i n u o u s s i l i c i f i e d beds are also scattered ne ar the top of th e member. a r e a l s o s c a t t e r e d n e a r t h e t o p of t h e member. Due to the swelling caused by the bentonite, sedimentary Due t o t h e s w e l l i n g c a u s e d by t h e b e n t o n i t e , s e d i m e n t a r y ::::tructure"s nrc poorly exposed. Most of the I!lUds to11e i s ~assive structures are poorly exposed. Most of t h e m u d s t o n e i s m a s s i v e but the scattered coarser units are cross l aminated and thin bedded. but t h e s c a t t e r e d c o a r s e r u n i t s a r e c r o s s l a m i n a t e d and t h i n bedded. Many minor local unconfo rmities are seen on freshly "leathered Many m i n o r l o c a l u n c o n f o r m i t i e s a r e s e e n on f r e s h l y weathered surfaces. Slumping and f olding that occured just after deposition surfaces. Slumping and f o l d i n g t h a t occured j u s t after deposition as well as slumping and folding assoc iated >"ith later structural as w e l l a s s l u m p i n g and f o l d i n g associated with l a t e r structural deformation are characte ristic of the member. deformation are c h a r a c t e r i s t i c ° A pt?cul1<n o (,,, occu ~~nce of t h e member. of petrified wood is seen near the base A p e c u l i a r o c c u r e n c e of p e t r i f i e d wood i s s e e n n e a r t h e base of the n:ember to the wes t of the movie set on th e south fla nk of of t h e member t o t h e w e s t of t h e m o v i e s e t on t h e s o u t h f l a n k of Calico Butt e . A brillia ntly colored bed of pe t r ified wood several Calico B u t t e . A brilliantly c o l o r e d bed of p e t r i f i e d wood several inches thick ar.d sevex-al square feEt in area is interhedd ed \-lith i n c h e s t h i c k and s e v e r a l s q u a r e f e e t i n a r e a i s i n t e r b e d d e d mudstone. mudstone. with Presumab l y this v;ras an acculllu lation of wood chips, bark, P r e s u m a b l y t h i s was a n a c c u m u l a t i o n of wood c h i p s , bark, and small twigs that f orn-led in a swamp or qui et part of a stream or and s m a l l t w i g s t h a t formed i n a swamp o r q u i e t p a r t of a s t r e a m lake and l ate r ,..ras petrified. i a k e and L a t e r was petrified. or 47 In Arizona I n northern northern A r i z o n a the t h e bbentonite e n t o n i t e contains c o n t a i n s the t h e remains r e m a i n s of of aaphibians, a m p h i b i a n s , reptiles, r e p t i l e s , pphytosaurs, h y t o s a u r s , and lung l u n g fish f i s h (Camp, 1930). 1930). Fresh Fresh water pelecypods p e l e c y p o d s have h a v e also a l s o been b e e n found f o u n d at a t vvarious a r i o u s locations l o c a t i o n s throughout throughout water the the plateau p l a t e a u country--especially c o u n t r y — e s p e c i a l l y in i n l:Llly l i m y beds. beds. jwl Member owl Rock Meniber The Owl Rock Member (Witkind ( W i t k i n d and and Thaden, T h a d e n , 1963, 1 9 6 3 , p. p . 22, 2 2 , 30) 30) indicates i n d i c a t e s a change c h a n g e in i n Chinle C h i n l e Deposition. Deposition. Stewart S t e w a r t (1969) ( 1 9 6 9 ) recognizes recognizes t h r e e pphases h a s e s of of Late L a t e Triassic T r i a s s i c deposition. deposition. three The first f i r s t is i s a sequence sequence of of bentonitic b e n t o n i t i c sandstone s a n d s t o n e and conglomeratic c o n g l o m e r a t i c sandstone sandstone (Shinarump, (Shinarump, Monitor Monitor Butte, B u t t e , Petrified P e t r i f i e d Forest F o r e s t of of Paria P a r i a area) a r e a ) deposited d e p o s i t e d in i n a fluvialfluviall a c u s t r i n e complex. complex. lacustrine s e c o n d phase p h a s e is i s a sequence s e q u e n c e of of non-bentonitic non-bentonitic The second s i l t s t o n e , freshwater f r e s h w a t e r limestone, l i m e s t o n e , and and fine f i n e sandstone s a n d s t o n e (Owl Rock of of siltstone, P a r i a area). area). Paria F i n a l l y a great g r e a t eolian e o l i a n sequence s e q u e n c e is i s rrepresented e p r e s e n t e d bby y the the Finally Sandstone. Wingate Sandstone. T h e r e f o r e a main m a i n characteristic c h a r a c t e r i s t i c of of the t h e Owl Rock Rock Therefore i s a lack l a c k (or ( o r very v e r y minor m i n o r amount) a m o u n t ) of of bbentonite. entonite. is F o r this t h i s reason r e a s o n plus plus For the fact f a c t tthat h a t the t h e member member is i s recognized r e c o g n i z e d in i n the t h e Lees L e e s Ferry F e r r y area area the ( P h o e n i x , 1963), 1 9 6 3 ) , Circle C i r c l e Cliffs C l i f f s area a r e a (Davidson, ( D a v i d s o n , 1967), 1 9 6 7 ) , and House Rock Rock (Phoenix, Valley area a r e a (Wells, ( W e l l s , 1960), 1 9 6 0 ) , the t h e Owl Rock Member is i s recognized r e c o g n i z e d in i n the the Valley P a r i a area a r e a in i n this t h i s report. report. Paria Although A l t h o u g h not n o t typically t y p i c a l l y developed d e v e l o p e d at a t Paria P a r i a as a s it i t is i s at at Monument Valley V a l l e y and other o t h e r areas a r e a s in i n southeastern s o u t h e a s t e r n Utah, U t a h , the t h e lack l a c k of betonite h e t o n l t e is i s readily r e a d i l y seen s e e n where w h e r e tthe h e member member is i s exposed. exposed. Its I t s lmver lower Contact c o n t a c t is i s highly h i g h l y transitional t r a n s i t i o n a l and may occur o c c u r through t h r o u g h a zone z o n e of of 50 feet f e e t or or more. more. A Gingham Gingham Skirt S k i r t Butte B u t t e the t h e unit u n i t is i s about a b o u t 100 feet f e e t but but this t h i s thickness· t h i c k n e s s 1S i s ar a r b· b. 1trary. itrary. The member is i s generally g e n e r a l l y covered c o v e r e d with with 48 em the Glen l u s from t h e overlying overlying G l e n Canyon Canyon Group and and in i n most m o s t places p l a c e s is i s quite quite ta1US fr s s i b l e so tthe h e sstudy t u d y of t was imited. inaccessible of iit was llimited. s o The Owl Owl Rock Rock Member Member The \ forms seep, s tt e e p , talus t a l u s covered c o v e r e d slopes s l o p e s in i n contrast c o n t r a s t to t o the t h e rrounded o u n d e d badland badland forms s l o p e s of of the t h e underlying u n d e r l y i n g Chinle C h i n l e (fig. ( f i g . 10). 10). slopes The Owl Rock is i s partially p a r t i a l l y exposed e x p o s e d under u n d e r the t h e protecting p r o t e c t i n g cliff cliff of of the t h e overlying o v e r l y i n g Wingate W i n g a t e Sandstone S a n d s t o n e and and could c o u l d bbe e reasonably r e a s o n a b l y ,,,,ell well studied s t u d i e d at a t several s e v e r a l localities. localities. The member is i s a reddish-grayishreddish-grayish- orange, o r a n g e , mottled m o t t l e d mudstone m u d s t o n e and sandy s a n d y siltstone s i l t s t o n e in i n thin t h i n horizontal horizontal layers. layers. The mudstone m u d s t o n e weathers w e a t h e r s into i n t o shiny, s h i n y , deep-red d e e p - r e d chips. chips. No limestone l i m e s t o n e typical t y p i c a l of of the t h e Owl Rock in i n other o t h e r areas a r e a s was exposed, e x p o s e d , but but this t h i s can can perhaps p e r h a p s be b e attributed a t t r i b u t e d to t o tthe h e limited l i m i t e d exposures. exposures. Only Only horizontal h o r i z o n t a l stratification s t r a t i f i c a t i o n was seen s e e n although a l t h o u g h this t h i s is i s typical. typical. No fossils were found f o s s i l s were f o u n d iin n tthe h e Paria P a r i a area. area. Depositional Environments Depositidnal~rtvirortmertts The depositional d e p o s i t i o n a l history h i s t o r y of of the t h e Chinle C h i n l e Formation F o r m a t i o n is i s not n o t as as clear c l e a r and consistent c o n s i s t e n t as a s that t h a t of of the t h e Moenkopi. Moenkopi. M uch of Much of the t h e parent parent rock rock of of the t h e Chinle C h i n l e is i s ppre-existing r e - e x i s t i n g sedimentary s e d i m e n t a r y rock r o c k bbut u t volcanics vclcanics play Monitor play an important i m p o r t a n t role r o l e in i n tthe he M o n i t o r Butte B u t t e and Petrified P e t r i f i e d Forest Forest (and in i n the t h e Paria P a r i a area a r e a tthe h e Shinarump). Shinarump). The Shinarump S h i n a r u m p is i s the t h e most m o s t difficult d i f f i c u l t member to t o fully f u l l y understand. understand, The problem problem is i s how can c a n such s u c h a tthin h i n sand s a n d and gravel g r a v e l deposit d e p o s i t cover c o v e r such such a large l a r g e area? area? Stokes S t o k e s (1950) ( 1 9 5 0 ) suggests s u g g e s t s pediment p e d i m e n t-type - t y p e deposition d e p o s i t i o n and and Witkind Witkind and Thaden Thaden (1963, ( 1 9 6 3 , pp.. 26) believe b e l i e v e that t h a t trees t r e e s grevl grew along along Shinarump Shinarump streams s t r e a m s in i n a savannah-like s a v a n n a h - l i k e climate. climate. An important i m p o r t a n t factor factor in n the t h e Paria P a r i a area a r e a is i s the t h e high h i g h content c o n t e n t of of tuffaceous t u f f a c e o u s material m a t e r i a l in i n the the 49 49- e r c e n t ) and in i n Honitor Monitor B u t t e (20 percent). percent) . Shinarump (15 ppercent) Butte This This ' n d i c a t e s a local l o c a l volcanic v o l c a n i c source s o u r c e to t o the t h e south s o u t h or o r west w e s t of of ~icates Paria. Paria. Xn addition a d d i t i o n at a t South S o u t h Honument Monument Valley V a l l e y (Stewart, ( S t e w a r t , and others, o t h e r s , 1959, 1959, In p 544) the t h e Shinarump Shinarump has h a s a hhigh i g h percent p e r c e n t of of feldspar f e l d s p a r and and mica mica p. i n d i c a t i n g a granitic g r a n i t i c source s o u r c e tto o the t h e southeast. southeast. indicating D i f f e r e n t topography topography Different in different d i f f e r e n t source s o u r c e areas a r e a s could c o u l d be b e responsible r e s p o n s i b l e for f o r different d i f f e r e n t climates climates in in the t h e local l o c a l areas a r e a s of of deposition. deposition. in W i t h o u t grasses g r a s s e s in i n the t h e Triassic, Triassic, Without even a climate c l i m a t e that t h a t could c o u l d support s u p p o r t large l a r g e conifers c o n i f e r s might m i g h t not n o t have have even s u f f i c i e n t ground g r o u n d vegetation v e g e t a t i o n to t o retard r e t a r d or o r confine c o n f i n e fluvial f l u v i a l and and sufficient a l l u v i a l processes. processes. alluvial Stewart S t e w a r t and others o t h e r s (1959, ( 1 9 5 9 , p. p . 563) 5 6 3 ) postulate p o s t u l a t e a ttectonic e c t o n i c uplift uplift i n the t h e source s o u r c e area a r e a accompanied a c c o m p a n i e d by o l c a n i c activity--and a c t i v i t y — a n d slight s l i g h t uplift uplift in by vvolcanic a t least l e a s t lack l a c k of of subsidence s u b s i d e n c e in i n ttt.e h e depositional d e p o s i t i o n a l a reas. reas. or at T h i s would would This account for f o r a large l a r g e volume v o l u m e of of poorly p o o r l y sorted s o r t e d material m a t e r i a l dispersed d i s p e r s e d over over account a r e a and the t h e lack l a c k of of thick t h i c k a ccumulation. ccumulation. a wide area T h i s resembles r e s e m b l e s the the This pediment concept c o n c e p t of of Stokes S t o k e s but b u t no m e n t i o n of of environment e n v i r o n m e n t or o r climate climate pediment mention I s made by Stewart S t e w a r t and others. others. is S t r e a m s flowed f l o w e d from from tthe h e southeast s o u t h e a s t to t o the t h e northvlest n o r t h w e s t during during Streams Shinarump time t i m e with w i t h the t h e Hogollon M o g o l l o n Highlands H i g h l a n d s being b e i n g the t h e main m a i n source s o u r c e and and Shinarump the Ancestral A n c e s t r a l Rockies R o c k i e s and and Uncompaghre Uncompaghre Highlands H i g h l a n d s also a l s o being b e i n g important important the (Poole, ( P o o l e , 19(1). 1961). According A c c o r d i n g to t o SteTdart S t e w a r t and others o t h e r s (1959, ( 1 9 5 9 , p. p . 563) 5 6 3 ) the t h e area a r e a of of deposition Mooni d e p o s i t i o n started s t a r t e d to t o subside s u b s i d e in in M n itor t o r Butte B u t t e time t i m e a.nd and sediments sediments accumulated. accumulated. V o l c a n i s m and t0ctonic t e c t o n i c uplift u p l i f t in i n tthe h e source s o u r c e area area Voleanism c o n t i n u e d and str s t r eeams a m s still s t i l l flo\ilec1 f l o w e d from from the t h e SOli s o u theast t h e a s t (Pool ( P o o l e , 1961). 1961). continued 50 50 material Paria The 20 ppercent e r c e n t ttuffaceous uffaceous m a t e r i a l iin n tthe he P a r i a aa.rea r e a iindicates n d i c a t e s the the llocal o c a l vvolcanic o l c a n i c ssource o u r c e tto o tthe h e ssouth o u t h was t i l l ppresent. resent. was sstill A fluvial A fluvial with eenvironment nvironment w i t h pperhaps e r h a p s some sscattered c a t t e r e d llacustrine a c u s t r i n e ddeposits e p o s i t s has has been e l l eestablished s t a b l i s h e d ffor o r tthe he M o n i t o r Butte B u t t e Member. been w well Monitor The ddecrease and ddecrease of the The e c r e a s e iin n ggrain r a i n ssize i z e and e c r e a s e iin n ssorting o r t i n g of the P etrified F o r e s t Member long w i t h iirr r r eegular g u l a r bbedding e d d i n g and minor Petrified Forest Hember aalong ~vith and minor ddiastems i a s t e m s iindicate n d i c a t e rrapid a p i d ssubsidence ubsidence w i t h intervening i n t e r v e n i n g pperiods e r i o d s when with s u b s i d e n c e hhalted a l t e d ((Stewart S t e w a r t and t h e r s , 1959, 1 9 5 9 , pp.. 5563). 63). subsidence and oothers, IIt t would would seem l o g i c a l tthat h a t during d u r i n g pperiods e r i o d s of of sstability t a b i l i t y llakes a k e s and o u l d form form logical and swamps swamps w would o l c a n i c ash a s h could c o u l d cconcentrate o n c e n t r a t e in i n tthe h e quasi-stable q u a s i - s t a b l e lacustrine lacustrine and vvolcanic environments. environments. The silica s i l i c a bbeds e d s and and bedded b e d d e d petrified p e t r i f i e d wood probably probably accumulated a c c u m u l a t e d in i n such s u c h an env e n v ironIllent. ironment. It I t a lso l s o f ecll:)ws l l o w s tthat h a t pper-iods e r i o d s of of heavy volcanism v o l c a n i s m ",ith w i t h much suspended s u s p e n d e d ash a s h in i n the t h e air a i r would u t oout u t part part heavy \vould ccut of of the t h e sun's s u n ' s rays r a y s and for f o r periods p e r i o d s of of time t i m e create c r e a t e a ccooler o o l e r climate. climate. S l i g h t climatic c l i m a t i c changes, c h a n g e s , different d i f f e r e n t rates r a t e s of of subsidence, s u b s i d e n c e , the t h e presence presence Slight or or absence a b s e n c e of of l aakes k e s or o r swamps, and differential d i f f e r e n t i a l amounts a m o u n t s of of volcanic volcanic material m a t e r i a l must m u s t certainly c e r t a i n l y produce p r o d u c e at a t least l e a s t slight s l i g h t chemical c h e m i c a l changes c h a n g e s and and p e r h a p s account a c c o u n t for f o r the t h e color c o l o r banding. banding. perhaps As the t h e volcanic v o l c a n i c activit a c t i v i t yy decrease d e c r e a s e dd,, tectonic t e c t o n i c activity a c t i v i t y of t h e source s o u r c e area a r e a substantially s u b s t a n t i a l l y decreased, d e c r e a s e d , and a slos l o w~., but b u t uniform u n i f o r m rate rate the s u b s i d e n c e in i n the t h e b asin a s i n continued, c o n t i n u e d , the t h e fine f i n e horizontal h o r i z o n t a l silts s i l t s and and of subsidence l i m e s t o n e s of of the t h e 0,.,1 Owl Rock we:i:"e w e r e deposited. deposited. limestones f l u v i a l and lacustri.ne lacustrine The fluvial complex in i n w:hich h i c h these t h e s e siltstones s i l t s t o n e s and limestones l i m e s t o n e s ,-lere w e r e deponited d e p o s i t e d had had a Very v e r y low energy e n e r g y with w i t h very v e r y little l i t t l e erosion. erosion, 51 5-1 a b s e n c e of of the t h e Church C h u r c h Rock Member (in ( i n the t h e Paria P a r i a area) a r e a ) which which The absence t i t u t e s an important i m p o r t a n t ppart a r t of of the t h e Chinle C h i n l e Formation F o r m a t i o n tto o the t h e north, north, constitutes n S e a s t and southeast s o u t h e a s t indicates i n d i c a t e s that t h a t following f o l l o w i n g 0,,71 Owl Rock deposition d e p o s i t i o n the the east, and P a r i a area a r e a became became a ppositive o s i t i v e area. area. Paria T h i s unconformity u n c o n f o r m i t y at a t the t h e base base This of the Glen Glen Canyon Canyon Group has h a s little l i t t l e or o r no relief. relief. of Glen Glen Canyon Canyon Group Group Canyon Group (Reeside ( R e e s i d e and and others, o t h e r s , 1927, 1 9 2 7 , p. p . 787) 787) The Glen Canyon was named for f o r a thick t h i c k section s e c t i o n of of 3 sandstone s a n d s t o n e formations f o r m a t i o n s exposed e x p o s e d in in w a l l s of of Glen G l e n Canyon. Canyon. the walls g r o u p and its i t s equivalents e q u i v a l e n t s are a r e present present The group throughout Utah U t a h east e a s t of of tthe h e Wasatch W a s a t c h Line, L i n e , southwestern s o u t h w e s t e r n Colorado, Colorado, throughout n o r t h w e s t e r n New Mexico, M e x i c o , northern northern A r i z o n a , and pparts a r t s of of southern southern northwestern Arizona, Nevada. 'evada. Four ~cu:::- f o r m a t i o n s have h a v e bbeen e e n ?seigned a s s i g n e d to t o the t h e ~len G l e n Canyon Canyon Group Group formations and are a r e in i n .ascending a s c e n d i n g order o r d e r the t h e lVingate W i n g a t e Sandstone, S a n d s t o n e , Hoenave Moenave Formation, Formation, Kayenta Kayenta Fo~ation, F o r m a t i o n , and and .Navaj0 N a v a j o Sandstone. Sandstone. The Glen G l e n Canyon Canyon Group Group i n c l u d e s rocks r o c k s of of Triassic T r i a s s i c and Jurassic J u r a s s i c age. age. includes L e w i s and and others o t h e r s (1961) (1961) Lewis reviewed reviewed the t h e faunal f a u n a l evidence e v i d e n c e found f o u n d in i n the t h e various v a r i o u s formations f o r m a t i o n s and and t h e i r revised r e v i s e d age a g e determinations d e t e r m i n a t i o n s are a r e used u s e d in i n this t h i s report. report. their In I n the t h e Paria P a r i a area a r e a the t h e Glen G l e n Canyon (;roup Group is i s approximately approximately 2200 to t o 2l.00 2400 feet f e e t tthick h i c k and is i s dominantly d o m i n a n t l y s2-uds s a n d s ttone o n e \-1i w i th t h some siltstone mudstone. s i l t s t o n e and m udstone. The group g r o u p thickens t h i c k e n s to t o the t h e \.;est w e s t and the the « i l t s t o n e and mudstone m u d s t o n e content c o n t e n t increases; i n c r e a s e s ; in i n the t h e Zion-Cedar Z i o n - C e d a r City C i t y area area Siltstone Navajo is i s 2l~OO 2400 feet f e e t thick t h i c k and and the t h e KayentCl K a y e n t a if'; i s nearly n e a r l y 1000 feet feet the Navajo thick t h i c k and ddo~inantly o m i n a n t l y fine f i n e grained. grained. Some of of tthe h e outst o u t s t aanding n d i n g scenery s c e n e r y of of the t h e Hest w e s t is i s fOrT.lCd formed by the Glen Glen Canyon Canyon Group. Group. The V Vermilion e r m i l i o n Cliffs, C l i f f s , composed composed mainly m a i n l y of of the the 52 Glen Canyon Canyon G Group, from Z I wer Glen r o u p , ffo11moJ o l l o w aan n iirregular r r e g u l a r ppattern a t t e r n from i o n Park Park lOWer . .Zion F e r r y tthat h a t iis s dicta d i c t a tted e d by t h e structure s t r u c t u r e of of tthe h e Grand Grand Canyon to Lees Ferry by the u p l i f tt and the t h e aassociated s s o c i a t e d faults. faults. uplif P a r i a tthe h e northeast-trending northeast-trending At Paria Verm i l i ° Cliffs C l i f f s ttu u rr nn abruptly a b r u p t l y so s o uuth,yard t h w a r d and ffo110;.7 o l l o w the t h e north-south north-south Vetm i lion n trending E ast K aibab m onocline. trending East Kaibab monocline. T h i s structure, s t r u c t u r e , kno\Vll known as a s the the This forms the t h e bbackbone a c k b o n e of of the the P a r i a area. area. Cockscomb, forms Paria Wingate W i n g a t e Sandstone Sandstone The W Wingate i n g a t e Sandstone S a n d s t o n e (Dutton, ( D u t t o n , 1885, 1 8 8 5 , pp.. 136) 136) hhas a s been been involved in i n several several m i s c o r r e l a t i o n s ; one involving i n v o l v i n g tthe h e ttype y p e section section iuvolved miscorre1ations; at Fort F o r t Wingate, W i n g a t e , New Mexico, M e x i c o , hhas a s bbeen e e n rectified r e c t i f i e d by s t rricting i c t i n g the the at by r eest o r i g i n a l usage u s a g e (Baker ( B a k e r and others, o t h e r s , 1947; 1947; W r i g h t and Becker, B e c k e r , 1951). 1951). original Hright The e r Dlain main miscorrela r a i s c o r r e l a ttion i o n 0ccun:ed o c c u r r e d iiI i n ::5outhwes s o u t h w e s t e rnl n U t a h and northern o t hher Utah dnd northern Arizona i nr.cluding c l u d i n g tthe he P a r i a and L e e s Ferry F e r r y areas. areas. Arizona Paria Lees IIn n these t h e s e areas a r e a s the the m a s s i v e , cliff-forming c l i f f - f o r m i n g sandstone s a n d s t o n e now assigned a s s i g n e d tto o tthe h e Moenave Formation massive, Moenave Formation ( H a r s h b a r g e r and and ooth t h eerr s, s , 1957, 1 9 5 7 , pp.. 12) 12) was o r i g i n a l l y considered considered (Harshbarger ,vas originally Wingate. I n tthe h e Kanab Canyon Canyon area a r e a a tongue t o n g u e of he N a v a j o w'ithin w i t h i n the the In of tthe Navajo Kayenta Formation F o r m a t i o n was m i s t aaken k e n ffor or W i n g a t e bby y Gregory G r e g o r y (1950) ( 1 9 5 0 ) and the the Kayenta wa s mist ~Hngate f o r m a t iion o n .,'<1:; was then t h e n rrecognized e c o g n i z e d i nn many pparts a r t s of of ssouthwestern o u t h w e s t e r n Utah. Utah. format r e c e n t work work by Averitt A v e r i t t and others o t h e r s ((1955) 1 9 5 5 ) and H a r s h b a r g e r and More recent und Harshbarger o t h e r s (1957) hhas a s ge g e ne n e rally r a l l y shown tthat h a t tthe he W i n g a t e is i s nnot o t ppresent r e s e n t in in others Hingate southern U t a h and northern n o r t h e r n ArizollCl A r i z o n a west w e s t of of Lees L e e s Ferry. Ferry. Southern Utah Wilson W i l s o n (1965, ( 1 9 6 5 , pp.. 38) sugges s u g g e s ts t s that t h a t a sandst s a n d s t oone n e unit unit Underlying Paria Lees Ferry n a e r l y i n g the t h e Hoenave Moenave ForlllaU_on F o r m a t i o n at at P a r i a and and L ees F e r r y may bbe e the the Wingate i n g a t e Sandstone S a n d s t o n e .. The i.Jingate Paria W i n g a t e i;_8 s recogniz r e c o g n i z eedd at at P a r i a for f o r the the 53 f l o w i n g rreasons: easons: following t h i s unit u n i t has h a s the t h e same lithology l i t h o l o g y and stratigraphic this and stratigraphic o s i t i o n as a s uunquestioned nquestioned W i n g a t e ; uunder n d e r the t h e binocular b i n o c u l a r microscope microscope position Wingate; c o n t r a s t of of the t h e Wingate Wingate w i t h the t h e Dinosaur D i n o s a u r Canyon Canyon iis s striking; striking; the contrast with e a s t , southeast, s o u t h e a s t , south, s o u t h , and southwest s o u t h w e s t edges e d g e s of t s depositional depositional on the east, of iits b a s i n the t h e massive m a s s i v e sandstones s a n d s t o n e s of of tthe h e VJingate W i n g a t e (Lukachukai ( L u k a c h u k a i Member of of basin Harshbarger and others) o t h e r s ) thin t h i n to t o a ddepositional, e p o s i t i o n a l , feather f e a t h e r eedge--a d g e — a few few Harshbarger miles west west of of Paria P a r i a would w o u l d mark m a r k tthe he w e s t edge e d g e of of deposition; d e p o s i t i o n ; tthe h e VJingate Wingate miles west of Paria P a r i a is i s highly h i g h l y jjointed o i n t e d which w h i c h is i s characteristic c h a r a c t e r i s t i c of of tthe h e Wingate Wingate of e l s e w h e r e ; and finally, f i n a l l y , the t h e upper u p p e r and and lower l o w e r contacts c o n t a c t s aare r e similar s i m i l a r to to elsewhere; c o n t r a c t s of of unquestionable u n q u e s t i o n a b l e vJingate W i n g a t e the t h e east--the e a s t — t h e lower l o w e r ccontact o n t a c t with with the contracts the Chinle C h i n l e is i s aa planar, p l a n a r , sharp, s h a r p , unconformity u n c o n f o r m i t y and and tthe h e ccontact o n t a c t "'ith w i t h the the the i s gradational g r a d a t i o n a l and may be b e intertongued. intertongued. Moenave is In I n the t h e Paria P a r i a area a r e a tthe h e Wingate W i n g a t e Sandstone S a n d s t o n e forms f o r m s tthe h e lowest lowest cliff c l i f f of of the t h e Cockscomb (fig. ( f i g . 10). 10). The Wingate W i n g a t e is i s 42 feet f e e t tthick h i c k at at the central more c e n t r a l ppart a r t of of the t h e Cockscomb and approximately a p p r o x i m a t e l y 60 or or m o r e feet feet thick ~.Jingate t h i c k near n e a r Paria-P a r i a — this t h i s is i s logical l o g i c a l as a s the the W i n g a t e sshould h o u l d tthicken h i c k e n tto o the the northeast n o r t h e a s t .. The Wingate W i n g a t e is i s a pale-orange, p a l e - o r a n g e , ffine~grained, i n e - g r a i n e d , fair f a i r tto o wellwell- s o r t e d , friable f r i a b l e sandstone s a n d s t o n e ,'lith w i t h sub-round s u b - r o u n d to t o sub-angular, s u b - a n g u l a r , vitreous vitreous Borted, q u a r t z grains g r a i n s and iron i r o n oxide o x i d e cement. cement. to waxy quartz Q u a r t z composes over Quartz composes over " percent p e r c e n t of the t h e grains g r a i n s and a silt s i l t matrix m a t r i x is i s less l e s s than t h a n 5 percent percent 95 i s in i n sharp s h a r p contrast c o n t r a s t to t o the t h e overlying o v e r l y i n g Dinosaur D i n o s a u r Canyon which is Canyon Member °f the the Hoenave Moenave Formation. Formation. of There T h e r e are a r e no horizont h o r i z o n t a l b eed d ss in i n the t h e Wing W i n gatea t e —-the t h e entire entire Hit has h a s massive m a s s i v e tange t a n g e nntial-type t i a l ™ t y p e cross c r o s s lam.inations l a m i n a t i o n s and s highly highly unit and iis jOinted. jointed. e x a c t correlation c o r r e l a t i o n of of tthe he W i n g a t e at a t Paria P a r i a with w i t h the the The exact Wingate Wingate i n the t h e Circle C i r c l e Cliffs C l i f f s is i s impossible i m p o s s i b l e unless u n l e s s deep d e e p ~ells w e l l s were were ingate in d r i l l e d in i n key k e y areas a r e a s tthrough h r o u g h tthe h e tthick h i c k Cretaceous C r e t a c e o u s sediments sediments to be drilled t 0 of the t h e Kaiparowits K a i p a r o w i t s Basin. Basin. of I t iis s ppossible o s s i b l e that t h a t this t h i s is i s a pod-shaped pod-shaped It l o c a l dune deposit d e p o s i t not n o t connected c o n n e c t e d to t o the t h e main m a i n mass m a s s of of Wingate W i n g a t e in i n the the local C i r c l e Cliffs C l i f f s area, a r e a , bbut u t the t h e evidence e v i d e n c e ppresented r e s e n t e d above a b o v e seems s e e m s to t o indicate indicate Circle t h a t this t h i s is i s bonafide bonafide W i n g a t e Sandstone. Sandstone. that Wingate No fossils f o s s i l s have h a v e bbeen e e n ffound o u n d in i n tthe h e Wingate W i n g a t e Sandstone S a n d s t o n e of of the the P a r i a area a r e a bbut u t its i t s stratigraphic s t r a t i g r a p h i c position p o s i t i o n and ppaleontologic a l e o n t o l o g i c evidence evidence Paria given by Lewis and others o t h e r s (1961) ( 1 9 6 1 ) indicate i n d i c a t e a Late Late T r i a s s i c age. age. &iven Triassic The Wingate winds W i n g a t e was deposited d e p o s i t e d by northwesterly northwesterly w i n d s in i n a slowly slowly s u b s i d i n g basin b a s i n in i n an a n arid a r i d climate. climate. subsiding s e d i m e n t a r y structnres s t r u c t u r e s are are The sedimentary s i m i l a r to t o tthose h o s e of of modern m o d e r n dunes d u n e s in i n large l a r g e sand s a n d deser~s. deserts. similar I n some In a r e a s of of the t h e Colorado C o l o r a d o Plateau P l a t e a u local l o c a l limestone l i m e s t o n e bbeds, e d s , presumably presumably areas d e p o s i t e d in i n small s m a l l lakes l a k e s or o r oases, o a s e s , are a r e found. found. deposited Hoenave Moenave Formation Formation Parts P a r t s of of the t h e Moenave Formation F o r m a t i o n (Harshbarger ( H a r s h b a r g e r and and others, o t h e r s , 1957) 1957) were at a t one ttime i m e included i n c l u d e d in i n the the. Chinle C h i n l e Formation F o r m a t i o n or o r Wingate W i n g a t e Sandstone Sandstone until u n t i l it i t was discovered d i s c o v e r e d that t h a t in i n places p l a c e s the t h e Moenave overlies o v e r l i e s the the Wingate. The type t y p e section s e c t i o n is i s at a t the t h e southern s o u t h e r n end end of of the t h e Echo Cliffs Cliffs near Moenave, Arizona. Arizona. near T h a t the the M Moenave i s younger y o u n g e r than t h a n the the That oenave is i s clearly c l e a r l y shmvtl shown in i n much of of tthe he N a v a j o0 Country C o u u t r y (Harshbarger (Harshbarger Wingate is Navaj o t h e r s , 1957, 1 9 5 7 , p. p . 12, 1 2 , p. p . 15, 1 5 , fig. f i g . II) I I ) and in i n the t h e Paria P a r i a area a r e a as as and others, discussed -i-scussed ear e a rIier. lier. d )5 55 T h r o u g h o u t the t h e Vermilion V e r m i l i o n and and Echo Cliffs C l i f f s and and much of of the the Throughout Navajo Country C o u n t r y the t h e Hoenave Moenave Formation F o r m a t i o n is i s divided d i v i d e d into i n t o two distinct distinct Navajo members, Members, a lower l o w e r silty s i l t y sandstone s a n d s t o n e sequence, s e q u e n c e , the t h e Dinosaur D i n o s a u r Canyon Canyon Kember, massive Member, and an upper upper m a s s i v e sandstone, s a n d s t o n e , the t h e Springdale S p r i n g d a l e Sandstone Sandstone Member. Member. Both Both are a r e easily e a s i l y rrecognized e c o g n i z e d and and are a r e mapped mapped separately s e p a r a t e l y in i n this this report. report. Dinosaur Cart Canyon Dinosaur yon Member The Dinosaur D i n o s a u r Canyon Canyon Member was named by Colbert C o l b e r t and Mook (1951, miles ( 1 9 5 1 , p. p . 151) for f o r exposures e x p o s u r e s in i n Dinosaur D i n o s a u r Canyon, C a n y o n , 10 m i l e s east e a s t of Arizona. Cameron, Arizona. i n o s a u r Canyon Canyon shows some marked m a r k e d differences differences The D Dinosaur i n lithology l i t h o l o g y and bedding b e d d i n g ttype y p e in i n the the N a v a j o Country C o u n t r y but b u t in i n the t h e Echo Echo in Navajo V e r m i l i o n Cliffs C l i f f s it i t is i s a fairly f a i r l y consistent c o n s i s t e n t hhorizor..tally o r i z o n t a l l y bedded bedded and Vermilion s i l t y sandstone s a n d s t o n e and siltstone s i l t s t o n e (Harshbarger ( H a r s h b a r g e r and others, o t h e r s , 1957, 1 9 5 7 , p. p . 13-15). 13-15). silty In Pari Dinosaur I n the the P a r i aa area a r e a the the D i n o s a u r Canyon Canyon Member is i s a steep steep s l o p e - or o r step-forming s t e p - f o r m i n g sandstone s a n d s t o n e and siltstone s i l t s t o n e that t h a t confornlably conformably slopeo v e r l i e s the t h e Wingate W i n g a t e Sandstone S a n d s t o n e and conformably c o n f o r m a b l y underlies u n d e r l i e s the t h e Springdale Springdale overlies Sandstone Member. Sandstone I t forms f o r m s the t h e lower l o w e r part p a r t of of tthe h e Cockscomb and ranges ranges It in thicknesses t h i c k n e s s e s from from 102 feet f e e t tto o over o v e r 150 feet. feet. in Along the t h e northern n o r t h e r n ppart a r t of of tthe h e Cockscomb and in i n some areas a r e a s of the Ve;nnilion V e r m i l i o n Cliffs, C l i f f s , tthe h e Dinosaur D i n o s a u r Canyon Canyon f01111s f o r m s a vvertical e r t i c a l cliff c l i f f and and is i s difficult d i f f i c u l t to t o separate s e p a r a t e from from the t h e overlying o v e r l y i n g Springdale S p r i n g d a l e Sandstone Sandstone (fig. ( f i g . 10). 10). The Dinosaur D i n o s a u r Canyon Canyon Hember Member iis s a pale p a l e reddish-orage, r e d d i s h - o r a g e , silty silty sandstone mudstone s a n d s t o n e with w i t h interbedded i n t e r b e d d e d fissile fissile m u d s t o n e and siltstone. siltstone. The 56 a n d s t o n e uunits n i t s are a r e composed composed of of very v e r y fine, f i n e , ppoorly o o r l y ssorted, o r t e d , angular, angular, sandstone s u b s p h e r i c a l , vvitreous i t r e o u s quartz q u a r t z grains. grains. 8ubspherical, Minor c h e r t grains g r a i n s and and Minor chert f e l d s p a r along along w i t h ttraces r a c e s of m i c a are a r e aaccessory ccessory m inerals. feldspar with of mica minerals. About 5 About p e r c e n t bblack l a c k grains, g r a i n s , pprobably r o b a b l y chert c h e r t and and heavy heavy m i n e r a l s , are are percent minerals, s c a t t e r e d throughout t h r o u g h o u t the t h e sandstone s a n d s t o n e uunits. nits. scattered with iron i r o n cement cement also a l s o cow~on. common. with C a l c i t e is i s the the m a i n cement cement Calcite main T h e s e sandstone s a n d s t o n e uunits n i t s show an an obvious obvious These t a n streak s t r e a k when freshly f r e s h l y scratched. scratched. tan The sandstones s a n d s t o n e s are a r e ggenerally e n e r a l l y 11 f e e t thick thick w i t h llow-angle o w - a n g l e cross c r o s s llaminations a m i n a t i o n s and and are a r e somevlhat somewhat to 8 feet with lenticular. lenticular. Interbedded with Interbedded w i t h the t h e sandstones s a n d s t o n e s aare r e rred, e d , fissile, f i s s i l e , slightly slightly micaceous shales shales w i t h iinterbedded n t e r b e d d e d lenticular l e n t i c u l a r ssandstones a n d s t o n e s and and siltstones siltstones micaceous with s e v e r a l iinches n c h e s tthick. hick. several From h e steep, s t e e p , sshale-covered h a l e - c o v e r e d sslope l o p e formed formed From tthe by the t h e Dinosaur D i n o s a u r Canyon Member it i t appears a p p e a r s tthat h a t tthe h e member i s mainly mainly Canyon Member member is shaly w i t h a few r e s i s t a n t sandstones s a n d s t o n e s that t h a t form s t e p s ; actually a c t u a l l y ",here where shaly with few resistant form steps; e r o s i o n is i s rrapid a p i d and the t h e member forms f o r m s a vertical v e r t i c a l cliff c l i f f as a s it i t does does erosion near P a r i a , it i t can c a n bbe e seen s e e n that t h a t the t h e member contains m o r e sandstone sandstone near Paria, member contains more c o a r s e siltstone s i l t s t o n e than t h a n shaly shaly m udstone. and coarse mudstone. t h i n shaly s h a l y units units The thin w e a t h e r rrapidly a p i d l y and and uundercut n d e r c u t the the m o r e resistant r e s i s t a n t sandstone s a n d s t o n e (fig. ( f i g . 12) 12) weather more g i v e the t h e member i t s typical t y p i c a l landform. landform. and give m,,"mber its Sedimentary and hhigh-angle S e d i m e n t a r y structures s t r u c t u r e s iinclude n c l u d e 10\,;'l o w - and i g h - a n g l e c.ross cross l a m i n a t i o n s , ripple r i p p l e marks m a r k s and rripple ipple m a r k cross c r o s s lhminations. a m i n a t i o n s , primary primary 18t1linations, mark current and som8 c u r r e n t llineation, i n e a t i o n , and some llenticular e n t i c u l a r bedding. bedding, Fossils Hember in F o s s i l s have h a v e not n o t bbeen e e n found f o u n d iin n the t h e Dinosaur D i n o s a u r Canyon Canyon Member in the t h e Paria P a r i a area, a r e a , hhOlvever, o w e v e r , the t h e ancet;tral a n c e s t r a l cocodilepy()tosuc.hus c o c o d i l e P r o t o s u c h u s hhas a s been been found Hook, 1951) found near n e a r tthe h e type t y p e ssection e c t i o n (Col ( C o l ber b e r t and and Mook, 1951) and and ffish i s h remains remains a r e fairly f a i r l y com common a t some localities. localities. are mon at 57 jeringdal e Sandstone S p r i n g d a l e Sandstone S a n d s t o n e was named named by by Gregory G r e g o r y ((1950, 1 9 5 0 , pp.. 67) The Springdale for a pprominent r o m i n e n t cliff-forming c l i f f - f o r m i n g sands s a n d s tt oone n e ex e x pposed o s e d near n e a r Springdale, S p r i n g d a l e , Utah; Utah; for a t the t h e south s o u t h entrance e n t r a n c e to to Z ion P ark. at Zion Park. G r e g o r y orginally o r g i n a l l y assigned assigned Gregory t h i s unit u n i t tthe h e Chinle C h i n l e Formation F o r m a t i o n but b u t more m o r e recent r e c e n t ~vork work hhas a s shmvn shown that that this S p r i n g d a l e Sandstone S a n d s t o n e is i s traceable t r a c e a b l e tto o the t h e Echo C liffs w h e r e it it the Springdale Cliffs where f i r s t mapped as a s Wingate W i n g a t e and later l a t e r included i n c l u d e d in i n tthe h e Moenave was first Formation (Harshbarger ( H a r s h b a r g e r and others, o t h e r s , 1957). 1957). Formation S p r i n g d a l e Sandstone Sandstone The Springdale u s u a l l y forms forms the t h e first f i r s t vertical v e r t i c a l cliff c l i f f of of the t h e Vermilion V e r m i l i o n Cliffs-Cliffs— usually where the t h e Kayenta K a y e n t a and and N a v a j o a rre e cliff-forming c l i f f - f o r m i n g it i t iis s tthe h e llowest o w e s t unit unit Navajo of a sheer s h e e r cliff c l i f f that t h a t may bbe e almost a l m o s t 1000 1000 feet f e e t hhigh. igh. of One of h e most most of tthe unusual ore o r e deposits d e p o s i t s is i s found f o u n d in i n the t h e Spring S p r i n g dale d a l e Sandstone S a n d s t o n e iin n the the unusual H a r r i s b u r g District, D i s t r i c t , Washington W a s h i n g t o n County, County, U tah. Harrisburg Utah. H e r e nnative a t i v e silver silver Here i s found found in i n massive m a s s i v e sandstones s a n d s t o n e s and and the t h e unit u n i t is i s locally l o c a l l y ccalled a l l e d the the is S i l v e r Reef Reef Sandstone S a n d s t o n e (Proctor ( P r o c t o r ,, 1953, 1 9 5 3 , p. p . 23). 23). Silver In I n tthe h e Paria P a r i a area a r e a the t h e Springdale S p r i n g d a l e Sandst S a n d s t oone n e fforms o r m s a sheer, sheer, unscalable u n s c a l a b l e cliff c l i f f that t h a t is i s breeched b r e e c h e d in i n only o n l y four f o u r pla p l a cce e ss iin n 9 miles. miles. lower contac c o n t a c t x?ith t h e Dinosaur D i n o s a u r Canyon Canyon is I s sha s h a rrp p and be The lower \vith the and may be u n c o n f o r m a b l e — t h e upper u p p e r cont c o n t a cc c t 'w i t h the t h e Kayenta K a y e n t a i ss ggradational radational unconron11able--the ;vith a r bitra b i t r a rry. y. and somewhat ar S pringdale r i n g d a l e Sandstone S a n d s t o n e r aanges n g e s from to The Sp from 125 to over 200 feet--part f e e t — p a r t of of tthis h i s large l a r g e difference d i f f e r e n c e is i s do tto o tthe h e arbitrary arbitrary aver c o n t a c t with w i t h the t h e Kayenta; Kayenta; w h e r e the t h e Sp:cing S p r i n g ddale--Kayenta a l e — K a y e n t a ccontact o n t a c t is is contact \vhere exposed on a cliff c l i f f face, f a c e , the t h e boundary b o u n d a r y can c a n be b e picked picked w i t h some exposed with a c c u r a c y , but b u t ~vhen when the t h e contact c o n t a c t is i s on tthe h e dipsl d i p s l oope p e of of tthe h e Cockscomb, Cockscomb, accuracy, the boundary b o u n d a r y is i s aarrbitrary. bitrary. 58 S p r i n g d a l e Sandstone S a n d s t o n e Member of of t hhe e Hoenave Moenave Formation F o r m a t i o n is is The Springdale e d d i s h - b r o w n , vvery e r y ffinei n e - tto o m e d i u m - g rained, r a i n e d , ppoorly o o r l y sorted, sorted, a reddish-brown, mediwn-g a r s l i g h t l y friable, f r i a b l e , silty s i l t y sandstone. sandstone. slightly S p r i n g d a l e contains c o n t a i n s 10 10 The Springdale percent w h i t e feldspar f e l d s p a r grains,S g r a i n s , 5 percent p e r c e n t sedimentary s e d i m e n t a r y rock r o c k fragments-fragments—• percent white m o stly t l y chert c h e r t and quartzite, q u a r t z i t e , and and approximately a p p r o x i m a t e l y 4 percent p e r c e n t black b l a c k mica. mica. mos l a t t e r may bbe e responsible r e s p o n s i b l e for f o r the t h e purplish p u r p l i s h cast c a s t that that The latter c h a r a c t e r i z e s the t h e unit u n i t in i n southwestern southwestern U tah. characterizes Utah. u a r t z grains grains The qquartz a r e extremely e x t r e m e l y varied; v a r i e d ; some are a r e orange, o r a n g e , some amber, a m b e r , and and some clear. clear. are s p h e r i c a l , broken, b r o k e n , or o r subangular s u b a n g u l a r gra g r a i nns s and their their They may bbee spherical, s u r f a c e textures t e x t u r e s are a r e extremely e x t r e m e l y varied--vitreous, v a r i e d — v i t r e o u s , waxy, w a x y , frosted, f r o s t e d , and and surface f r e s h l y bbroken. roken. freshly The cement c e m e n t is i s calcite c a l c i t e and iron. iron. c o n t a i n s about a b o u t 15 percent p e r c e n t silt s i l t matrix. matrix. contains The sandstone sandstone I n t e r b e d d e d with w i t h the the Interbedded lenticular m a s s e s of of sandstone, s a n d s t o n e , e::p2cially e s p e c i a l l y nnear e a r the t h e tC? t o p of of tth,= h e ~,'!en'.ber, member, lenticular masses a r e thin t h i n siltstones. siltstones. are L i k e tthe h e sandstone s a n d s t o n e beds b e d s tthe h e siltstone s i l t s t o n e is is Like h i g h l y lent l e n ticular. icular. highly Th~ extreme The e x t r e m e lenticular l e n t i c u l a r bbedding e d d i n g is i s the t h e most m o s t characteristic characteristic f e a t u r e of of tthe h e Springdale S p r i n g d a l e Sands S a n d s tone. tone. feature I n d i v i d u a l lentils l e n t i l s are a r e generally generally Individual t o 15 15 feet f e e t thick t h i c k and and several s e v e r a l hundred h u n d r e d feet f e e t wide. wide. 1 to Many of of the the Hany lenticular by vvery l e n t i c u l a r beds b e d s are a r e separated s e p a r a t e d by e r y thin t h i n s.i.lt s i l t bbeds e d s although a l t h o u g h in in l o w e r 40 feet f e e t of of the t h e member 3iJ.t s i l t is i s rare. rare. the lower individual The individual lentils l e n t i l s are a r e highly h i g h l y cross c r o s s l aarninated; m i n a t e d ; bboth o t h the t h e lOH low and high h i g h angle angle type are a r e prese.nt p r e s e n t but b u t the t h e cross c r o s s laminations l a m i n a t i o n s do not n o t "leatheT w e a t h e r as as p r o m i n e n t l y as a s thos t h o s ee iin n tthe h e overlying o v e r l y i n g Kayenta K a y e n t a and. and Navaj N a v a j o0 FOTInations. Formations. prominently The Springdale S p r i n g d a l e Sandstone S a n d s t o n e , :i..s i s probably p r o b a b l y equivalent e q u i v a l e n t ,-lith w i t h the the K a y e n t a at a t Kayenta, K a y e n t a , Arizona A r i z o n a (Wilson, ( W i l s o n , 1965, 1 9 6 5 , p. p . 40). 40), type Kayenta Southwest Southwest °f Kayenta) Kayenta, A r i z o n a t hhe e Kayenta K a y e n t a r<. r a1ppidly i d l y grades g r a d e s :Lnto i n t o a silty s i l t y facies f a c i e s and and of Arizona 59 S9 • easily e a s i l y ddistinguished i s t i n g u i s h e d (although ( a l t h o u g h the t h e contact c o n t a c t is i s somewhat somewhat is s adational) ,radational) from he S pringdale S andstone. from tthe Springdale Sandstone. But nnortheast of a line But o r t h e a s t of line extending from tthe Kayenta-Marsh Pass of A Arizona extending from he K ayenta-Marsh P a s s aarea r e a of r i z o n a tto o tthe h e Paria Paria area iin n U t a h tthe he K a y e n t a iis s ddominantly o m i n a n t l y ssandstone a n d s t o n e and s difficult difficult area Utah Kayenta and iis to from tthe Springdale Sandstone to distinguish d i s t i n g u i s h from h e uunderlying nderlying S pringdale S a n d s t o n e ((fig. f i g . 12). 12). Fossils uncommon iin Sandstone; F o s s i l s aare r e uncommon n tthe h e Springdale Springdale S a n d s t o n e ; tthe h e only only fossils were from tthe of tthe f o s s i l s eever v e r rreported eported w e r e ffish i s h from h e llowest o w e s t bbeds e d s of h e member (Eastman, (Eastman, 11911, 9 1 1 , 1917). 1917). Eastman workers E a s t m a n ((1917) 1 9 1 7 ) and and ssubsequent ubsequent w o r k e r s have have a s s i g n e d tthese h e s e ffish ish a L ate T r i a s s i c age. age. assigned Late Triassic Depositional Environments Depositiorta1Environmertts The sedimentary and tthe s e d i m e n t a r y strnctures s t r u c t u r e s and h e stratigraphic s t r a t i g r a p h i c pposition o s i t i o n in in t h i c k sequence s e q u e n c e of of continental c o n t i n e n t a l red r e d beds b e d s indicate i n d i c a t e that t h a t the the a thick Dinosaur Canyon was probably p r o b a b l y deposited d e p o s i t e d by a fluvial f l u v i a l processes. processes. Dinosaur The Dinosaur Canyon was deposited d e p o s i t e d in i n a local l o c a l basin b a s i n and although a l t h o u g h the the Dinosaur u n d e r l i e s it i t in i n tthe h e Paria P a r i a area a r e a as a s well w e l l as a s some areas a r e a s to to Wingate und~rlies t h e east, e a s t , the t h e Dinosaur Dj/nosaur Canyon is i s probably p r o b a b l y contemporaneous c o n t e m p o r a n e o u s with w i t h much the of of the t h e Wingate W i n g a t e to t o th t h ee northeast. northeast. Therefore T h e r e f o r e in i n the t h e Paria P a r i a area a r e a and and parts p a r t s of of the t h e Navaj N a v a j o0 Country C o u n t r y the t h e basins b a s i n s of of the t h e two units u n i t s overlap o v e r l a p and and H a r s h b a r g e r and others o t h e r s (1957, ( 1 9 5 7 , p. p . 13) the t h e units u n i t s overlap. overlap. as shown by Harshbargel: In addition a d d i t i o n some of of the t h e sand s a n d from from the t h e Hingate W i n g a t e ,vas was redeposited r e d e p o s i t e d by b y the the r i v e r s of of the t h e Dinosaur D i n o s a u r Canyon. Canyon, rivers r i v e r s of of the t h e Dinosaur D i n o s a u r Canyon Canyon The riVCJ7S t h e i r source s o u r c e in i n the t h e Mogol M o g o llon l o n Highlands H i g h l a n d s to t o the t h e south. south. had their climate The climate was most likely l i k e l y semi-arid s e m i - a r i d to t o arid. arid. was The sedimentary s e d i m e n t a r y structures, s t r u c t u r e s , s tratigraphic t r a t i g r a p h i c position, p o s i t i o n , and and fossil f o s s i l fresh\>later f r e s h w a t e r fish f i s h indicate i n d i c a t e that t h a t the t h e Springdale S p r i n g d a l e Sandstone S a n d s t o n e Hember Member 60 d e p o s i t e d iin n a continental c o n t i n e n t a l fluvial f l u v i a l environment. environment. Moderate M o d e r a t e uplift uplift t h e source s o u r c e areas a r e a s tto o the t h e northeast, n o r t h e a s t , east, e a s t , and s o u t h e a s t fed fed i11 the and southeast water and sediment s e d i m e n t tto o streams s t r e a m s tthat h a t meandered m e a n d e r e d across a c r o s s flat f l a t alluvial alluvial water l a i n s depositing d e p o s i t i n g llarge a r g e ppoint o i n t bbars a r s tthat h a t formed formed tthe h e llenticular e n t i c u l a r strata strata plains f the t h e Springdale S p r i n g d a l e Sandstone. Sandstone. of 0 b l a c k mica, m i c a , much much of of the t h e feldspar feldspar The black of the t h e quartz q u a r t z pprobably r o b a b l y was derived d e r i v e d from h e crystaline c r y s t a l i n e rocks rocks and some of from tthe of the t h e Ancestral A n c e s t r a l Rockies R o c k i e s and and M ogollon H i g h l a n d s ; much of tthe h e varied varied of Mogollon Highlands; mlJch of q u a r t z and silt s i l t pprobably r o b a b l y was eroded e r o d e d from from sedimentary s e d i m e n t a r y rocks r o c k s that that quartz b e t w e e n the t h e crystalline c r y s t a l l i n e source s o u r c e aarea r e a and and the t h e bbasin a s i n of of deposition. deposition. were between f r o s t e d and wind wind faceted f a c e t e d qquartz u a r t z grains grains w e r e pprobably r o b a b l y derived derived The frosted ~"rere from the t h e Wingate W i n g a t e desert d e s e r t to t o the t h e nnorth o r t h and east e a s t and e r e carried c a r r i e d by by from and w were s t r e a m s and deposited d e p o s i t e d in i n tthe h e Springdale S p r i n g d a l e basin. basin. the streams a b u n d a n t bblac!z l a c k mica m i c a ,md and feldspar f e l d s p a r iil1dir.ate n d i c a t e thAt that The abundant chemical w e a t h e r i n g ,-las was vvery ery m i n o r and and the t h e climate c l i m a t e was probably probably chemical weathering minor dry and w a r m — t h e rred e d beds b e d s also a l s o indicate i n d i c a t e tthis. his. dry yJarm--the The Springdale Springdale Sandstone was deposited d e p o s i t e d iin n a m o d e r a t e l y ssubsiding u b s i d i n g bbasin a s i n tthat h a t was Sandstone moderately contemporaneous w i t h , but b u t pprobably r o b a b l y somewhat somewhat separate s e p a r a t e from from those t h o s e of of contemporaneous with, the Wingate Kayenta Wingate and K a y e n t a Formations. Formations. K a y e n t a Formation Formation Kayenta ayenta F o r m a t i o n was o r i g i n a l l y and questionably The K Kayenta F0:t111ation 'i"ras originally and questionably considered Limestone c o n s i d e r e d a ssandy a n d y facies f a c i e s of of tthe h e Todilto Todilto L i m e s t o n e by Gregory Gregory (1917, pp.. 56). 56). His Baker H i s doubts d o u b t s proved p r o v e d ccorrect) o r r e c t , and and in i n 1931 1931 B a k e r and o t h e r s introduced i n t r o d u c e d tthe he K ayenta F ormation w i t h a ttype y p e section s e c t i o n just just others Kayenta Formation with north Arh:ona. n o r t h of of Kayenta, Kayenta, A rizona. younger than t h a n tthe h e Kayenta. Kayenta. younger The Toclilto T o d i l t o is i s no,,! now knO'iffi known to t o bbe e much 61 At its most i t s type t y p e section s e c t i o n and throughout throughout m o s t of of southeastern s o u t h e a s t e r n Utah Utah F o r m a t i o n is i s a blanketblanketp a r t s of of western w e s t e r n Colorado, C o l o r a d o , the t h e Kayenta Ka3 enta Formation and parts 7 ,. e widespread, horizontally-bedded, cross-laminated sandstone y P , w i d e s p r e a d , h o r i z o~n t a l l y - b e d d e d , c r o s s - l a m i n a t e d s a n d s t o n e ttype with with subordinate s u b o r d i n a t e siltstone s i l t s t o n e and limestone. limestone. The formation f o r m a t i o n averages averages about about 150 feet f e e t thick t h i c k and forms f o r m s a rresistant e s i s t a n t ledge l e d g e tthat h a t ccaps a p s the the Wingate Cliff. Cliff. South Kayenta S o u t h and .west w e s t of of a lline i n e from from the the K a y e n t a aarea r e a to to the t h e Paria P a r i a area a r e a the t h e Kayenta K a y e n t a tthickens h i c k e n s and grades g r a d e s into i n t o a sshaly h a l y facies. facies. The Kayenta K a y e n t a Formation F o r m a t i o n of of the t h e Paria P a r i a area a r e a iis s ssimilar i m i l a r tto o the the type Kayenta K a y e n t a and is i s a ledge-forming l e d g e - f o r m i n g or o r cliff-forming c l i f f - f o r m i n g sandstone sandstone with w i t h some interbedded i n t e r b e d d e d siltstone s i l t s t o n e and at a t least l e a s t one o n e llimestone i m e s t o n e bed. bed. The Kayenta of tthe Kayenta often o f t e n forms f o r m s the t h e caprock c a p r o c k and dipslope d i p s l o p e of h e Cockscomb Cockscomb,. (fig. ( f i g . 12). 12). The K Kayenta a y e n t a is i s a lithologically l i t h c i o g i c a l l y complex complex ffluvial l u v i a l unit unit composed predaninantly p r e d o m i n a n t l y of of horizontally-bedded, h o r i z o n t a l l y - b e d d e d , cross-laminated, cross-laminated, variably v a r i a b l y textured, t e x t u r e d , poorly p o o r l y sorted, s o r t e d , well-cemented w e l l - c e m e n t e d tto o some\-lhat somewhat friable friable sandstone. sandstone. Most of of the t h e quartz q u a r t z is i s vvitreous i t r e o u s although a l t h o u g h many textures, Host many textures, shapes s h a p e s and sizes s i z e s of of quartz q u a r t z grains g r a i n s are a r e ppresent. resent. Feldspar F e l d s p a r composes composes about 15 percent p e r c e n t of of the t h e sandstone s a n d s t o n e and and a silt s i l t matrix m a t r i x aaccounts c c o u n t s for for about about 20 percent p e r c e n t of of the t h e unit. unit. about M i c a is i s present p r e s e n t in i n ttrace r a c e amounts. amounts. Hica The distinct d i s t i n c t amber amber or o r orange o r a n g e quartz q u a r t z grains g r a i n s of of the t h e Springdale Springdale S a n d s t o n e are a r e not n o t ppresent--most r e s e n t — m o s t of of the t h e grains g r a i n s are a r e cclear l e a r oorr light light Sandstone brown. d o m i n a n t color c o l o r of of the t h e Kayenta K a y e n t a is i s a grayish g r a y i s h oor r silverysilveryThe dominant red but b u t some light-buff l i g h t - b u f f bbeds e d s as a s -well a s vvery e r y deep-red d e e p - r e d bbeds e d s aare r e also also red well as seen. seen. Interbedded w i t h tthe h e s aand n d s ttones o n e s '-lhich w h i c h are a r e ggenerally e n e r a l l y several several Interbedded with f e e t thick t h i c k are a r e thin, t h i n , bbright-red r i g h t - r e d siltstone s i l t s t o n e and shaly s h a l y ssiltstone i l t s t o n e units units feet 62 62 t h a t vvery e r y ppoorly o o r l y sorted. sorted. .are that Vermili° ve~ilion n m i l e s west w e s t of of Paria P a r i a along a l o n g the the A few few miles C l i f f s tthis h i s is i s the t h e dominant d o m i n a n t lithology l i t h o l o g y of of tthe h e Kayenta. Kayenta. Cliffs At least l e a s t one o n e dense, d e n s e , gray, g r a y , ffreshwater r e s h w a t e r limestone l i m e s t o n e is i s present present near the t h e ttop o p of of the t h e formation. formation. near T h i s llimestone i m e s t o n e was observed o b s e r v e d iin n the the This southern s o u t h e r n ppart a r t of of the t h e Cockscomb Cockscomb along a l o n g the t h e highly h i g h l y faulted f a u l t e d KayentaKayentaNavajo contact c o n t a c t at a t several s e v e r a l llocations o c a t i o n s bbut u t due to t o tthe h e ffaulting a u l t i n g could could Navajo not be ttraced r a c e d laterally l a t e r a l l y and and is i s therefore t h e r e f o r e uuseless s e l e s s in i n correlation. correlation. DOt S e v e r a l limy l i m y beds, b e d s , tthough h o u g h not n o t as a s pure p u r e aas s tthose h o s e above, a b o v e , aare r e ppresent r e s e n t in in Several n o r t h e r n half h a l f of of tthe h e Cockscomb also. also. the northern Mud-pebble M u d - p e b b l e cconglomerates o n g l o m e r a t e s are a r e common and and ooccur c c u r in i n both b o t h the the s a n d s t o n e and siltstone. sandstone and siltstone. I n addition a d d i t i o n some of of tthe h e sand s a n d ggrains r a i n s form form In w e l l - c e m e n t e d bbunches u n c h e s tthat hat w e a t h e r out o u t as a s ssmall m a l l pellets p e l l e t s on the the well-cemented weather s u r f a c e of of the t h e rrock o c k and and form form a distinctive d i s t i n c t i v e layer l a y e r on tthe h e Kayenta Kayenta surface dipslope. dipslope. The sedimentary s e d i m e n t a r y structures s t r u c t u r e s include i n c l u d e bboth o t h lowl o w - and and high-angle high-angle cross c r o s s laminations. laminations. DOt not too t o o common. Current C u r r e n t lineation l i n e a t i o n iis s ppresent r e s e n t on some bbeds e d s but but The sandstones s a n d s t o n e s form f o r m horizontal, h o r i z o n t a l , somewhat somewhat lenticular lenticular beds (not ( n o t nearly n e a r l y as a s lenticular l e n t i c u l a r as a s tthe h e Springdale S p r i n g d a l e Sandstone) Sandstone) averaging by silty a v e r a g i n g about a b o u t 8 to t o 15 feet f e e t thick t h i c k separated s e p a r a t e d by s i l t y sshale h a l e beds b e d s ,". several s e v e r a l inches i n c h e s to t o several s e v e r a l feet f e e t tthick. hick. IIn n general g e n e r a l the t h e llower o w e r ppart a r t of the more the formation f o r m a t i o n has h a s thicker t h i c k e r bbeds e d s and and m o r e sand s a n d than t h a n tthe h e uupper p p e r part. part. r e s i s t a n t sandstones s a n d s t o n e s and interbedded i n t e r b e d d e d shaL~s s h a l e s are a r e responsible responsible These resistant for the t h e lledgy e d g y ccliff l i f f and dipslopes d i p s l o p e s so s o common tto o tthe h e Kayenta K a y e n t a ",here where for i t s typical t y p i c a l fades f a c i e s is i s developed. developed. its Where tthe h e Kayenta K a y e n t a fforms o r m s tthe h e clipslope d i p s l o p e of of tthe h e Cockscomb Cockscomb dipping dipping at a t 15 to t 40 4Q degrees d e g r e e s both b o t h contacts c o n t a c t s are a r e very v e r y ddifficult i f f i c u l t tto o pick pick 0 accurately. accurately. t h e southern s o u t h e r n portion p o r t i o n of of the t h e Cockscomb Cockscomb the the Along the K a y e n t a - N a v a j o contact c o n t a c t is i s in i n a fault f a u l t zzone o n e and both b o t h fformations o r m a t i o n s are are Kayenta-Navajo badly broken b r o k e n making m a k i n g the t h e contact c o n t a c t difficult d i f f i c u l t to t o pick. pick. badly B o t h contacts contacts Both of the t h e Kayenta K a y e n t a appear a p p e a r to t o bbe e conformable c o n f o r m a b l e bbut u t in i n viev7 v i e w of the of of the p r e c e d i n g statement s t a t e m e n t this t h i s cannot c a n n o t be b e said s a i d with w i t h certainty. certainty. preceding At Shurtz marked by a S h u r t z Gorge G o r g e tthe h e top t o p of of the t h e Kayenta K a y e n t a is is m a r k e d by r e l a t i v e l y obvious o b v i o u s 4 foot, f o o t , ddeep-red, e e p - r e d , silty s i l t y shale s h a l e tthat h a t fforms o r m s a notch notch relatively a t the t h e base b a s e of of tthe h e sheer sheer N a v a j o Cliff. Cliff. at Navajo U n f o r t u n a t e l y tthis h i s uunit n i t is is Unfortunately not present p r e s e n t in i n most m o s t of of the t h e area a r e a and elsewhere e l s e w h e r e the t h e Navajo-Kayenta Navajo-Kayenta Dot boundary is i s not n o t so s o definite. definite. boundary If most of the I f the t h e Springdale S p r i n g d a l e Sandstone S a n d s t o n e is i s equivalent e q u i v a l e n t tto o m o s t of the K a y e n t a , and the t h e silty s i l t y facies f a c i e s of of tthe h e Kayenta K a y e n t a equivalent e q u i v a l e n t to t o the the type Kayenta, upper ppart a r t of of the the N a v a j o0 Sandstone S a n d s t o n e of of eastern eastern U t a h as a s 'i-Jilsou W i l s o n (1965) (1965) upper Navaj Utah b e l i e v e s , then t h e n tthe h e Kayenta K a y e n t a of of the t h e Paria P a r i a area, a r e a , which w h i c h grades g r a d e s into i n t o the the believes, s i l t y facies f a c i e s a short s h o r t distance d i s t a n c e to t o the t h e west w e s t and south, s o u t h , is i s probably probably silty e q u i v a l e n t to t o ppart a r t of of the t h e Kayenta K a y e n t a and part p a r t of of the the N a v a j o of of eastern eastern equivalent Navajo Utah and Arizona. Arizona. T h i s uncertain u n c e r t a i n correlation c o r r e l a t i o n is i s ffurther u r t h e r complicated complicated This by intertonguing i n t e r t o n g u i n g of of the the N a v a j o and Kayenta K a y e n t a Formations F o r m a t i o n s tto o tthe h e west. west. Navajo t o n g u e s are a r e beautifully b e a u t i f u l l y exposed e x p o s e d in i n Johnson J o h n s o n and Canyons These tongues and Kanab Ca nyons i l e s to t o the t h e west w e s t respectively. respectively. 20 and 40 m miles l o w e r ttongue o n g u e of of the the The lower Navajo was m i s c o r r e l a t e d \vith w i t h the the W i n g a t e by Gr G r eg e g oory r y (1950). (1950). Navajo miscorrelated ~.Jingate K a y e n t a rrepresen e p r e s e n tts s a blanket-type b l a n k e t - t y p e fluvial f l u v i a l ddeposit. eposit. The I<ayenta In In its i t s typical t y p i c a l sandy s a n d y facies, f a c i e s , deposition d e p o s i t i o n slightly s l i g h t l y exceeded e x c e e d e d subsedence subsedence t h e large l a r g e volume v o l u m e of of sand s a n d was spread s p r e a d out o u t over over a w i d e area area and the vlide w i t h o u t acquiring a c q u i r i n g great g r e a t thickness; t h i c k n e s s ; to t o the t h e west w e s t and and ssouth o u t h of Paria without of Paria 64 s uIDIIJ· b s i d....e n cce e was more rrapid a p i d and the t h e grain g r a i n size s i z e decreases d e c r e a s e s rapidly. rapidly. ~··· _ The e n e r a l decrease d e c r e a s e in i n grain g r a i n size s i z e throughout t h r o u g h o u t the t h e pplateau l a t e a u country c o u n t r y indicates indicates with Kayenta streams s t r e a m s flowed f l o w e d from from east e a s t tto o west west w i t h tthe h e primary p r i m a r y source source being the t h e southern s o u t h e r n part p a r t of of tthe h e Uncompahgre Uncompahgre Highlands. Highlands. being T h a t the t h e Kayenta Kayenta That streams had a low gradient g r a d i e n t and and were w e r e near n e a r base b a s e level l e v e l as a s indicated i n d i c a t e d by by .treams t h e lack l a c k of of basal b a s a l channel c h a n n e l cutting c u t t i n g and and a lack l a c k (for ( f o r the t h e most m o s t part) part) tbe of intraformational i n t r a f o r m a t i o n a l channel c h a n n e l cutting. cutting. of v a r i e t y of of quartz q u a r t z and and The variety abundant abundant feldspar f e l d s p a r indicates i n d i c a t e s that t h a t the t h e hhighland i g h l a n d source s o u r c e area a r e a and and i n t e r v e n i n g ppiedmont i e d m o n t area a r e a supplied s u p p l i e d .both both crystalline c r y s t a l l i n e and sedimentary sedimentary intervening s o u r c e s in i n a dry, d r y , warm climate. climate. sources On the t h e basis b a s i s of of fossil f o s s i l rreptiles e p t i l e s bbelonging e l o n g i n g to t o the the superfamily superfamily T r i t y l o d o n t o i d e a found f o u n d near n e a r Kayenta, K a y e n t a , Arizona, A r i z o n a , Lewis L e w i s and and others others Trity1odontoidea (1961, p. p . 1439-1440) 1 4 3 9 - 1 4 4 0 ) assign a s s i g n the t h e Kayenta K a y e n t a FO~lliatio~ F o r m a t i o n a Late L a t e Triassic(?) Triassic(?) age. age. Triassic(?) T r i a s s i c ( ? ) arid and JJtirassic u r a s s i c Systems Systems Navajo N a v a j o Sandstone Sandstone Perhaps P e r h a p s tthe h e most m o s t impressive i m p r e s s i v e formation f o r m a t i o n of of the t h e Paria P a r i a area area and most of of southern s o u t h e r n Utah U t a h is i s the t h e Navaj N a v a j o0 Sandstone. Sandstone. The Navaj N a v a j 0o was named .by Gregory Navaj G r e g o r y (1915, (19.15, 1917) 1917) after a f t e r tthe he N a v a j o0 Country C o u n t r y of of the the four four corners c o r n e r s area. area. Navajo A striking s t r i k i n g feature f e a t u r e of of the the N a v a j o is i s tthe h e steady, steady, progressive, \vestward progressive, w e s t w a r d thickening; t h i c k e n i n g ; from from a depositional d e p o s i t i o n a l edge e d g e along along the Utah-Colorado Navajo U t a h - C o l o r a d o line l i n e the the N a v a j o thickens t h i c k e n s to t o about a b o u t 400 feet f e e t at at Comb Ridge, R i d g e , 600 feet f e e t in i n the t h e White W h i t e Canyon area, a r e a , 1500 feet f e e t in i n the the Canb Lees Fet"ry:trea, F e r r y a r e a , 1800 1800 feet f e e t along a l o n g the t h e E2St E a s t Kaibab K a i b a b Nonocline, M o n o c l i n e , 2200 2200 tees f e e t in i n the t h e Zion Z i o n area a r e a and and pperhaps e r h a p s close c l o s e to t o 3000 feet f e e t in i n southern southern feet 65 Nevada. The. N Navaj a v a j o0 is i s extremely e x t r e m e l y consistant c o n s i s t a n t iin n lithology l i t h o l o g y and and is is .early mi..nor and limestone n e a r l y a pure p u r e sandstone s a n d s t o n e every,.,here--very everywhere—very m i n o r silt s i l t and limestone are present p r e s e n t at a t some localities. localities. are In of the I n the t h e Paria P a r i a area a r e a tthe h e Navajo N a v a j o forms f o r m s the t h e backbone b a c k b o n e of the Cockscomb Vermilion Cockscomb and ccaps a p s the the V e r m i l i o n Cliffs C l i f f s and and forms f o r m s the t h e massive massive White Cliffs C l i f f s tto o tthe h e ,.,:rest. west. Due to t o tthe h e extreme e x t r e m e faulting, f a u l t i n g , shearing, shearing, and jjointing Navajo Paria most o i n t i n g of of the the N a v a j o in i n the the P a r i a area, a r e a , in in m o s t pplaces l a c e s its its typical well t y p i c a l landforms l a n d f o r m s are a r e not not w e l l developed. developed. Only Only nnorth o r t h of of the t h e Paria Paria River, Canyon (fig. and at R i v e r , along a l o n g Catstairs C a t s t a i r s Canyon ( f i g . 13) and a t scattered s c a t t e r e d locations locations along the Cockscomb does Navajo t h e Cockscomb d o e s tthe he N a v a j o form form ccharacteristic h a r a c t e r i s t i c rounded rounded buttes, with b u t t e s , nipples, n i p p l e s , slot s l o t canyons canyons w i t h sheer s h e e r cliffs, c l i f f s , hummocky slickrock s l i c k r o c k country, c o u n t r y , and massive m a s s i v e rounded r o u n d e d ddomes. omes. North of tthe N o r t h of h e Paria Paria River Rush B Beds--scme mast River tthe h e Navaj Navajo0 forms f o r m s the t h e Rush e d s — s o m e of of tthe he m o s t ert'ded, eroded, unpenetrable u n p e n e t r a b l e "slick " s l i c k rock" r o c k " country c o u n t r y anywhere. anywhere. m o s t of t h e Cockscomb tthe he N a v a j o forms f o r m s oone, n e , or o r more more Along most of the Navajo t w o , pparallel a r a l l e l razor-back r a z o r - b a c k ridges r i d g e s that t h a t are a r e bbadly a d l y shattered shattered commonly two, sandstone by nnumerous of calcite s a n d s t o n e ppenetrated e n e t r a t e d by u m e r o u s vveins e i n s of c a l c i t e and and hematite h e m a t i t e and and in at a t lleast e a s t one locality, l o c a l i t y , vveins e i n s of c o p p e r minerals. minerals. in of copper Where lfuere two r i d g e s are a r e ppresent r e s e n t they t h e y are a r e generally g e n e r a l l y sseparated e p a r a t e d by a "V"-shaped "V"-shaped ridges v a l l e y dev d e v eloped e l o p e d on a u l t or o r fault f a u l t zone. zone. valley on a ffault e d d i n g or o r cross cross No bbedding l a m i n a t i o n s are a r e apparent a p p a r e n t in i n tthis h i s highly h i g h l y shattered s h a t t e r e d rrock o c k and lam.ina.tions and any s e d i m e n t a r y study s t u d y of of the t h e Navajo N a v a j o iis s im p o s s i b l e along a l o n g tthese h e s e ri.dges. ridges, sedimentary mpossible fhe Navajo s t u d i e d iin n Shur S h u r ttz z G o r g e and Cat C a t stairs s t a i r s Canyon where The Navajo was ,.,:ras studied Gorge Canyon where i t is i s more ttypically y p i c a l l y Jeveloped. developed. it The sand sand grains g r a i n s of of the the N a v a j o are a r e oov~r v e r 98 ppercent e r c e n t quartz q u a r t z and and 'the Navajo 66 are most r e sub round, r o u n d , frosted f r o s t e d or o r vitreous, v i t r e o u s , well w e l l sorted, s o r t e d , and and m o s t aare r e very very a spherical. spherical. The grain medium w with g r a i n size s i z e ranges r a n g e s from from fine f i n e to t o medium i t h a few few c o u r s e grains g r a i n s scattered s c a t t e r e d throughout. throughout. course Most s a m p l e s are a r e vvery e r y friable friable Most samples w i t h calcite c a l c i t e and iron i r o n oxide o x i d e being b e i n g the t h e common cements. cements. with L o c a l wellwellLocal cemented beds b e d s have h a v e a high h i g h iron i r o n content c o n t e n t and in i n some areas a r e a s of intense cemented of intense a c t u r i n g the t h e Navajo N a v a j o is i s a quartzite. quartzite. f rracturing N e a r tthe h e top t o p of of tthe h e formation formation Near a peculiar p e c u l i a r red r e d speckling s p e c k l i n g is i s seen s e e n where w h e r e gray-white g r a y - w h i t e sandstone s a n d s t o n e has has c l u s t e r s of of pin p i n head-size h e a d - s i z e concentrations c o n c e n t r a t i o n s of of red r e d iron-coated i r o n - c o a t e d sand sand clusters g r a i n s which, w h i c h , except e x c e p t for f o r the t h e iron i r o n coating, c o a t i n g , are a r e no different different grains from the t h e rest r e s t of of the t h e sand s a n d grains. grains. from The Navajo N a v a j o varies v a r i e s in i n color c o l o r bboth o t h laterally l a t e r a l l y and and vertically. vertically. To the white t h e west w e s t in i n tthe h e vlhite W h i t e Cliffs C l i f f s most m o s t of of tthe h e formation f o r m a t i o n iis s w h i t e or or p a l e light l i g h t brown w i t h some darker d a r k e r beds b e d s nnear e a r the t h e bbase. ase. pale brovln with IIn n tthe h e Rush the N a v a j o is i s generally g e n e r a l l y a light-colored l i g h t - c o l o r e d sandstone sandstone w i t h large, large, Navajo with Beds the s c a t t e r e d areas a r e a s of of bright, b r i g h t , rust-orange r u s t - o r a n g e pa p a tches t c h e s that t h a t ccan a n bbe e sseen e e n for for . scattered miles. miles. of these t h e s e near n e a r tthe h e jjunction u n c t i o n of of tthe h e Paria Paria R i v e r and One of River Cottonwood Creek C r e e k form~ f o r m s an extremely e x t r e m e l y bright b r i g h t orange o r a n g e butte. butte. Cottonwood I n Shurtz Shurtz In Gorge the t h e lower l o w e r ppart a r t of of the t h e Navajo N a v a j o is i s a pale-orang p a l e - o r a n g ee ssandstone a n d s t o n e that that e r o d e s into i n t o a dark-brown, d a r k - b r o w n , de d e sert-varni s e r t - v a r n i sshed h e d cliff; c l i f f ; the t h e uupper p p e r ppart a r t is is erodes grayish w h i t e to t o pale p a l e orange o r a n g e and and grayish white d i s c u s s e d above. above. discussed commonly shows the t h e sspeckled p e c k l e d effect effect corrrm.only I n tthe h e southern s o u t h e r n hhalf a l f of of tthe h e .. map area a r e a near n e a r Catstairs Catstairs In t h e Navaj N a v a j o0 is i s commonly pale p a l e orange o r a n g e or o r light l i g h t ttan. an. Canyon, the Where t is is \·lhere iit b a d l y sheared s h e a r e d the the N a v a j o0 is i s leached l e a c h e d a monotonous m o n o t o n o u s cream cream white. white. badly Navaj On the t h e bbasis a s i s of of s eediment d i m e n t a r yy s t rructures u c t u r e s the t h e Navajo N a v a j o ccan a n be be d i v i d e d into i n t o t\vO two uni u n i ts. ts. w e r ' tunit r a i t has h a s 8 tto o 10 massive, massive, The l oower Figure 14.--Carmel-Navajo tongues in Catstalrs Canyon. F i g u r e 13.--Navajo 1 3 . — Wavajo Sandstone S a n d s t o n e in in C a t s t a i r s Canyon. Canyon. Figure Catstairs Figure 17.--Cannel and Entrada Formations in West Cove. Figure lS.--Paria River Member of Carmel Formation in West Cove. 68 horizontal ^ Q r i ^ o n t a l bbeds e d s with w i t h both b o t h lowl o w - and and hhigh-angle i g h - a n g l e cross c r o s s laminations. laminations. h o r i z o n t a l bedding b e d d i n g planes p l a n e s are a r e quite q u i t e distinct d i s t i n c t and and persistent. persistent. The horizontal r a n g e from from 8 tto o over o v e r 50 feet f e e t in i n thickness t h i c k n e s s and and contain c o n t a i n minor minor Beds range s i l t beds. beds. silt u n i t is i s 272 feet f e e t tthick h i c k in i n Shurtz S h u r t z Gorge Gorge w h e r e iit t forms forms The unit where s h e e r , overhanging o v e r h a n g i n g cliff c l i f f several s e v e r a l hundred h u n d r e d feet f e e t high. high. a sheer, a The upper Navajo u p p e r uunit n i t of of the the N a v a j o is i s a highly h i g h l y crossbedded crossbedded s a n d s t o n e ,.,ith w i t h no hhorizontal o r i z o n t a l bbedding e d d i n g planes. planes. sandstone The m a g n i t u d e and magnitude angle of of dip d i p vvaries; a r i e s ; some bbeds e d s contain c o n t a i n many closely c l o s e l y sspaced p a c e d high-angle high-angle augle c r o s s laminations l a m i n a t i o n s several s e v e r a l feet f e e t long l o n g that t h a t are a r e often o f t e n overturned, overturned, cross o r very v e r y steep steep w h i l e other o t h e r bbeds e d s are a r e composed u g e duneduneslumped, or while composed of of hhuge c r o s s laminations l a m i n a t i o n s 10 tto o over o v e r 100 feet f e e t long long w i t h amplitudes amplitudes formed cross with of tens t e n s of of feet. feet. of of these t h e s e are a r e also a l s o slumped s l u m p e d and and bbadly a d l y contorted. contorted. Some of of tne t h e snattered s h a t t e r e d nnature a t u r e of of most m o s t of of the the N a v a j o south s o u t h of the Because of Navajo of the P a r i a River, R i v e r , only o n l y in i n a few few places p l a c e s are a r e these t h e s e large l a r g e ccross r o s s laminations laminations Paria well exposed. exposed. well I n the t h e Glen G l e n Canyon, C a n y o n , Kanab, K a n a b , and Zion Z i o n aareas r e a s tthey h e y form form In s t r i k i n g features f e a t u r e s of of the t h e landscape. landscape. striking B e c a u s e of of the t h e llack a c k of bedding Because of bedding p l a n e s and severe s e v e r e faulting f a u l t i n g and jjointing o i n t i n g in i n the t h e Paria P a r i a aarea, r e a , no no planes a c c u r a t e measurement m e a s u r e m e n t is I s possible p o s s i b l e but b u t it it m u s t approach a p p r o a c h 1800 1800 feet; feet; accurate must g i v e s an apprOXL~ate approximate m e a s u r e m e n t of of 1700 1700 ffeet e e t ffor o r the the Wells (1960) gives measurement e n t i r e Navajo Navajo iin n House Rock V a l l e y several several m i l e s t oo tthe h e south. south. entire Valley miles Ever Navajo, Ever since s i n c e Gregory's G r e g o r y ' s first f i r s t studies s t u d i e s of of the the N a v a j o , it i t has has been classified c l a s s i f i e d pprimarily r i m a r i l y on the t h e basis b a s i s of of sedimentary s e d i m e n t a r y sstructures t r u c t u r e s aas s a desert-type d e s e r t - t y p e eolioan e o l i o a n sands s a n d s ttone. one. A fe,>l and foot few dinosaur d i n o s a u r skeletons s k e l e t o n s and foot prints p r i n t s hhave a v e also a l s o bbeen e e n cited c i t e d as a s evidence e v i d e n c e for f o r tthe h e continental c o n t i n e n t a l origin origin of °f the t h e Navajo. Navajo. 69 a v a j o is i s a wedge-shaped w e d g e - s h a p e d deposit d e p o s i t that t h a t tthickens h i c k e n s from from The N Navajo a feather f e a t h e r edge e d g e in i n ex e x ttreme r e m e eastern e a s t e r n Utah U t a h to t o over o v e r 2500 feet f e e t in i n the the a Zion Canyon area. area. This T h i s is i s essentially e s s e n t i a l l y a sand-filled s a n d - f i l l e d geosynclinal geosynclinal deposit. deposit. Parts Navajo, P a r t s of of tthe he N a v a j o , especially e s p e c i a l l y nnear e a r tthe h e base, b a s e , are a r e probably probably partly p a r t l y aqueous a q u e o u s in i n oorigin. rigin. In weerr 275 feet I n Shurtz S h u r t z Gorge tthe h e llO' ow f e e t of of the zhe Navajo Navajo is i s distinctly d i s t i n c t l y different d i f f e r e n t from from tthe h e overlying o v e r l y i n g part. part. The cross of tthe c r o s s llaminations a m i n a t i o n s aare r e smaller s m a l l e r scale, s c a l e , the t h e ddip i p of h e laminations laminations are a r e not n o t as a s steep, s t e e p , and and tthe h e festoon f e s t o o n ppattern a t t e r n is i s much lless e s s in i n evidence. evidence. The cross-laminated massive c r o s s - l a m i n a t e d sets s e t s are a r e iin n m a s s i v e bbeds e d s 5 to t o 30 ffeet e e t tthick. hick. is multiple i s possible p o s s i b l e tthat h a t these t h e s e hhorizontal o r i z o n t a l bbeds e d s are are m u l t i p l e paralle1paralleltruncation t r u n c a t i o n bbedding e d d i n g pplanes l a n e s (Stokes, ( S t o k e s , 1968). 1968). This T h i s structure s t r u c t u r e fforms o r m s in in sandy deserts water with d e s e r t s where w h e r e tthe he w a t e r table t a b l e rrises ises w i t h ssedimentation e d i m e n t a t i o n and occasionally o c c a s i o n a l l y rreaches e a c h e s tthe h e ssurface. urface. The wind The w i n d action a c t i o n rremoves e m o v e s the the dry sand water sand down tto o tthe he w a t e r table t a b l e and and an eero r o s iional o n a l truncation truncation bedding bedding plane p l a n e is i s formed f o r m e d ((Stokes, S t o k e s , 1968, 1 9 6 8 , pp.. 5512, 1 2 , fig. f i g . 1). 1). If I f the the water water table t a b l e ccontinues o n t i n u e s tto o rrise, i s e , shallow s h a l l o w llak a k ees s or o r pplayas l a y a s may form. form. Perhaps of ddepo Perhaps this t h i s is i s tthe h e environment e n v i r o n m e n t of e p oss ition i t i o n of of tthe h e lower l o w e r ppart a r t of of the Navaj Navajo0 in i n Shurt S h u r t zz Gorg G o r ge-e —ss imila1.i m i l a r bbedding e d d i n g is i s se s e een n near n e a r the t h e base base at Zion at Kanab and Z i o n Canyons. Canyons. The source i rmnense amount of sand s o u r c e area a r e a of of the t h e immense amount of s a n d in i n the the Navajo Navajo is i s ppartially a r t i a l l y in i n ddoubt. oubt. Pos P o s s ibly i b l y sands a n d - lladen a d e n stre s t r e aams m s ff lm'ling lowing south\olard southward from from tthe h e Canadian C a n a d i a n Shield S h i e l d tran t r a n sspported o r t e d tthe h e sand s a n d i nnto t o the the intermountain m t e r m o u n t a i n region. region. Then \·.rinds Then ppee rsistent r s i s t e n t nnorthT,;est o r t h w e s t e rly rly w i n d s b1eH blew the t h e sand sand off off tthe h e rriv i v ee rr fflood l o o d pl p l aa iin n and ddeposit e p o s i t eedd iit t in i n the the It It 70 e o s y n c l i n e on tthe h e western w e s t e r n ppart a r t of of tthe he C o l o r a d o Plateau. Plateau. geosyncline Colorado It of tthe I t iis s also a l s o ppossible o s s i b l e that t h a t at a t lleast e a s t some of h e sand s a n d was d e r i v e d from from pre-existing p r e - e x i s t i n g sandstones s a n d s t o n e s tthat hat w e r e bbeing e i n g gently gently derived were u p l i f t e d to t o tthe h e south s o u t h and and west. west. uplifted Fossils Navajo F o s s i l s are a r e extremely e x t r e m e l y rare r a r e iin n the the N a v a j o Sandstone S a n d s t o n e bbut u t if if the Late Kayenta L a t e Triassic T r i a s s i c aage g e aassignment s s i g n m e n t of of tthe he K a y e n t a is i s correct, c o r r e c t , then then because Kayenta Navajo because of of intertonguing i n t e r t o n g u i n g bbetween e t w e e n the the K a y e n t a and and tthe he N a v a j o and the Navajo Navajo Navajo and the t h e Carmel C a m e l ((~vith w i t h Jurassic J u r a s s i c fossils), f o s s i l s ) , tthe he N a v a j o is is both both Late L a t e Triassic T r i a s s i c and and Jurassic J u r a s s i c in i n aage g e with w i t h tthe h e syst~~atic s y s t e m a t i c boundary boundary hidden hidden in i n 1800 feet f e e t of of ccrossbedded r o s s b e d d e d uunfossiliferous n f o s s i l i f e r o u s sandstone. sandstone. The N Navajo Nugget Sandstone a v a j o iis s eequivalent q u i v a l e n t tto o tthe h e Nugget S a n d s t o n e of of northern northern Utah and w western Wyoming--this estern W y o m i n g — t h i s can c a n bbe e shown shown by iindirect n d i r e c t physical physical . correlation c o r r e l a t i o n and st:cat::i.graphic s t r a t i g r a p h i c position. position. The Nugget N u g g e t also a l s o thickens thickens to the though nnot t h e west w e s t though^ o t aas s regular r e g u l a r aass tthe h e Navajo. Navajo. { Indirectly Navajo I n d i r e c t l y the the N a v a j o hhas a s two eeconomic c o n o m i c vvalues--tourism a l u e s — t o u r i s m is is the largest Navajo l a r g e s t industry i n d u s t r y of of southern s o u t h e r n Utah U t a h and and tthe he N a v a j o iis s perhaps perhaps responsible r e s p o n s i b l e for f o r more m o r e ttourist o u r i s t attractions a t t r a c t i o n s tthan h a n any other o t h e r uunit; n i t ; ground ground water and tthe Navajo water is i s the t h e life l i f e of of ssouthern o u t h e r n Utah U t a h and he N a v a j o is i s its i t s most most important i m p o r t a n t aquifer. aquifer. ' Jurassic Svstem J u r a s s i c...- -",--System Tongues of the Navaj T o n g u e s of the N a v a j o0 and and Carmel Carmel Navajo and Carmel IIntertonguing n t e r t o n g u i n g of of tthe he N a v a j o Sandstone S a n d s t o n e and C a m e l Formation Formation has been been mapped mapped and and ddescribed e s c r i b e d iin n south-central s o u t h - c e n t r a l and and southwestern s o u t h w e s t e r n Utah. Utah. Examples of of tthis h i s condition c o n d i t i o n hhave a v e rrecent e c e n t lly y bbeen e e n discovered d i s c o v e r e d in i n the the Skutumpah-Paria-Lees Ferry SKutumpah-Paria-Lees F e r r y aal:eas r e a s (Phoenix, ( P h o e n i x , 1963, 1 9 6 3 , p. p . 32). 32), In I n Catstairs Catstairs 71 71 CaDyon of tthe Navajo by aa ssequence Canyon tthe h e uupper p p e r ppart a r t of he N a v a j o iis s iinterrupted n t e r r u p t e d by e q u e n c e of of iiDterca1ated n t e r c a l a t e d ,, hhorizontally o r i z o n t a l l y bbedded, e d d e d , ssandstone, a n d s t o n e , ssiltstone, i l t s t o n e , and mudstone. and mudstone. T h i s ssequence e q u e n c e iis s tthen h e n ooverlain v e r l a i n by a s s i v e , cross-stratified cross-stratified This by m massive, sandstone w h i c h iis s iin n tturn u r n ooverlain v e r l a i n by he C amel F ormation. sandstone which by tthe Carmel Formation. Regional Regional mapping hhas a s shown h a t tthe h e iintercalated, n t e r c a l a t e d , hhorizontally o r i z o n t a l l y bbedded e d d e d sequence sequence mapping shown tthat is a a ttongue o n g u e of he C amel F o m a t i o n tthat h a t originates o r i g i n a t e s nnear e a r Skutumpah Skutumpah 1s of tthe Carmel Formation T e r r a c e and and ppinches i n c h e s oout u t nnear ear L ees F e r r y ; tthe he m a s s i v e , cross-stratified cross-stratified Terrace Lees Ferry; massive, s a n d s t o n e iis s a ttongue o n g u e of he N a v a j o Sandstone S a n d s t o n e tthat h a t ooriginates r i g i n a t e s near near landstone of tthe Navajo Lees FFerry e r r y and and ppinches i n c h e s out o u t nnear e a r Skutumpah Skutumpah Terrace. Terrace. Bedding B e d d i n g plane plane u n c o n f o r m i t i e s eextend x t e n d ffor or m i l e s bbeyond e y o n d tthe h e ppinchouts i n c h o u t s of of bboth o t h tongues. tongues. unconformities miles In were I n 1963 shortly s h o r t l y after a f t e r tthe h e rrelationships elationships w e r e discovered, discovered, Phoenix Phoenix named tthe h e uunits n i t s the t h e Judd J u d d Hollow H o l l o w Tongue of of tthe h e Carmel C a m e l Formation Fomation and the Navajo t h e Thousand Thousand Pockets P o c k e t s T0ngue Tongue of of tthe he N a v a j o Sandstone. Sandstone. Judd Hollow TOrtgue Tongue Overlying Navajo O v e r l y i n g the t h e main m a i n mass m a s s of of the the N avajo Sandstone S a n d s t o n e in i n the the Paria P a r i a area a r e a with w i t h slight s l i g h t unconformity u n c o n f o m i t y is i s the t h e Judd J u d d HolICt; H o l l o w Tongue of of the the Carmel C a m e l Formation. Fomation. It I t is i s 99 feet f e e t thick t h i c k at a t Catstairs C a t s t a i r s Canyon Canyon but b u t thins thins irregularly i r r e g u l a r l y to t o the t h e north n o r t h along a l o n g the t h e Cockscomb and is i s less l e s s than t h a n 60 60 feet f e e t thick t h i c k at a t the t h e Paria P a r i a River R i v e r in i n Shurtz S h u r t z Gorge Gorge. The irregular irregular thickness t h i c k n e s s of of the t h e Judd J u d d Hollo\.; H o l l o w is i s due d u e partly p a r t l y to t o a massive m a s s i v e sandstone sandstone i n the t h e Judd J u d d HolICt; H o l l o w that t h a t changes c h a n g e s rapidly r a p i d l y in i n thickness t h i c k n e s s and may bed in d i s a p p e a r or o r merge m e r g e locally l o c a l l y with w i t h the t h e Thousand T h o u s a n d Pockets P o c k e t s Tongue (fig. ( f i g . 14). 14). disappear At Catstairs C a t s t a i r s Canyon three t h r e e lithologic l i t h o l o g i c units units m a r"ee present p r e s e n t in in the t h e Judd Hollm... Hollow. The lo\;errcost l o w e r m o s t 50 feet f e e t is i s a sequence s e q u e n c e of of red r e d ,, gray g r a y ,, g r a y i s h - b l u e , and light-buff, l i g h t - b u f f , sandy, s a n d y , fissil f i s s i l ee siltstone s i l t s t o n e and structurestructuregrayish-blue, l e s s mudstone. mudstone. less G e n e r a l l y the t h e blue b l u e and and gray g r a y bbeds e d s are a r e fine f i n e and and lack lack Generally a p p r e c i a b l e sand s a n d but b u t the t h e redbeds r e d b e d s are a r e quite q u i t e sandy. sandy. appreciable a r e copper c o p p e r stained. stained. beds are Many of of the the }lany e x t u r e , size, s i z e , shape, s h a p e , and color c o l o r of of the the The ttexture, q u a r t z grains g r a i n s show considerable c o n s i d e r a b l e range. range. quartz of the t h e mudstone m u d s t o n e and and Much of s i l t s t o n e weathers w e a t h e r s into i n t o chips c h i p s or o r irregular i r r e g u l a r lumps l u m p s many of of which w h i c h have have siltstone s h i n y surface s u r f a c e (due ( d u e partially p a r t i a l l y to t o gypsum). gypsum). a shiny of the t h e beds b e d s are are Most of q u i t e limy l i m y and further f u r t h e r north n o r t h limestones l i m e s t o n e s appear a p p e a r in i n this t h i s lower l o w e r unit. unit. quite S u b t l e color c o l o r banding b a n d i n g is i s present p r e s e n t in i n tthis h i s unit u n i t and individual i n d i v i d u a l beds b e d s can can Subtle t r a c e d for f o r miles. miles. be traced o o r l y preserved p r e s e r v e d pelecypods p e l e c y p o d s were w e r e found found Some ppoorly about 2 miles m i l e s north n o r t h of of U. S. Highway 89 in i n tthis h i s unit u n i t and although although about u n i d e n t i f i a b l e , are a r e pprobably r o b a b l y marine. marine. unidentifiable, Bedding ranges Bedding r a n g e s from from fissile f i s s i l e to t o massive m a s s i v e and and sedimentary sedimentary structures Havy bedding s t r u c t u r e s include i n c l u d e wavy b e d d i n g cc8JJsed a u s e d by ripple r i p p l e laminations, laminations, ripple r i p p l e marks, m a r k s , and and ppoorly o o r l y developed d e v e l o p e d current c u r r e n t lineation. lineation. The middle m i d d l e unit u n i t is i s a very v e r y mature m a t u r e cross-stratified c r o s s - s t r a t i f i e d quartz quartz s a n d s t o n e , grayish grayish w h i t e to t o ppale a l e orange o r a n g e in i n color; c o l o r ; it i t closely c l o s e l y resembles resembles sandstone, white t h e main main Navajo Navajo and Thousand Thousand Pockets P o c k e t s Tongue. Tongue. the T h i s uunit n i t is i s 29 feet feet This thick t h i c k at a t Catstairs C a t s t a i r s Canyon but b u t thins t h i n s and thickens t h i c k e n s irregularly i r r e g u l a r l y to t o the the n o r t h and apparently a p p a r e n t l y merges merges w i t h the t h e Thousand T h o u s a n d Pockets P o c k e t s Tongue. Tongue. north with m e d i a l sandstone s a n d s t o n e was pprobably r o b a b l y deposited d e p o s i t e d as a s an a n off·-shore o f f - s h o r e bar bar This medial i t s exact e x a c t relationship r e l a t i o n s h i p with w i t h tthe h e Thousand T h o u s a n d Pockets P o c k e t s Tongue is i s not not and its cleqr. clear. The uupper p p e r 20 feet f e e t of of the t h e Judd J u d d Hollow H o l l o w consists c o n s i s t s of of bright-red bright-red s i l t y shale s h a l e and mudstone m u d s t o n e similar s i m i l a r to t o the t h e llower o w e r uunit. nit. Silty T h i s unit u n i t thins thins This and thickens t h i c k e n s irregularly i r r e g u l a r l y along a l o n g the t h e backslope b a c k s l o p e of of tthe h e Cockscomb. Cockscomb. At p l a c e s it i t pinches p i n c h e s out o u t bbetvleen e t w e e n the t h e middle m i d d l e sr.ndstone s a n d s t o n e unit u n i t of of the t h e Judd Judd places 73 Holl° w Tongue and the t h e Thousand T h o u s a n d Pockets P o c k e t s Tongue. Tongue. e n t i r e Judd J u d d Hollow H o l l o w Tongue f o r m s a notch n o t c h bbetween e t w e e n two The entire Tongue forms massive sandstones s a n d s t o n e s on the t h e dipslope d i p s l o p e of of the t h e Cockscomb. Cockscomb. aassive jfrnnsand P o c k e t s Tongue ~ousartdPocketsTbrtgue T h o u s a n d Pockets P o c k e t s Tongue is i s similar s i m i l a r to t o tthe he m a i n Navajo. Navajo. The Thousand main I t consists c o n s i s t s of of finef i n e - to t o medium-grained, m e d i u m - g r a i n e d , vlell-sorted w e l l - s o r t e d qquartz u a r t z grains grains It a l m o s t no matrix. matrix. with almost u n i t is i s grayish g r a y i s h orange, o r a n g e , friable, friable, The unit cemented with w i t h calcite. calcite. and cemented T h o u s a n d Pockets P o c k e t s Tongue i s 230 feet The Thousand Tongue is 230 feet t h i c k at a t Catstairs C a t s t a i r s Canyon Canyon and appears a p p e a r s to t o maintain m a i n t a i n about a b o u t this this thick t h i c k n e s s throughout t h r o u g h o u t the t h e mapped mapped area. area. thickness The tongue t o n g u e cconsists o n s i s t s of three, of three, m a s s i v e , cross-alminated c r o s s - a l m i n a t e d sandstone s a n d s t o n e bbeds e d s separated s e p a r a t e d by distinct massive, by distinct bedding pplanes. lanes. bedding One of of these t h e s e bbedding e d d i n g pplanes l a n e s contains c o n t a i n s a channel c h a n n e l 10 10 f e e t deep filled f i l l e d with w i t h poorly p o o r l y sorted s o r t e d rred e d sandy s a n d y siltstone s i l t s t o n e similar s i m i l a r to to feet t h e Judd HollmV' H o l l o w Tongue and and overlying o v e r l y i n g Paria P a r i a River R i v e r Member the the Hember of of the Formation. Carmel Formation. c o n t a c t bbetween e t w e e n the t h e two ttongues o n g u e s shows cchanneling h a n n e l i n g with with The contact relief and some reworking. r e l i e f approaching a p p r o a c h i n g 2 feet f e e t and reworking. This T h i s unconformity unconformity passes main westward p a s s e s into i n t o the the m a i n mass m a s s of of Carmel and and continues continues w e s t w a r d for f o r many miles m i l e s (Thompson (Thompson and Stokes, S t o k e s , in i n press). press). gDepositional g £ g s i t i o n a l Enviror~ents Environments t h e deposition d e p o s i t i o n of of sand s a n d diminished, d i m i n i s h e d , marine m a r i n e sseas e a s returned returned As the to the t h e western w e s t e r n Colorado C o l o r a d o Plateau P l a t e a u and deposited d e p o s i t e d tthe h e Judd J u d d Hollow Hollow Tongue. Because from tthe west B e c a u s e tthe h e Judd J u d d Hollow H o l l o w Tongue originates o r i g i n a t e s from he w e s t and p i n c h e s out o u t in i n a sequence s e q u e n c e of of '·lell···sorl.:ed w e l l - s o r t e d sands s a n d s to t o tthe h e east, e a s t , the the pinches s o u r c e of of tthe h e poorly p o o r l y so:rted s o r t e d interealated i n t e r c a l a t e d siltstone s i l t s t o n e and and mudstone m u d s t o n e "laS was source 74 robably w estward. probably westward. T h i s iis s ffurther u r t h e r eevidence v i d e n c e of i g h l a n d in in This of a hhighland .t. L i- Arizona A r i z o n a and o u t h e r n Nevada h a t by a r l y JJurassic u r a s s i c had had western and ssouthern Nevada tthat by E Early west e ( p r n 1 formed bbetween and ppossibly westward of tthe Mogollon and Mesoformed e t w e e n and ossibly w e s t w a r d of he M o g o l l o n and Mesoc o r d i l l e r a n Highlands. Highlands. cordilleran The JJudd Hollow Tongue ccan The udd H o l l o w Tongue a n bbe e ddirectly i r e c t l y ttraced r a c e d iinto n t o the the main Formation and Thompson Thompson and and SStokes main Carmel Carmel F o r m a t i o n and t o k e s ((in i n ppress) r e s s ) propose propose names Kolob Kolob L Limestone Member and Crystal tthe h e formal f o r m a l names i m e s t o n e Member and C r y s t a l Creek C r e e k Member Member for of tthe main Carmel westward for tthe h e uunits n i t s of he m ain C a r m e l tthat h a t aare re w e s t w a r d eequivalents q u i v a l e n t s of of the Judd Hollow Hollow T Tongue. the Judd ongue. The Member contains The Kolob Kolob Limestone L i m e s t o n e Member c o n t a i n s aa definite (Thompson and d e f i n i t e Bajocian B a j o c i a n (Middle ( M i d d l e JJurassic) u r a s s i c ) fauna f a u n a (Thompson and Stokes, Stokes, in i n press). press), Sand Sand ddeposition e p o s i t i o n did d i d nnot o t terminate t e r m i n a t e immediately--the i m m e d i a t e l y — t h e "great "great sand moved 'Vlestward sand ppile" i l e " moved w e s t w a r d across a c r o s s the t h e marine m a r i n e sediments s e d i m e n t s jjust u s t deposited deposited by by the t h e Judd Judd Hollow H o l l o w seas. seas. Several minor Several m i n o r intertonguings i n t e r t o n g u i n g s apparently apparently took took place p l a c e between b e t w e e n the t h e main m a i n tongues t o n g u e s as a s shown shown by by the t h e Catstairs Catstairs section. section. The The Thousand T h o u s a n d Pockets P o c k e t s Tongue Tongue seems seems to t o represent r e p r e s e n t aa complex complex beach beach deposit--both d e p o s i t — b o t h shallow s h a l l o w marine m a r i n e and and eolian. eolian. The The distinct distinct diastems d i a s t e m s are a r e most m o s t likely l i k e l y periods p e r i o d s of of minor m i n o r erosion. erosion. The The erosion erosion was was st~'ong s t r o n g enough e n o u g h to t o prcduce p r o d u c e channels c h a n n e l s that t h a t W2re w e r e later l a t e r filled f i l l e d 'Vlith with silts s i l t s and and shales s h a l e s deposite d e p o s i t e dd on on aa tidal t i d a l flat. flat. Fin~ F i n a lly l l y the t h e littoral littoral deposits d e p o s i t s of of the t h e Ca C arr mel m e l Formation F o r m a t i o n cove c o v e red r e d the t h e entire e n t i r e area. area. San Rafael R a f a e l Group Group The San Rafael R a f a e l Group \vas was described d e s c r i b e d and named for f o r exposures exposures i n the t h e San Rafael R a f a e l Swell. Swell. in F o r m a t i o n s at a t the t h e type t y p e locality l o c a l i t y include include Formations in i n asscending a s s c e n d i n g order o r d e r the t h e Carme C a r m ell Form F o r mation, a t i o n , the t h e Entrada E n t r a d a Sandstone, S a n d s t o n e , the the '75 75 C u r t i s Formation, F o r m a t i o n , and and tthe h e Summerville S u m m e r v i l l e Formation. Formation. curtiS Only tthe h e Entrada Entrada Only d Carmel Formations F o r m a t i o n s are a r e present p r e s e n t in i n the t h e Paria P a r i a area. area. and a n Both formations marginal Both f o r m a t i o n s were w e r e deposited d e p o s i t e d in i n and m a r g i n a l tto o sseas e a s that that extended-down from from tthe h e Arctic A r c t i c region--no r e g i o n — n o known connection c o n n e c t i o n existed existed extended-down (in Ocean oorr Gulf Gulf of ( i n the t h e Western W e s t e r n Interior) I n t e r i o r ) with w i t h either e i t h e r the t h e Pacific P a c i f i c Ocean of Mexico. R a f a e l time t i m e the t h e Colorado C o l o r a d o Plateau P l a t e a u was surrounded surrounded By San Rafael t h r e e sides s i d e s by hhighlands i g h l a n d s with w i t h only o n l y the t h e north n o r t h being b e i n g oopen. pen. on three To t h e east e a s t were w e r e the t h e low l o w hills h i l l s of of the t h e Uncompahgre H i g h l a n d s , tto o the the the Uncompahgre Highlands, south the t h e Mogollon M o g o l l o n Highlands, H i g h l a n d s , tto o the the w e s t tthe h e complex complex Mesocordilleran Mesocordilleran south west H i g h l a n d s , and bbridging r i d g i n g the t h e gap g a p bbetween e t w e e n the t h e latter l a t t e r ttwo, w o , a new Highlands, h i g h l a n d sometimes s o m e t i m e s referred r e f e r r e d to t o as a s Mojavia M o j a v i a or o r tthe he N a v a j o Highlands Highlands highland Navajo ( L e s s e n t i m e , 1969, 1 9 6 9 , p. p . 107). 107). (Lessentime, Carmel C a r m e l Formation Formation The Carmel Formation Reeside Carmel F o r m a t i o n was na~ed named bby y Gilluly G i l l u l y and and R e e s i d e (1926) (1926) f i r s t described d e s c r i b e d by b y Gregory G r e g o r y and Moore (1931, ( 1 9 3 1 , p. p . 69) o r rocks rocks and first 69) ffor exposed Mt. exposed nnear ear M t . Carmel, C a r m e l , Utah. Utah. It I t is i s the t h e only o n l y member member of of tthe h e San Rafael with Swell R a f a e l Group w i t h a ttype y p e section s e c t i o n not n o t in i n the t h e San Rafael Rafael S w e l l area. area. The Carmel widely much of Carmel Formation F o r m a t i o n is is w i d e l y exposed e x p o s e d throughout t h r o u g h o u t much of the t h e Colorado C o l o r a d o Plateau P l a t e a u 'vest w e s t of of the t h e Four F o u r Corners C o r n e r s rregion. egion. vJest of of the West the Green Green and Colorado C o l o r a d o Rivers R i v e r s the t h e Carmel Carmel. increases i n c r e a s e s in i n tthickness h i c k n e s s and lim,estone l i m e s t o n e appears a p p e a r s in i n the t h e lower l o w e r part. part. To tthe and ssoutheast h e south s o u t h and o u t h e a s t sand sand i n c r e a s e s and in i n the t h e Black B l a c k Mesa Basin B a s i n area a r e a of of Arizona, A r i z o n a , tthe h e Carmel C a r m e l is is increases i n s e p a r a b l e from from the t h e overlying o v e r l y i n g Entrada. Entrada. inseparable 76 Carmel of of southwestern southwestern U t a h hhas a s hhad a d a long l o n g history h i s t o r y of of The Carmel Utah miscorrelation. miscorrelation. P a r t s of of iit t hhave a v e bbeen e e n considered c o n s i d e r e d Entrada, E n t r a d a , Summerville, Summerville, Parts C u r t i s , and M o r r i s o n equivalents. equivalents. curtis, Horrison The eentire n t i r e history h i s t o r y of of tthe h e Carmel Carmel m i s i n t e r p r e t a t i o n is i s summed up by S t o k e s (in ( i n press), press), misinterpretation by Thompson Thompson and and Stokes p r o p o s e and name new s u g g e s t iimproved m p r o v e d correlations. correlations. who propose nev; members members and suggest a b l e to t o verify v e r i f y many of of these t h e s e correlations c o r r e l a t i o n s and the t h e new terminology terminology I was able i s used used in i n this t h i s paper. paper. is of tthe he m o s t distinctive d i s t i n c t i v e and o r m a t i o n s in i n the the One of most and complex complex fformations a r e a , the t h e Carmel f o r m s cliffs, c l i f f s , ledges, l e d g e s , hhogbacks, o g b a c k s , rounded r o u n d e d valleys, valleys, area, Carmel forms s l o p e s , and badlands b a d l a n d s bbetween e t w e e n tthe h e dipslope d i p s l o p e of he T h o u s a n d Pockets Pockets slopes, of tthe Thousand h e cliff-forming c l i f f - f o r m i n g lower l o w e r Entrada E n t r a d a Sandstone S a n d s t o n e ((fig. f i g . 3). 3). Tongue and tthe The e n t i r e formation f o r m a t i o n iis s ccompletely o m p l e t e l y exposed e x p o s e d iin n West h e r e iit t was entire West Cove w where measured and studied s t u d i e d in i n detail. detail. measured S e v e r a l other o t h e r exposures e x p o s u r e s between between Several West Cove and the the P a r i a River R i v e r were w e r e studied s t u d i e d also. also. Paria Paria The Carmel C a r m e l Formation F o r m a t i o n in i n tthe he P a r i a aarea r e a is i s entirely e n t i r e l y clastic clastic (Judd Hollow Tongue eexcepted) xcepted) w h i c h is i s in in m a r k e d contrast c o n t r a s t tto o the the (Judd Hollow Tongue which marked type section Ut. miles west, where s e c t i o n nnear ear M t . Carmel, C a r m e l , 40 m i l e s tto o tthe he w est, w h e r e limestone limestone comprises comprises a llarge a r g e part p a r t of of tthe h e formation. formation. In I n general, g e n e r a l , limestone l i m e s t o n e is is restricted r e s t r i c t e d to t o the t h e 10\.;er l o w e r ppart a r t of of the t h e formation f o r m a t i o n and increases i n c r e a s e s in in thickness of tthe Paria t h i c k n e s s and purity p u r i t y tto o the t h e north n o r t h and west w e s t of he P a r i a area. area. 1\';0 Two main compose the· Paria wain lithologies l i t h o l o g i e s compose t h e Carmel C a r m e l Fonmation F o r m a t i o n iin n the the P a r i a area. area. The first mature and the f i r s t is I s a vhite, w h i t e , well-sorted, well-sorted, m a t u r e sandstone s a n d s t o n e and t h e second second i s a red, r e d , poorly p o o r l y sorted, s o r t e d , sandy s a n d y tto o . clayey c l a y e y siltstone. siltstone. is comprise 50-60 5 0 - 6 0 ppercent e r c e n t of of tthe h e ttotal o t a l formation. formation. Comprise The rred e d units units T h e s e two contrasting contrasting These i i t h o l o g l e s ggive i v e much of h e Cannel C a r m e l a "candy " c a n d y call.e c a n e "·-striped " - s t r i p e d appearance. appearance, lithologies of tthe 77 The Carmel Formation Carmel F o r m a t i o n of of tthe h e Paria P a r i a area a r e a iis s ddivisible i v i s i b l e into i n t o three three d i s t i n c t uunits, n i t s , two of of w h i c h are a r e formal f o r m a l members members and and the t h e third t h i r d an an distinct which i n f o r m a l ffacies. acies. informal T h e s e are, a r e , in i n assending a s s e n d i n g order, o r d e r , tthe h e Paria P a r i a River River These Member, the t h e white w h i t e sandstone s a n d s t o n e facies, f a c i e s , and and tthe he W i n s o r Member. Winsor The t o t a l Carmel Carmel in i n West Cove is i s 6621 2 1 feet f e e t thick. thick. total P a r i a _ River R i v e r_______ Paria Member The P aria R i v e r Member (Thompson S t o k e s , in i n ppress) r e s s ) was was Paria River (Thompson and and Stokes, f o r exposures e x p o s u r e s nnear e a r tthe h e Paria P a r i a River R i v e r about a b o u t 12 m i l e s nnorth o r t h of of the the named for miles t o w n s i t e of of Paria. Paria. townsite A l t e r n a t i n g hard h a r d and soft s o f t strata s t r a t a appear a p p e a r in in Alternating h o g b a c k s , dips1opes, d i p s l o p e s , and 1mv low hhills i l l s and and cliffs. cliffs. hogbacks, I n tthe h e area a r e a studied studied In t h e Paria Paria R i v e r Member d i p s aatt angles a n g l e s from e g r e e s tto o over o v e r 45 the River Member dips from 30 ddegrees d e g r e e s bbut u t tto o tthe h e east e a s t and and nnorth o r t h where w h e r e the t h e uunit n i t iis s nnearly e a r l y horizontal horizontal degrees i t forms forms bbenches, e n c h e s , low e s a s , and and 1edgy l e d g y ccliffs. liffs. it low m mesas, The Paria P a r i a River River Member is i s 218 feet f e e t tthick h i c k in i n West West Cove bbut u t this t h i s thickness t h i c k n e s s varies varies along tthe h e Cockscomb Cockscomb due d u e tto o iintertonguing n t e r t o n g u i n g and and grading grading w i t h the t h e overlying overlying along ~vith w h i t e sandstone s a n d s t o n e facies. facies. white Three T h r e e complexly c o m p l e x l y iinterbedded n t e r b e d d e d lithologies l i t h o l o g i e s ddominate o m i n a t e the t h e Paria Paria R i v e r Member--a Member—a red, r e d , poorly p o o r l y sorted s o r t e d sandstone, s a n d s t o n e , a rred e d siltstone s i l t s t o n e and and River lnUdstone mudstone sequence, s e q u e n c e , and white w h i t e tto o grayish-orange g r a y i s h - o r a n g e eexx ttremely r e m e l y mature mature sar-dstone s a n d s t o n e (fig. ( f i g . 15). 15). fine matrix. f i n e silt silt m atrix. The red r e d sandstone s a n d s t o n e is i s arkosic a r k o s i c with w i t h an abundant abundant Grain G r a i n size, s i z e , shape, s h a p e , color, c o l o r , ttexture, e x t u r e , and and roundness roundness vary with v a r y considerably c o n s i d e r a b l y and tthe h e uunit n i t is i s ccemented, emented, w i t h iron i r o n and and calcite. calcite, ihe rred e d silt, s i l t , shale s h a l e and and cl c l aaystone y s t o n e are a r e tthe h e deepest d e e p e s t cc.olored o l o r e d red r e d rocks rocks The °f the t h e area. area. of The C armel F o m a t i o n on tthe he C o l o r a d o Plateau P l a t e a u averages averages Ca-!:.-mel Formation Colorado o e r c e n t iron i r o n (Newman, 1962, 1 9 6 2 , p. p . 413); 4 1 3 ) ; tthis h i s is i s the t h e highest h i g h e s t content content 1.0n percent of any Mesozoic M e s o z o i c formation, f o r m a t i o n , so s o these t h e s e dark d a r k rred e d rrocks o c k s of of the t h e Paria Paria of a r e a probably p r o b a b l y exceed e x c e e d that t h a t figure. figure. area s i l t s t o n e is i s similar s i m i l a r in in The siltstone c o m p o s i t i o n to t o the t h e red r e d sandstone s a n d s t o n e and is i s also a l s o vvery e r y poorly p o o r l y sorted. sorted. composition The s i l t s t o n e and mudstone m u d s t o n e are a r e generally g e n e r a l l y fissile f i s s i l e and weather w e a t h e r into into siltstone c h i p s with w i t h the t h e latter l a t t e r hhaving a v i n g a shiny s h i n y waxy surface s u r f a c e with w i t h black b l a c k mica m i c a on on chips t h e bedding b e d d i n g pplanes. lanes. the Gypsum (but ( b u t no calcite) c a l c i t e ) is i s common in i n these these f i n e - g r a i n e d sediments. sediments. fine-grained B e d d i n g planes p l a n e s are a r e often o f t e n striated s t r i a t e d or o r pock pock Bedding u t this t h i s is i s probably p r o b a b l y due tto o removal r e m o v a l of of salt s a l t and gypsum crystals. crystals marked bbut w h i t e to t o grayish-orange g r a y i s h - o r a n g e sandstone s a n d s t o n e is i s the the m o s t mature mature The white most rock type t y p e of of all a l l the t h e uunits n i t s studied. studied. rock T h e s e sandstones s a n d s t o n e s contain c o n t a i n clear, clear, These f r o s t e d , well-sorted, w e l l - s o r t e d , rounded r o u n d e d quartz q u a r t z grains g r a i n s with w i t h almost a l m o s t no matrix matrix frosted, or acce$sory accessory m inerals. or minerals. of tth~ h e units u n i t s are a r e n2crly n e a r l y ,;"r.ite w h i t e but b u t others others Some of b e e n partially p a r t i a l l y stained s t a i n e d rred e d by ground g r o u n d water. water. have been Other O t h e r less l e s s common but b u t often o f t e n laterally l a t e r a l l y persistent p e r s i s t e n t lithologies lithologies :I.nclude i n c l u d e a series s e r i e s of of vvery e r y limy l i m y gray g r a y sandstone s a n d s t o n e beds b e d s interbedded I n t e r b e d d e d with with bentonitic b e n t o n i t i c shale, s h a l e , a very v e r y distinct d i s t i n c t unconsolidated u n c o n s o l i d a t e d chert c h e r t gravel, g r a v e l , and and conglomeratic c o n g l o m e r a t i c sandstone. sandstone. The limy l i m y sandstone s a n d s t o n e pprobably r o b a b l y represents represents the t h e easternmost e a s t e r n m o s t lime l i m e ddeposit e p o s i t of of the t h e Carmel Carmel sea. sea. The chert c h e r t gravel gravel is w·ith i s unique u n i q u e and along along w i t h the t h e conglomeratic c o n g l o m e r a t i c sandstone s a n d s t o n e (abundant (abundant near n e a r the t h e ttop o p of of the t h e member) rreflects e f l e c t s a local, l o c a l , short-lived s h o r t - l i v e d source source area, a r e a , probably p r o b a b l y to t o tthe h e south. south. The Paria River Paria R i v e r Mernber Member contains c o n t a i n s an a n abnormally a b n o r m a l l y large l a r g e variety variety of of primary p r i m a r y sedimentary s e d i m e n t a r y structures. structures. Bedding B e d d i n g thickness t h i c k n e s s rranges a n g e s from from f i s s i l e to t o massive; m a s s i v e ; cont.orted c o n t o r t e d bbedding, e d d i n g , slumping, s l u m p i n g , and and flaille f l a m e structure structure fisSile a r e common in i n the t h e silty s i l t y sandstones. sandstones. are C l a s t i c d.ykes, d y k e s , characteristic c h a r a c t e r i s t i c of of Clastic '79 79 the Carmel, mapped aarea 15 m miles he C a r m e l , aare r e ggenerally e n e r a l l y ssmall m a l l iin n tthe h e mapped r e a bbut u t 15 i l e s to to t Kodachrome FFlat tthe h e nnorth o r t h iin n Kodachrome l a t sseveral e v e r a l llarge a r g e oones n e s ccan a n bbe e sseen e e n from from the rroad. the oad. The ppure The u r e ssandstone a n d s t o n e iis s ggenerally e n e r a l l y ccross r o s s llaminated a m i n a t e d (both (both hicrh n g l e ) bbut u t some e d s show r o s s llaminations a m i n a t i o n s aat t all. all. high and and low low aangle) some bbeds show no no ccross ManY of of tthe weather Many h e ccoarse o a r s e ssiltstones iltstones w e a t h e r iinto n t o eexfoliated x f o l i a t e d humps; humps; c o n t o r t e d bbedding e d d i n g iis s uusually s u a l l y aassociated ssociated w i t h tthese h e s e bbeds. eds. contorted with R a i n drop drop Rain pprints r i n t s and ipple m a r k s aare r e common on h e ffine i n e ssiltstones i l t s t o n e s aas s is is and rripple marks on tthe ccurrent u r r e n t pparting a r t i n g llineation. ineation. Many h e bbeds, e d s , rregardless e g a r d l e s s of grain Hany of of tthe of grain s i z e , hhave a v e aabundant b u n d a n t ddiastems, i a s t e r n s , ccut u t and i l l cchannels hannels w i t h coarse coarse size, and ffill with b a s a l ssands, a n d s , and e d d i n g pplane l a n e ddiastems. iastems. basal and bbedding B e n t o n i t e , common iin n the the Bentonite, c l a y s t o n e s , causes c a u s e s a ""popcorn p o p c o r n surface" s u r f a c e " tto o develop. develop. claystones, About feet About 40 feet below tthe h e top t o p of of tthe he P aria R i v e r Member a w h i t e ssandstone a n d s t o n e bed bed below Paria River white c o n t a i n s abundant a b u n d a n t lload oad contains o r flute f l u t e ccasts. asts. or T h i s particu~ar p a r t i c u l a r tced e d lS is This p r e s e n t at a t bboth o t h the t h e north n o r t h and s o u t h ends e n d s of h e map area a r e a and and conse·conse­ present and south of tthe q u e n t l y is i s more than t h a n jjust u s t a local l o c a l lens l e n s or o r channel. channel. quently The Paria P a r i a River R i v e r Member was apparently a p p a r e n t l y called c a l l e d the t h e Curtis C u r t i s by Gregory Gregory (1950), ( 1 9 5 0 ) , but b u t Wright W r i g h t and Dickey D i c k e y (1963), ( 1 9 6 3 ) , Cashion C a s h i o n (1967), ( 1 9 6 7 ) , and and Thompson and Stokes S t o k e s (in ( i n press) p r e s s ) show conclusively c o n c l u s i v e l y that t h a t it i t belongs b e l o n g s in in the t h e Carmel Formation. Formation. Most of of the t h e Carm C a r mel e l Formation F o r m a t i o n of of the t h e Lake L a k e Powell Powell area a r e a is i s equivalent e q u i v a l e n t to t o the t h e Paria P a r i a River R i v e r Member. Member. White sanustonefacies sandstone facies w h i t e s ands a n d s ttone o n e facies f a c i e s of of the t h e Carmel C a r m e l Formation F o r m a t i o n as a s defined defined The white in i n this t h i s paper p a p e r lies l i e s between b e t w e e n and interfingers i n t e r f i n g e r s and and grades g r a d e s ,'lith w i t h both both the t h e Paria P a r i a River R i v e r and HillSO~ W i n s o r Hembers Members and for f o r this t h i s reason r e a s o n is i s not not -- included i n c l u d e d with w i t h either. either. l.Jhite White sandstcne s a n d s t o n e increases I n c r e a s e s in i n the t h e Care-el C a r m e l in i n aa 80 80 Coal Canyon nnear Tuba C City, Arizona s outherly u t h e r l y ddirection i r e c t i o n uuntil n t i l aat t C o a l Canyon e a r Tuba ity, . A r i z o n a almost almost 80 all of tthe Carmel iis white a l l of h e Carmel s w h i t e ssandstone a n d s t o n e tthat h a t iis s ddifficult i f f i c u l t tto o separate separate from Entrada Sandstone. from tthe he E ntrada S andstone. The w white The h i t e ssandstone a n d s t o n e ffacies a c i e s iis s possibly possibly Carmel of of C Coal Canyon and and the ppartially a r t i a l l y oor r 1Yholly w h o l l y eequivalent q u i v a l e n t tto o tthe h e Carmel o a l Canyon the Black a s i n area. area. Black Mesa Mesa B Basin white West Cove The w h i t e sandstone s a n d s t o n e ffacies a c i e s iis s 97 ffeet e e t tthick h i c k aat t "West but Paria River. but tthins h i n s tto o less l e s s tthan h a n 40 feet f e e t nnear e a r tthe he P aria R iver. IIt t ccrops r o p s out out along tthe h e bback a c k of h e Cockscomb o n t i n u e s ssouthward o u t h w a r d aaround r o u n d East East along of tthe Cockscomb and and ccontinues Cove. Along tthe h e Cockscomb t forms f o r m s rrounded, o u n d e d , hhumped, u m p e d , hhogbacks o g b a c k s and and Along Cockscomb iit i s generally g e n e r a l l y covered c o v e r e d by a l l u v i u m iin n West Cove. is by alluvium West Cove. i t is i s flat-lying f l a t - l y i n g it i t forms f o r m s sheer s h e e r cliffs. cliffs. it In E a s t Cove where In East Cove where i w h i t e sandstone s a n d s t o n e facies f a c i e s is i s texturally texturally m a t u r e and cross The white mature and cross stratified. stratified. I t displays d i s p l a y s low-angle l o w - a n g l e cross c r o s s stratification s t r a t i f i c a t i o n aatt the the It i g h - a n g l e cross c r o s s stratification s t r a t i f i c a t i o n at a t the t h e ttop--the o p — t h e significance significance base and hhigh-angle w i l l be b e discussed d i s c u s s e d later. later. will N e a r U. S. High,.,ay Highway 89 no silt s i l t is i s ppresent r e s e n t in in Near t h e facies; f a c i e s ; in i n the t h e north n o r t h part p a r t of of West Cove one o n e thin t h i n rred e d siltstone siltstone the i s present p r e s e n t near n e a r the t h e base; b a s e ; at a t the t h e Paria P a r i a River R i v e r many silt s i l t beds b e d s are are is p r e s e n t and the t h e reco8nizable r e c o g n i z a b l e facies f a c i e s is i s l ee sss s than t h a n 40 feet f e e t tthick. hick. present The The t h i c k n e s s of of the t h e Ca Carmel F o r m a t i o n as a s a whole w h o l e increases i n c r e a s e s to t o the t h e north north thickness r mel Formation so the t h e '"hite w h i t e sandstone s a n d s t o n e facies f a c i e s merely m e r e l y grade g r a d e s into i n t o the t h e Paria P a r i a River River i n that t h a t direction d i r e c t i o n (fig. ( f i g . 16). 16). and Winsor Members in w h i t e sands s a n d s ttone o n e facies f a c i e s is i s "leakly w e a k l y cemented c e m e n t e d ,.,ith w i t h calcite. calcite. The white i s very v e r y fine f i n e grained--some g r a i n e d — s o m e bed b e d s are a r e almost a l m o s t siltstone. siltstone. The sand is l i t h o l o g y is i s common in i n the t h e Entrada E n t r a d a Sandstone. Sandstone. lithology This This The term Winsor term W i n s o r was first f i r s t giv~n g i v e n formational f o r m a t i o n a l status s t a t u s by by Gregory (1948, ( 1 9 4 8 , pp.. 235; 2 3 5 ; 1950, 1 9 5 0 , p. p . 98). 98). Gregory U n f o r t u n a t e l y , because b e c a u s e the the Unfortunately, P a r i a River R i v e r Member was the t h e considered c o n s i d e r e d to t o be b e the t h e Curtis, C u r t i s , the t h e Winsor Winsor Paria s thought t h o u g h t to t o bbe e equivalent e q u i v a l e n t to t o the t h e uppermost u p p e r m o s t San Rafael R a f a e l Group and and waas w perhaps part p a r t of of the t h e Morrison M o r r i s o n Formation. Formation. perhaps f u r t h e r complicate complicate To further a t t e r s , in i n an easterly e a s t e r l y direction d i r e c t i o n along a l o n g tthe h e Sub-Dakota S u b - D a k o t a unconformity unconformity matters, ( t o be discussed d i s c u s s e d in i n ddetail e t a i l later) l a t e r ) successively s u c c e s s i v e l y younger y o u n g e r formations formations (to are exposed exposed and and they they w e r e also a l s o thought t h o u g h t tto o be b e part p a r t of of the t h e Winsor W i n s o r by by are were e a r l y workers--and w o r k e r s — a n d thus t h u s all a l l post p o s t Curtis. Curtis. early Thompson and and Stokes S t o k e s (in (in Thompson p r e s s ) discuss d i s c u s s this t h i s problem p r o b l e m in i n detail d e t a i l and and ttheir h e i r solution, s o l u t i o n , which w h i c h this this press) paper follows, f o l l o w s , appears a p p e a r s tto o clarify c l a r i f y the t h e matter. matter. paper s u m m a r i z e their their To summari.ze f i n d i n g s , at a t Mt. Mt, Carmel C a r m e l tthe h e Winsor W i n s o r is i s overlain o v e r l a i n unconformably u n c o n f o r m a b l y by by findings, t h e Dakota Dakota F o r m a t i o n , bbut u t successively s u c c e s s i v e l y eastward e a s t w a r d a yyounger o u n g e r member member the Formation, of the t h e Carmel Carmel appears, a p p e a r s , one bby y one tthree h r e e members of of the t h e Entrada Entrada of a r e exposed,near exposed, n e a r Henrieville H e n r i e v i l l e a newly n e w l y proposed p r o p o s e d fonnation, f o r m a t i o n , the the are H e n r i e v i l l e Sandstone S a n d s t o n e is i s present, p r e s e n t , and finally f i n a l l y between b e t w e e n the t h e Paria P a r i a River River Henrieville Wahweap t h e Morrison Morrison F o r m a t i o n appears a p p e a r s below b e l o w the t h e Sub-Dakota Sub-Dakota and Wah~" eap the Formation unconformity. unconformity. A l l t hhe e sse e uni u n i ts t s ex e x ce c e pptt the the M r r i s oon n w e r e until until All Hoorris were r e c e n t l y included i n c l u d e d in i n the t h e lVinsor W i n s o r For F o rmation. mation. recently The Hinsor member of W i n s o r was reduced r e d u c e d in i n rrank a n k to t o a member of the t h e Carmel Carmel Formation by Cashion worked F o r m a t i o n by C a s h i o n (1967, ( 1 9 6 7 , pp.. JJ5) 5 ) and its i t s stratigraphy stratigraphy w o r k e d out out S t o k e s (in ( i n press). press). by Thompson and Stoke N N CANNONVILLE CANNONVILLE -=--==---::-:_.' : ' _.' ~- -. ' . ' . _.' - -- :~~• ._ ~ MOUTH COTTONWOOD CREEK s PARIA PLATEAU WEST COVE MOUTH COTTONWOOD continental eolian fluvial deltaic tacustrine 600 Ft 400 rv'lixed eolian eon an beach beach tldal tidal deltaic deltaic Marine Marine & & t'd-I t iI d ~ a l flat flat 200 a ~I-~':---"""-2 4 6' Mi GYPSUM ~ from Thompson F i0g__ u_ r e 16 l 6• .--Sand~ S . n d - .i I t r e l a t i o n s of C a r t e l a n d E n t r a d a Fonnations P o r t i o n s as a s shown shown along a l o n g East B u t Ka'b K a1i bab a b Monocl' M o n o c lne. line. Fio-ure ., of'; Cannel .and J~nt rada and ... c:: tcl-tes '~i oa.' 1. f led . - fro", Sl.lompscn 11 t r e.a ' tions • , In press ) (( M o d i f i e d 8 and S t o k e s , in press) 83 In Winsor I n the t h e Paria P a r i a area a r e a the the W i n s o r Member of of the t h e Carmel C a r m e l Formation Formation d i s t i n c t i v e , badland-forming b a d l a n d - f o r m i n g unit u n i t tthat h a t uunderlies n d e r l i e s the t h e Entrada Entrada 1s a distinctive, Sandstone w i t h apparent a p p a r e n t conformity. conformity. Sandstone with I t is i s 309 feet f e e t thick t h i c k in i n West West It u t thickens t h i c k e n s somevlhat somewhat to t o tthe h e north n o r t h due to t o the t h e pinching p i n c h i n g out out Cove bbut f the t h e underlying underlying w h i t e sandstone s a n d s t o n e facies f a c i e s (fig. ( f i g . 16). 16). of white 0 The Winsor Winsor dominates the t h e scenery s c e n e r y at a t West Cove where w h e r e it i t forms f o r m s a "candy " c a n d y cane"cane"dominates s t r i p e d bbadland a d l a n d below b e l o w the the w h i t e , vertical v e r t i c a l Entrada E n t r a d a Cliff C l i f f but b u t north north striped ,..hite, of West Cove where w h e r e it i t averages a v e r a g e s a 45 degree d e g r e e dip, d i p , it i t forms f o r m s a striped striped of s t r i k e valley v a l l e y along a l o n g the t h e back b a c k of of the t h e Cockscomb Cockscomb (fig. ( f i g . 17). 17). strike Farther Farther south in i n West Cove and East E a s t Cove tthe h e sand s a n d content c o n t e n t increases i n c r e a s e s and the the south forms cliffs c l i f f s and buttes b u t t e s such s u c h as a s Johnson J o h n s o n Store S t o r e Butte. Butte. Winsor forms The lithology l i t h o l o g y of of the t h e Winsor W i n s o r Member is i s complex complex although a l t h o u g h not not as much as Hember. a s that t h a t of of tthe h e Paria P a r i a River R i v e r Member. The main m a i n difference difference between Winsor between the t h e Paria P a r i a River R i v e r and the the W i n s o r Members is i s that t h a t tthe h e Winsor Winsor c o n t a i n s abundant a b u n d a n t bentonite. bentonite. contains i n s o r consists c o n s i s t s of of interbedded interbedded The W Winsor sandstone, mudstone, minor sandstone, m u d s t o n e , and and siltstone s i l t s t o n e with w i t h local local m i n o r conglomerate conglomerate associated a s s o c i a t e d with w i t h channel c h a n n e l structures. structures. The sandstones s a n d s t o n e s are a r e light light orange orange or o r light l i g h t bbro,vn r o w n and are a r e similar s i m i l a r to t o the t h e other o t h e r sandstones s a n d s t o n e s of the Carmel Carmel except e x c e p t that t h a t they t h e y contain c o n t a i n more silt s i l t matrix. matrix. The sorting s o r t i n g is i f a i r , the t h e grains g r a i n s are a r e generally g e n e r a l l y frosted f r o s t e d and calcite c a l c i t e is i s the t h e main main fair, cementing agent. agent. cementing of the t h e sandstones s a n d s t o n e s are1t!ell a r e w e l l cemented c e m e n t e d and others other Some of a r e friable. friable. are The siltstone s i l t s t o n e and and m u d s t o n e beels b e d s are a r e red~ r e d , brown, b r o w n , gray, g r a y , orange, orange mudstone or purple p u r p l e and are a r e extremely e x t r e m e l y ppoorly o o r l y sorted. sorted. or Mica i.s i s fairly fairly Hica abundant and m o s t of of the t h e beds b e d s are a r e bentonitic, bentonitic. abundant most s h a p e and texture texture The shape 84 84 of h e llarger a r g e r ggrains r a i n s iis s vvariable a r i a b l e and h e ccolors o l o r s rrange a n g e from h i t e , to to of tthe and tthe from w white, saber, tto amber, o rredish e d i s h bbrown. rown. of tthe weather Many of h e bbanded a n d e d ssilty i l t y bbeds eds w e a t h e r to to a "popcorn " p o p c o r n " sur s u rff ace. ace. The W Winsor on tthe The i n s o r ccan a n bbe e ddivided i v i d e d iinto n t o tthree h r e e uunits n i t s on h e bbasis a s i s of of the ssand-silt the a n d - s i l t rratio. atio. The llowest 50 ffeet and gray The o w e s t 50 e e t iis s ddominantly o m i n a n t l y rred e d and gray banded bbentonitic with few rreistant banded e n t o n i t i c ssiltstone iltstone w i t h a few e i s t a n t ssandstone a n d s t o n e beds. beds. Host of of tthe and much much of of the Most h e bbeds e d s aare r e lless e s s tthan h a n sseveral e v e r a l ffeet e e t tthick h i c k and the s i l t s t o n e iis s tthin h i n bbedded e d d e d tto o ffissile. issile. siltstone i n tthis h i s uunit. nit. in A b u n d a n t bbedded e d d e d gypsum s found found Abundant gypsum iis IIt t fforms o r m s a ssteep, t e e p , iirregular r r e g u l a r bbadland a d l a n d sslope. lope. The middle The middle u n i t which s aabout b o u t 55 ffeet e e t tthick h i c k iis s ddominantly o m i n a n t l y sandstone s a n d s t o n e and silty unit ,.rhich iis and silty sandstone. sandstone. The bbedding e d d i n g iis s tthick h i c k tto o m a s s i v e bbut u t tthe h e abundant a b u n d a n t silt s i l t in in massive of the t h e bbeds e d s ccauses a u s e s much of of tthe h e uunit n i t tto o w e a t h e r iinto n t o exfoliated exfoliated some of \.reather o r bumps. bumps. knobs or Most of tthe h e sandstone s a n d s t o n e is i s ccross r o s s llaminated a m i n a t e d and minoe minor Most of c h a n n e l s , uunconformities, n c o n f o r m i t i e s , and l o c a l conglomerate c o n g l o m e r a t e lenses l e n s e s are a r e common. channels, and local of the t h e individual i n d i v i d u a l bbeds e d s show faulting f a u l t i n g tthat h a t does d o e s nnot o t penetrate penetrate Many of o r below b e l o w and there t h e r e is i s evidence e v i d e n c e of of associated a s s o c i a t e d depositional depositional beds above or s l u m p i n g — b o t h are a r e probably p r o b a b l y related r e l a t e d to t o expulsion e x p u l s i o n of of water w a t e r during during slumping-·-both compaction. compaction. u n i t forms f o r m s a knoby k n o b y cliff c l i f f or o r hogback. hogback. The unit upper The upper f e e t of of the the W i n s o r Hember Member contains c o n t a i n s about a b o u t equal e q u a l rat r a t iios o s of of sandsand­ 204 feet Winsor s t o n e beds b e d s to t o siltstone s i l t s t o n e and mudstone m u d s t o n e beds. beds. stone T h i s is i s the t h e most m o s t intensely intensely This p a r t of of the t h e member and it i t forms f o r m s hadland b a d l a n d slopes s l o p e s and ledgy ledgy banded part cliffs. cliffs. Most of of the t h e beds b e d s are a r e less l e s s than t h a n 3 feet f e e t thick t h i c k although a l t h o u g h some of Host t h e sandstones s a n d s t o n e s and bentonitic b e n t o n i t i c mudstones m u d s t o n e s are a r e massive. massive. the C r o s s stratificastratifica­ Cross t i o n is i s common in i n the t h e sandstone s a n d s t o n e and some of of the t h e units u n i t s have h a v e flute flute tion c a s t s developed d e v e l o p e d on o n them. them. casts Many local l o c a l unconformities u n c o n f o r m i t i e s and gravel-filled gravel-filled Hany 85 c h a n n e l s are a r e ppresent r e s e n t in i n bboth o t h tthe h e sand s a n d and s i l t units. units. channels and silt Hinsor N.e mber of Paria No fossils f o s s i l s were w e r e found f o u n d in i n tthe he W i n s o r Member of tthe he P a r i a area area but Mt. but some ppelecypods e l e c y p o d s found f o u n d nnear ear M t . Carmel C a r m e l iin n tthe h e uupper p p e r ppart a r t of of the the Carmel Formation Bajocian F o r m a t i o n iindicate n d i c a t e iit t is i s pprobably robably B a j o c i a n or o r early e a r l y Callovian Callovian in age (Imlay, ( I m l a y , 1964, 1 9 6 4 , pp.. C5). C5). in D e p o s i t i o n a l Environments Environments Depositional The Carmel C a r m e l Formation F o r m a t i o n was deposited d e p o s i t e d in in a w i d e vvariety a r i e t y of of wide environments. environments. Some uunits, n i t s , especially e s p e c i a l l y pparts a r t s of h o s e in i n eeastern a s t e r n Utah Utah of tthose n o r t h e r n Arizona, A r i z o n a , are a r e eentirely n t i r e l y continental c o n t i n e n t a l and a r t s of of some and northern and pparts u n i t s , especially e s p e c i a l l y those t h o s e iin n southwestern southwestern U t a h , aare r e entirely e n t i r e l y off-shore off-shore units, Utah, shallow m arine. shallow marine. But o s t of of the t h e Carmel Carmel F o r m a t i o n including i n c l u d i n g rocks rocks But m most Formation i n tthe h e Paria P a r i a aarea r e a is i s of of m ixed m a r i n e and c o n t i n e n t a l origin. origin. in mixed marine and continental A l t h o u g h ggenerally e n e r a l l y tthe h e bbasal a s a l ppart a r t of h e Carmel C a r m e l Fo~~ation Formation Although of tthe c o n t a i n s .the t h e most m o s t llimestone, i m e s t o n e , tthe he P aria R i v e r Member of tthe h e Paria P a r i a area area contains Paria River Member of c o n t a i n s only o n l y one l i m y uunit--a n i t — a series s e r i e s of of w h i t e llimy i m y ssandstones a n d s t o n e s and contains one limy white interbedded m u d s t o n e s in i n tthe h e uupper p p e r ppart a r t of h e member. interbedded mlldstones of tthe i s dominantly d o m i n a n t l y clastic. clastic. member is The rrest e s t of th of the The w h i t e sandstone s a n d s t o n e probably probably white r e p r e s e n t s bbeach e a c h and bbar a r deposits d e p o s i t s and s s o c i a t e d sshallow hallow m a r i n e and and represents and aassociated marine e o l i a n sands. sands. eolian The most m o s t pplausible l a u s i b l e source s o u r c e area a r e a was tto o tthe h e south south r e - e x i s t i n g sedimentary s e d i m e n t a r y rr,)ck, ock, m ostly N a v a j o0 Sandstone, S a n d s t o n e , was where ppre-existing mostly Navaj being gently g e n t l y uuplifted p l i f t e d ((L2.ssentine, L a s s e n t i n e , 1969, 1 9 6 9 , pp.. 107). 107). being The ppoorly o o r l y sorted sorted red sandstone, s a n d s t o n e , siltstone, s i l t s t o n e , and and m udstone w e r e pprobably r o b a b l y ddeposited e p o s i t e d on ,red mudstone were complex mud and i d a l flats f l a t s and a s s o c i a t e d llagoons, a g o o n s , deltas, d e l t a s , fluvial fluvial and ttidal and associated c o m p l e x e s , and and pplayas. layas. complexes, T h a t tthis h i s llithologic i t h o l o g i c ttype y p e iincreases n c r e a s e s tto o the the That 86 west and nnorth o r t h may iindicate n d i c a t e a source s o u r c e iin n tthis h i s direction. direction. The i g h l a n d s was still s t i l l a slight s l i g h t ppositive o s i t i v e area a r e a and and probably probably Uncompahgre H Highlands p p l i e d some of of these t h e s e sediments. sediments. supplied s u The w white of sedimentary h i t e sandstone s a n d s t o n e facies, f a c i e s , on tthe h e eevidence v i d e n c e of sedimentary s t r u c t u r e s , was ddeposited e p o s i t e d iin n two environments. environments. structures, The llower o w e r ppart a r t of of the facies f a c i e s contains c o n t a i n s low low aangle n g l e ccross r o s s laminations l a m i n a t i o n s and and is i s apparently apparently the shallow m arine. shallow marine. Towards h e ttop o p of h e uunit n i t tthe h e angle a n g l e of of tthe h e cross cross Towards tthe of tthe l a m i n a t i o n s ssteepens t e e p e n s and and a hhigher i g h e r energy e n e r g y eenvironment--a n v i r o n m e n t — a beach-barbeach-barlaminations e o l i a n complex complex iis s iindicated. ndicated. eolian T h a t tthis h i s uunit n i t tthickens h i c k e n s tto o the t h e south south That and ttongues ongues w i t h rredbeds e d b e d s tto o tthe h e nnorth o r t h iindicates n d i c a t e s a ssoutherly o u t h e r l y source-source— with the h a t of t h e sands s a n d s of he P aria R i v e r Member. the same aass tthat of the of tthe Paria River IIf f these these sands pplus l u s tthe h e sands s a n d s of of tthe he P aria R i v e r and i n s o r Members aall l l merge merge sands Paria River and W Winsor and form n i t iin n tthe he C oal C anyon-W h i t e Mesa r e a s of r i z o n a , then then form one uuuit Coal Canyon;·fuite Mesa aareas of A Ari~ona, the N avajo, C armel, E n t r a d a , and Springs F o r m a t i o n s , form an the Navajo, Carmel, Entrada, and Cow Springs Formations, form an u n b r o k e n , tthick, hick, w h i t e ssandstone a n d s t o n e sequence s e q u e n c e nnear e a r tthe h e source s o u r c e area area unbroken, white ( L e s s e n t i m e , 1969, 1 9 6 9 , pp.. 109). 109). (Lessentime, Bedded gypsum gypsum iin of tthe Winsor Member indicates Bedded n tthe h e bbase a s e of he W i n s o r Member indicates s h a l l o w , ssaline, a l i n e , rrestricted e s t r i c t e d marine m a r i n e and a g o o n a l conditions conditions shallow, and oorr llagoonal a s s o c i a t e d with w i t h a llarge a r g e ttidal i d a l ccomplex. omplex. associated IIn n tthe h e ttime i m e span s p a n represented represented the m i d d l e uunit, n i t , more a n d was bbrought r o u g h t iin n from h e ssouth o u t h and beaches by the middle more ssand from tthe and beaches bars, and sshallow marine b a r s , and hallow m a r i n e sandstone s a n d s t o n e deposits d e p o s i t s rresulted. esulted. Some of of the the sand iis s aalso l s o ffluvial l u v i a l and d e l t a i c as a s shown h e nnu~erous u m e r o u s unconformitie unconformitie sand and deltaic show"n by by tthe llocal o c a l conglomeratic c o n g l o m e r a t i c sandstone s a n d s t o n e and and cchannels h a n n e l s of s a n d and and fine f i n e gravel. gravel. of sand h i c k uupper p p e r sequence s e q u e n c e iis s a vvery e r y complex c o m p l e x fluvial--paludal-tidal fluvial-paludal-tidal The tthick f l a t sequence. sequence. flat V o l c a n i c sources s o u r c e s tto o tthe h e s oouth u t h and o u t h w est e s t supplied supplied Volcanic and ssouth\\1 t h e vvolcanic o l c a n i c ash a s h tthat h a t hhas as w e a t h e r e d tto o bentonite. bentonite. the weather~d .87 87 Entrada E n t r a d a Sandstone Sandstone The Entrada E n t r a d a Sandstone S a n d s t o n e (Gilluly ( G i l l u l y and Reeside, R e e s i d e , 1926) 1926) hhas a s been been e x t e n s i v e l y miscorrelated m i s c o r r e l a t e d and and m i s n a m e d in i n southwestern southwestern U tah. extensively misnamed Utah. Near Near j i t . Carmel tthe h e name E n t r a d a was applied a p p l i e d (Baker, ( B a k e r , Kane, K a n e , and Reeside, Mt. Entrada and Reeside, G r e g o r y , 1950) 1950) to t o rrocks o c k s now assigned a s s i g n e d to t o the the C a r m e l Formation. Formation. 1936; Gregory, Carmel t h e Paria P a r i a area a r e a tthe h e Entrada E n t r a d a was m i s c o r r e l a t e d with w i t h tthe h e Thousand Thousand In the miscorrelated P o c k e t s Tongue of of the the N a v a j o Sandstone S a n d s t o n e by by Gregory G r e g o r y and h e true true pockets Navajo and tthe E n t r a d a was miscorrelated m i s c o r r e l a t e d with w i t h part p a r t of of tthe h e Winsor Winsor F ormation. Entrada Formation. This This T l a t t e r mistake m i s t a k e hhas a s appeared a p p e a r e d in i n several s e v e r a l papers p a p e r s since s i n c e tthe h e early e a r l y 50's. 50 s. latter t o further f u r t h e r complicate c o m p l i c a t e matters, m a t t e r s , between b e t w e e n West West Cove and Cottonwood And to and Cottonwood t h e upper u p p e r two members of of the t h e Entrada E n t r a d a Sandstone S a n d s t o n e uundergo ndergo a Canyon the r a p i d facies f a c i e s change c h a n g e and north n o r t h of of the t h e mouth m o u t h of of Cottonwood Cottonwood C r e e k and they rapid Creek and they resemble resemble t h e type t y p e Hinsor. Winsor. the I f tthe h e tvlO two following f o l l o w i n g facts f a c t s aare r e kkept e p t in in If mind 1) the t h e Entrada E n t r a d a of of the t h e Paria-Cannonvil1e P a r i a - C a n n o n v i l l e area a r e a ccan a n bbe e directly directly t r a c e d by outcrop o u t c r o p tto o tthe h e Entrada E n t r a d a of of tthe h e Lake Powell P o w e l l aarea r e a (which ( w h i c h can can traced be correlated c o r r e l a t e d \vith w i t h reasonable r e a s o n a b l e certainty c e r t a i n t y tto o the t h e type type E n t r a d a iin n the the Entrada R a f a e l Swell) S w e l l ) and 2) bbecause e c a u s e of of tthe h e sub-Cretaceous s u b - C r e t a c e o u s unconformity, unconformity, San Rafael t h e Entrada E n t r a d a is i s ttruncated r u n c a t e d jjust u s t west w e s t of of Lick L i c k Wash (Thompson the (Thompson and S t o k e s , in i n ppr.ess) r e s s ) and and no equivalent e q u i v a l e n t rocks r o c k s of of tth~ he E n t r a d a aare r e found found Stokes, Entrada west of of this t h i s area a r e a in i n southvlestern s o u t h w e s t e r n Utah U t a h the t h e Entrada E n t r a d a pproblem r o b l e m ccan a n be be west b e t t e r uunderstood n d e r s t o o d (fig. ( f i g . 18). 18). better A l l three t h r e e members of of tthe h e Entrada E n t r a d a Sandston(~ S a n d s t o n e as a s proposed proposed All S t o k e s aar<~ r e present p r e s e n t in i n the t h e Paria P a r i a area, a r e a , and following by Thompson and Stokes and following t h e i r suggestion s u g g e s t i o n no cow Cow ' Springs S p r i n g s Sandstone S a n d s t o n e is i s recognized. recognized. their These These members a r e in i n asscending a s s c e n d i n g o' o r der d e r the t h e Gunsight G u n s i g h t Butte, B u t t e , Car.nonville, C a n n o n v i l l e , and and tnembe' t:s are 88 88 E s c a l a n t e Members. Escalante fl gj{rht B u t t e Hember Member Gunsight Butte - nr The G unsight B u t t e Member t o k e s , iin n ppress) r e s s ) is is Gunsight Butte Hember (Thompson (Thompson and and SStokes, o r tthe h e tthick, h i c k , ccliff-forming l i f f - f o r m i n g ssandstone a n d s t o n e tthat h a t fforms o r m s tthe h e first first named ffor m a s s i v e ccliff l i f f aatt G unsight B u t t e and t h e r ccliffs l i f f s and u t t e s in in massive Gunsight Butte and many many oother and bbuttes the Powell the Lake P o w e l l rregion. egion. The uunit n i t hhas a s llong o n g bbeen e e n uunquestioned n q u e s t i o n e d Entrada Entrada i s correlative correlative w i t h ppart a r t of he E n t r a d a of h e Henry Mountain as ii tt is with of tthe Entrada of tthe Henry Hountain r e g i o n , San San R afael S w e l l , and of tthe he N a v a j o0 Country. Country. region, Rafael Sw'ell, and much much of Navaj IIt t has has p r e v i o u s l y bbeen e e n rreferred e f e r r e d tto o aas s the t h e lower l o w e r member of tthe he E n t r a d a oor r the the previously member of Entrada lower sandy sandy member member by many writers. writers. lower I n the t h e Paria P a r i a area a r e a tthe h e Guns;,ght G u n s i g h t Butte B u t t e Hember Member tthickens h i c k e n s rapidly rapidly In f e e t at a t West West Cove to t o around a r o u n d 200 feet f e e t in i n lower lower C o t t o n w o o d Canyon. Canyon. from 42 feet Cottoml7ood r a p i d change c h a n g e of of thickness t h i c k n e s s is i s due to t o depositional d e p o s i t i o n a l tthinning h i n n i n g rather rather This rapid t h a n erosion e r o s i o n as a s the t h e member thickens t h i c k e n s to t o 375 feet f e e t in i n the t h e Lake o w e l l area area than Lake PPml7ell ( S t o k e s and Thompson, 1969, 1 9 6 9 , p. p . 186). 186). (Stokes Gunsight B u t t e Nember Member is is a The Gunsight Butte ^ e l l o w i s h - g r a y , cliff-forming c l i f f - f o r m i n g ,sandstone. sandstone. yellOtl7ish-gray, i t forms f o r m s sheer sheer At West Cove it c l i f f s (fig. ( f i g . 17), 1 7 ) , along a l o n g the t h e back b a c k of of the t h e Cocksco:nb Cockscomb it i t forms f o r m s a resistant resistant cliffs hogback, and in more i n CottomrlOod C o t t o n w o o d Creek C r e e k where w h e r e it i t dips d i p s 45 deg d e g rees r e e s or or m o r e it it forms curious c u r i o u s needles n e e d l e s and standing s t a n d i n g rocks. rocks. It I t overlies o v e r l i e s the t h e ~nnsor Winsor Member of of the t h e Carmel C a r m e l with w i t h apparent a p p a r e n t conformity c o n f o r m i t y but b u t is i s separated s e p a r a t e d from from the t h e Cannonville C a n n o n v i l l e Member of of the t h e Entrada E n t r a d a l,y by a minor m i n o r unconformity u n c o n f o r m i t y (Stokes (Stokes and Thompson, 1969, 1 9 6 9 , p. p . 186). 186). 89 The unsight B u t t e Member s a vvery e r y uunifonn, niform, m a s s i v e , yellowishyellowishThe G Gunsight Butte Nember iis massive, r a y - tto o ggreenish-gray, r e e n i s h - g r a y , ccross-laminated, r o s s - l a m i n a t e d , ffine-grained, i n e - g r a i n e d , qquartz u a r t z sandstone. sandstone. grayThe g r a i n s aare re w ,veIl e l l rrounded, ounded, w well e l l ssorted, o r t e d , and and aare r e ttransparent r a n s p a r e n t oor r white white with e r y oobvious b v i o u s amber rains. with a few few vvery amber oorr brown brown ggrains. s t a i n s aare r e sscattered c a t t e r e d tthroughout h r o u g h o u t tthe h e ooutcrop. utcrop. stains S m a l l cconcentric o n c e n t r i c iron iron Small A l t h o u g h tthe h e cross cross Although l a m i n a t i o n ddoes o e s nnot ot w e a t h e r pprominantly, r o m i n a n t l y , iit t iis s aapparent p p a r e n t aatt closer closer lamination weather inspection. inspection. Most r o s s llaminations a m i n a t i o n s aare r e hhigh i g h angle a n g l e eolian-type. eolian-type. Host ccross Gunsight Butte Hember ffollows of Jurassic The G unsight B u t t e Member o l l o w s tthe h e ggeneral e n e r a l ppattern a t t e r n of Jurassic s e d i m e n t a t i o n iin n that t h a t it i t iis s w h i t e , ssandy, a n d y , and and cross c r o s s laminated l a m i n a t e d southward southward sedimentation white, but increases i n c r e a s e s in i n silt s i l t and and bbecomes e c o m e s red r e d north\vard--at n o r t h w a r d — a t Cannonville C a n n o n v i l l e the the but s a dark-red, d a r k - r e d , fine f i n e sandy s a n d y siltstone. siltstone. member iis Cannonville Cannonv i 11 e Member Member The Cannonville C a n n o n v i l l e Member of of the t h e Entrada E n t r a d a (Thompson and Stokes, S t o k e s , in in press) p r e s s ) has h a s ppreviously r e v i o u s l y been b e e n referred r e f e r r e d to t o as a s the t h e middle m i d d l e member or o r medial medial silty s i l t y member of of the t h e Entrada. Entrada. South S o u t h of of a line l i n e from from Warm Creek C r e e k Bay on on P o w e l l to t o West Cove, C o v e , the t h e Cannonville C a n n o n v i l l e Member is i s a gray, g r a y , crosscrossLake Powell l a m i n a t e d sandstone s a n d s t o n e but b u t to t o the t h e north n o r t h silt s i l t increases i n c r e a s e s and near near Imninated C a n n o n v i l l e ,, Utah the t h e member is i s dominantly d o m i n a n t l y siltstone s i l t s t o n e (Stokes ( S t o k e s and and Cannonville 1 9 6 9 , p. p . 186). 186), Thompson, 1969, p r e v iious o u s workers w o r k e r s have h a v e assigned a s s i g n e d the the Many prev C a n n o n v i l l e silty s i l t y facies f a c i e s to t o the t h e \.Jinsor W i n s o r Formation F o r m a t i o n but b u t recent r e c e n t 'vork work by by Cannonville Thompson and Stokes S t o k e s has h a s shown that t h a t it i t is i s part p a r t of of the t h e Entrada E n t r a d a Sandstone. Sandstone. thompson Eastward in i n the t h e Lake Pmvz P o w ell l l region r e g i o n Harshbarger H a r s h b a r g e r and others o t h e r s (1957) (1957) c o r r e l a t e d part p a r t of of it i t wHh w i t h the t h e Summerville S u m m e r v i l l e Fonna.tion F o r m a t i o n (Stokes ( S t o k e s and and correlated 1 9 6 9 , p. p . 186). 186). Thompson, 1969, w w E MT. CARMEL MX. CARMLL SKUTUMPAH S KUTUMPAH DAKOTA PAR IA PARIA FM. KOLOB - -.- .... ...J NAVAJ O SS. :E e:: 00: Co.) r:::: l0 0 1 22 I 4 66 8 8 Mi. Mi. F u r e 18 1 8 .... ,—G e n e r a l i z e d ccross r o s s ssection e c t i o n fro fromm tthe h e Pa P a ria r i a area a r e a tto o tthe h e Mt. a r m e l aarea, r e a , Utah s h o w i nng g the the Fii ggure Generalized Ht. C Carmel Utah showi ~vestwa::.-d o f J uuras of lithologies pprogr~: r o g r e sssive sive w e s t w a r d ttruncation r u n c a t i o n of r a s ssic i c st s t rr aata t a and a n d tthe h e similarity s i m i l a r i t y of l i t h o l o g i e s tthat h a t lled e d to to the miiss correla Utah. the m c o r r e l a ttions i o n s of of J uurass r a s s iic c Forma F o r m ations t i o n s in i n s oouthwe u t h w estern stern U tah. The Kolob }lember Member was the t h e origorig­ Nember was m miscorrelated Hith Paria River iinal n a l Carmel C a r m e l , t hhe e Crystal C r y s t a l Creek C r e e k Member iscorrelated w i t h tthe h e Entrada E n t r a d a ,, the the P aria R i v e r Nember Member miiscorrelClted with was m scorrelated w i t h the t h e Curtis C u r t i s Formation, F o r m a t i o n , and a n d the t h e Hinsor W i n s o r was thought t h o u g h t t oo be equivalent e q u i v a l e n t to t o the the No::-rison Att Paria M o r r i s o n formation. Formation. A P a r i a the t h e JJudd u d d Hollow Hollow Tongue Tongue 'vas was the t h e entire e n t i r e Carmel, C a r m e l , the t h e Thousand T h o u s a n d Po P ockets ckets Tongue .,ras Tongue was tthe h e Entrada, E n t r a d a , tthe h e Faria P a r i a River R i v e r Hembar Member was tthe h e Curtis C u r t i s and a n d the t h e r eest st o off the t h e Carmel C a r m e l and a n d all all the E n t r a d a was the W i n s o r Formation. F o r m a t i o n . ((~lodified M o d i f i e d from from Thompson Thompson and a n d S t ookes, k e s , in i n press) press) the Entl'eda '-7a5 the 'tansor 991 1 Cannonville Member iis IIn n tthe h e PParia a r i a aarea r e a tthe he C a n n o n v i l l e Member s ccharacterized h a r a c t e r i z e d by an b r u p t ffacies a c i e s cchange. hange. an aabrupt At h e member s a ggray, r a y , crosscrossAt West West Cove Cove tthe member iis l a m i n a t e d ssandstone a n d s t o n e aabout b o u t 200 e e t tthick. hick. laminated 200 ffeet At h e bbase a s e aare r e two red At tthe two red s t r i p e s tthat h a t aare r e sslightly lightly m o r e ssilty i l t y tthan h a n tthe h e rrest e s t of h e member (fig. .tripes more of tthe member (fig. 1 9 ) ; tthe h e llowest o w e s t sstripe tripe m a r k s tthe h e bbase a s e and i e s on b s c u r e erosion erosion 19); marks and llies on an an oobscure s u r f a c e ((Stokes S t o k e s and 9 6 9 , pp.. 186). 186). surface and Thompson, Thompson, 11969, N o r t h w a r d aat t tthe h e mouth mouth Northward of Cottonwood Cottonwood Canyon h e Cannonville C a n n o n v i l l e Member s a ggray r a y ssandy a n d y siltstone siltstone of Canyon tthe Member iis with tthin h i n bbands a n d s of u r p l e and e d cclaystone. laystone. with of ppurple and rred H e r e tthe h e bbasal a s a l contact contact Here with tthe he G unsight B u t t e Member s generally g e n e r a l l y cconcealed o n c e a l e d bby y aalluvium l l u v i u m but but with Gunsight Butte Member iis the estimated e s t i m a t e d tthickness h i c k n e s s of h e Cannonville C a n n o n v i l l e is i s approximately a p p r o x i m a t e l y 300 300 feet. feet. the of tthe The gray, g r a y , ccross-laminated r o s s - l a m i n a t e d ffacies a c i e s is i s a llight i g h t greenish-graygreenish-grayto yellowish-white, y e l l o w i s h - w h i t e , fine-grained, f i n e - g r a i n e d , quartz q u a r t z sandstone. sandstone. to o w e r 42 feet, feet The llower between and iincluding n c l u d i n g the t h e two rred e d stripes, s t r i p e s , iis s a ppoorly o o r l y sorted, s o r t e d , silty, silty, between f i n e - g r a i n e d , sandstone s a n d s t o n e with w i t h silt s i l t matrix. matrix. fine-grained, r e d stripes s t r i p e s contain contain The red s l i g h t l y more silt s i l t and and appear a p p e a r to t o be b e mechanically m e c h a n i c a l l y deposit~d d e p o s i t e d as a s red r e d beds beds slightly r a t h e r than t h a n post p o s t diagenically d i a g e n i c a l l y chemically c h e m i c a l l y altered. altered. rather C r o s s laminations laminations Cross i n this t h i s unit u n i t are a r e of of the t h e lowl o w - or o r medium-angle m e d i u m - a n g l e planar p l a n a r or o r trough-type. trough-type. in u n i t weathers w e a t h e r s into i n t o broken b r o k e n irregular i r r e g u l a r cliffs c l i f f s and hodoos. hodoos. The unit upper The upper p a r t of of the t h e gray, g r a y , cross-laminated c r o s s - l a m i n a t e d facies f a c i e s is i s a yellmvish-gray, y e l l o w i s h - g r a y , wel1wellpart s o r t e d , fine-grained, f i n e - g r a i n e d , friable f r i a b l e sandstone s a n d s t o n e that t h a t weathers w e a t h e r s into i n t o vertical vertical sorted, c l i f f s or o r rounded r o u n d e d knolls. knolls. cliffs T h i s unit u n i t contains c o n t a i n s a silt s i l t matrix m a t r i x but b u t in in This l e s s e r amounts a m o u n t s than t h a n the t h e lower l o w e r unit. unit. lesser q u a r t z grains g r a i n s are a r e subround subround The quartz a r e generally g e n e r a l l y white w h i t e or o r transparent t r a n s p a r e n t with w i t h a fe~v few brown and a n d red r e d grains. grains and are t h e top t o p several s e v e r a l sporadic s p o r a d i c red r e d and green g r e e n 2-foot-thick 2 - f o o t - t h i c k silt silt Towards the l e n t e l s o~ o r tongues t o n g u e s are a r e probably p r o b a b l y the t h e first f i r s t sign s i g n of of the t h e impending i m p e n d i n g facies facies lente1s t o the t h e north. north. change tc A l l of of the t h e sand sand All F i g u r e 19.--Entrada 1 9 . — E n t r a d a Sandstone S a n d s t o n e iin n West Cove. Cove, Figure Compare i t h figure f i g u r e 20. 20, Compare w with Figure F i g u r e 20.--Entrada 2 0 . — E n t r a d a Sandstone S a n d s t o n e iin n Cottonwood Cottonwood Canyon Canyon showing s h o w i n g silty s i l t y facies f a c i e s in i n Cannonville C a n n o n v i l l e and a n d Escalante Escalante Members. (Photograph ( P h o t o g r a p h by A. E. Thompson) Thompson) Figure Plains F i g u r e 24.--Southern 2 4 . — S o u t h e r n end end of of Brigham Brigham P l a i n s showing showing Tropic T r o p i c and a n d Straight S t r a i g h t Cliffs C l i f f s Formations. Formations. Ksd F i g u r e 2222 .--Cretaceous , — C r e t a c e o u s sstrata t r a t a in i n Cottonwood Cottonwood Figure Canyon. I%vajo S a n d s t o n e forms f o r m s tthe h e skyline. skyline. Navajo Sandstone 93 ·' above shows hhigh-angle, above tthe h e rred e d sstripes t r i p e s shows i g h - a n g l e , ffestoon-type, e s t o o n - t y p e , cross cross llaminations a m i n a t i o n s bbut u t of m a l l e r sscale c a l e tthan h a n tthat h a t iin n tthe he N a v a j o Sandstone. Sandstone. of a ssmaller Navajo h e s e ccross r o s s llaminations a m i n a t i o n s show a s h ppattern attern w h e r e one group Some of of tthese show a hhash where one group of r o s s llaminations a m i n a t i o n s iis s aat t aalmost l m o s t rright i g h t aangles n g l e s tto o tthose h o s e aabove b o v e and of ccross below b u t tthe h e uunit n i t shows e r y llittle i t t l e sslumping). lumping), below ((but shows vvery A p p a r e n t l y the the Apparently c r o s s llaminations a m i n a t i o n s became e m i c o n s o l i d a t e d and hen w e r e rripped i p p e d apart. apart. cross became ssemiconsolidated and tthen were Several miles Several m i l e s tto o tthe h e nnorth o r t h tthe h e ggray r a y ccross-stratified r o s s - s t r a t i f i e d facies facies g r a d e s into i n t o tthe h e ggray r a y silty s i l t y ffacies. acies. grades At ottonwood C r e e k tthere h e r e is is At C Cottonwood Creek s t i l l abundant a b u n d a n t ssandstone a n d s t o n e bbut u t tthe h e uunit n i t is i s dominantly d o m i n a n t l y a siltstone siltstone still e a t h e r s into i n t o steep s t e e p slopes s l o p e s and s m a l l badland b a d l a n d forms f o r m s (fig. ( f i g . 20); 20); and w weathers and small beds containing c o n t a i n i n g abundant a b u n d a n t sandstone s a n d s t o n e form k n o b s or o r bbroken r o k e n ledges. ledges. beds form knobs The of rred e d and purple p u r p l e claystone c l a y s t o n e are a r e several s e v e r a l feet f e e t thick--the thick—the bands of e n t i r e uuuit n i t is i s horizontally h o r i z o n t a l l y bedded b e d d e d 'w i t h some of of the t h e more massive massive entire ;vith c o n t a i n i n g cross-stratified c r o s s - s t r a t i f i e d silty s i l t y sandstone. sandstone. beds containing N o r t h w a r d the the Northward C a n n o n v i l l e becomes becomes finer f i n e r grained g r a i n e d and more m o r e varicolored v a r i c o l o r e d indicating indicating Cannonville a southerly s o u t h e r l y source s o u r c e for f o r the t h e sediment. sediment. Escalante E s c a l a n t e Member E s c a l a n t e Hem Member of the t h e Entrada E n t r a d a Sandstone S a n d s t o n e was named named ber of The Escalante f o r exposures e x p o s u r e s near n e a r Escalante, E s c a l a n t e , Utah, U t a h , by Thompson and Stokes S t o k e s (in ( i n press). press) for This T h i s unit u n i t has h a s prev p r e v iously i o u s l y been b e e n called c a l l e d the t h e uppe u p p e r member or o r clean clean sandy member. L i k e much of of the t h e Ca C anr m e l and the t h e rest r e s t of of the t h e Entrada, Entrada, Like nel this t h i s member consists c o n s i s t s of of clean c l e a n ",hite w h i t e sandstone s a n d s t o n e to t o the t h e south s o u t h but but s i l t y and red r e d to t o the t h e north1Vest-·-again n o r t h w e s t — a g a i n the t h e Paria P a r i a area a r e a is is becomes more ' silty l o c a t e d within w i t h i n this t h i s zone z o n e of of transition. transition. located The Escalante E s c a l a n t e Member was was c o r r e l a t e d with w i t h the t h e Surr.merville S u m m e r v i l l e by b y Har H a r shbarg s h b a r g eer r and ot o t hers h e r s (1957) (1957) Correlated 94 t h e Cow Springs(?) S p r i n g s ( ? ) by Peterson P e t e r s o n and and W a l d r o p (1965). (1965). and the Waldrop According According S t o k e s and Thompson Thompson (1969, ( 1 9 6 9 , p. p . 189) 189) this t h i s uunit n i t correlates c o r r e l a t e s with w i t h the the to Stokes lower portion p o r t i o n of of the t h e type t y p e Cow Springs. Springs. lower On tthe most h e map area area m o s t of of the t h e Escalante E s c a l a n t e Member has has t r u n c a t e d by the t h e sub-Cretaceous s u b - C r e t a c e o u s unconformity. unconformity. truncated been been F o r example, e x a m p l e , the the For E s c a l a n t e Member aaverages v e r a g e s around a r o u n d 170 feet f e e t thick t h i c k in i n the t h e southern southern Escalante P o w e l l rregion e g i o n but b u t it i t has h a s bbeen e e n truncated t r u n c a t e d to t o 84 feet f e e t thick t h i c k at at Lake Powell Cove—a distance d i s t a n c e of of approximately a p p r o x i m a t e l y 35 miles. miles. West Cove--a t h e southern southern On the of the t h e mapped mapped area a r e a in i n West Cove and along a l o n g the t h e lower l o w e r Paria Paria edges of R i v e r , tthe h e Escalante E s c a l a n t e Member is i s a mottled m o t t l e d silty s i l t y sandstone s a n d s t o n e that t h a t forms forms River, a cliff c l i f f or o r steep s t e e p slope s l o p e beneath b e n e a t h the t h e Dakota D a k o t a caprock. caprock. T h i s sandstone sandstone This i s silty, s i l t y , light-tan l i g h t - t a n to t o white, w h i t e , with w i t h lmv-angle l o w - a n g l e cross c r o s s laminations. laminations. is I n t e r b e d d e d with w i t h the t h e sandstone s a n d s t o n e are a r e I-to 1 - t o 3-foot-thic~ 3 - f o o t - t h i c k bbeds e d s of of ~ed red Interbedded g r e e n mottled m o t t l e d siltstone s i l t s t o n e and and claystone. claystone. and green T h e s e units u n i t s decrease decrease These e a s t w a r d and apparently a p p a r e n t l y are a r e absent a b s e n t east e a s t of of the t h e Paria P a r i a River R i v e r but b u t they they eastward i n c r e a s e to t o the t h e north n o r t h and west w e s t and are a r e abundant a b u n d a n t along a l o n g lower lower increase Cottonwood Creek. Creek. Cottonwood r e n d noticeable n o t i c e a b l e in i n the the P a r i a area a r e a and apparently apparently A ttrend Paria e l s e w h e r e is i s that t h a t the t h e silt s i l t is i s more m o r e prevalent p r e v a l e n t near n e a r the t h e base b a s e of of the the elsewhere E s c a l a n t e Member and the t h e sandstone s a n d s t o n e increases i n c r e a s e s towards t o w a r d s the t h e top. top. Escalante Hember and This This i s especially e s p e c i a l l y obvious o b v i o u s in i n Cot C o t ttomwod o n w o o d Canyon Canyon ';Jhere w h e r e a dark d a r k purple p u r p l e shale shale is a t the t h e bbase a s e grades g r a d e s up'vards u p w a r d s into i n t o mottled m o t t l e d siltstone s i l t s t o n e whi.::h w h i c h in i n turn turn at p a s s e s into i n t o a cross-lamina c r o s s - l a m i n a tted e d white w h i t e sandstone s a n d s t o n e (fi-g. ( f i g . 20). 20). passes B o t h contacts c o n t a c t s of of tthe h e Escalante E s c a l a n t e Member are a r e marked m a r k e d by by Both unconformities, unconformities~ b a s a l unconformity u n c o n f o r m i t y is i s sharp s h a r p and pplanar l a n a r with w i t h no no The bas:3-l o b v i o u s relief r e l i e f and is i s regional r e g i o n a l in i n extent e x t e n t (Stokes ( S t o k e s and Thompson, 1969, 1969, obvious P . 189). 189). p. p p e r contact c o n t a c t under u n d e r the t h e Dakota D a k o t a Formation F o r m a t i o n represents represents The uupper 95 v e r a l unconformities u n c o n f o r m i t i e s _ (to ( t o bbe e ddiscussed i s c u s s e d later) l a t e r ) and and hhas a s local l o c a l relief relief ss eevera1 of at a t least l e a s t 10 feet. feet. of S e v e r a l hhundred u n d r e d ffeet e e t of of Morrisen, M o r r i s o n , about a b o u t 100 100 Several f e e t of of Summerville S u m m e r v i l l e and and at a t least l e a s t 100 100 feet f e e t ef of Escalante E s c a l a n t e have h a v e been been feet r i o r tto. o Daketa D a k o t a deposition. deposition. removed pprior On tthe h e mapped r e a the the mapped aarea t h i c k n e s s of of tthe h e Escalante E s c a l a n t e Member rranges a n g e s frem from almest a l m o s t 90 feet f e e t along along thickness the Paria P a r i a River R i v e r tto. o near n e a r zero. z e r o feet f e e t in i n pparts a r t s ef of Cottonweed C o t t o n w o o d Canyen-Canyon— the a l l due to. t o the t h e ssub-Cretaceous u b - C r e t a c e o u s uncenfermities. unconformities. all D e p o s i t i o n a l Environments Environments Depositional Very little en tthe ef the Very l i t t l e werk work has h a s bbeen e e n ddone o n e on h e envirenments e n v i r o n m e n t s of the E n t r a d a Sandstene. Sandstone. Entrada L a r g e - s c a l e ffestoon-type e s t o o n - t y p e ccross r o s s stratificatien stratification Large-scale s c a t t e r e d dinosaur d i n o s a u r ttracks r a c k s have h a v e bbeen e e n cited c i t e d as a s evidence evidence and a few scattered f o r eolian e o l i a n deposition. deposition. for A l t h o u g h tthe h e eoliafL e o l i a n environIileiit e n v i r o n m e n t is is Altheugh r e p r e s e n t e d , the t h e Entrada E n t r a d a is i s a cemplex complex deposit d e p o s i t ef of ddeltaic, e l t a i c , fluvial, fluvial, represented, r o b a b l y lacustrine l a c u s t r i n e ssand, a n d , silt, s i l t , and and mud. mud. and pprebably The P Paria with a r i a area a r e a lies l i e s in i n a transition t r a n s i t i o n zzene one w i t h dominantly dominantly c o n t i n e n t a l cenditions c o n d i t i o n s seuthward s o u t h w a r d and d o m i n a n t l y aaqueeus q u e o u s conditiens conditions continental and deminantly n o r t h w a r d (fig. ( f i g . 16). 16). northward IIn n aall l l tthree h r e e members u t especia e s p e c i a lly l l y tthe h e two. two members bbut uppennest and centinental uppermost tthe h e conf c o n f lic.t l i c t bbet1.Jeen e t w e e n aqueeus a q u e o u s and c o n t i n e n t a l iis s apparent apparent with We st Ceve w i t h maj m a j oor r fa f a cc iies e s cchan.ge h a n g e s tak t a k iing n g pplace l a c e bbe e ttwee w e e nn West Cove and and Cot tell\olcod Creek. Cottonwood Creek. D uring G u n s ight i g h t Butte B u t t e deposition d e p o s i t i o n large l a r g e vvolumes o l u m e s ef of ssand a n d were were During Guns shed by hhighlands and w west shed by i g h l a n d s that t h a t l aay y to. t o tthe h e sOl:th s o u t h and e s t .• d e p o s i t e d along a l o n g tthe h e s oouthe u t h e rril n edg e d g ee of of deposited u n c o n f o r m i t y at a t tthe h e top top unconformity This T h i s sand s a n d was a nn a qque u e oous u s environment. environment. The of the t h e Guns G u n sight ight B u t t e lfember Member may represent represent ef Butte t h e change c h a n g e in i n rre e ggime i m e from from con c o n tinen t i n e n ta t a l tto o a qqueous u e o u s conditions. conditions. the 96 The a s a l ssilty i l t y rrocks o c k s of he C a n n o n v i l l e Member e r e llaid a i d in in The bbasal of tthe Cannonville Member w were s h a l l o w body ater. a shallow body of of w water. The ggray r a y ccross-stratified r o s s - s t r a t i f i e d facies f a c i e s represents represents hallow w a t e r ddeposit e p o s i t and h e ssilty i l t y ffacies a c i e s iis s probably probably a beach beach and and sshallow water and tthe a f f - s h o r e aaqueous q u e o u s ddeposit eposit w i t h pperiodic e r i o d i c nnorthward o r t h w a r d ssurges u r g e s of and an off-shore with of ssand a n 0 rresulting e s u l t i n g iin n ooff-shore f f - s h o r e bbar a r and e a c h deposits. deposits. and bbeach A i a t u s aat t tthe h e ttop o p of he C a n n o n v i l l e Member correlate A hhiatus of tthe Cannonville Member may correlate w i t h an n c o n f o r m i t y aas s ffar a r away s C o l o r a d o and e x i c o (Stokes (Stokes with an uunconformity away aas Colorado and New M Mexico 1 9 6 9 , pp.. 189). 189). and Thompson, 1969, The s c a l a n t e Member e p o s i t e d iin n a vvariety a r i e t y of of The E Escalante Member was ddeposited environments. environments. The bbasal and ppurple The a s a l rred e d and u r p l e shales s h a l e s aalong l o n g Cottonwood Cottonwood Creek are a r e pprobably r o b a b l y mud flat f l a t and and flood f l o o d pplane l a n e ddeposits e p o s i t s of altered Creek of altered v o l c a n i c aash. sh. volcanic M e d i a l ddepe p 'o)sits s i t s aagain g a i n shox^ h e conflict c o n f l i c t between between Medial shmv tthe c o n t i n e n t a l conditions c o n d i t i o n s ami. and tthe h e uupper p p e r sandy s a n d y uUriits n i t s a:::-e are aqueous and continental p r o b a b l y a pprelude r e l u d e tto o the t h e great g r e a t fluvial f l u v i a l sequence s e q u e n c e tto o follow f o l l o w in in probably M o r r i s o n and and Dakota D a k o t a time. time. Morrison }fuch Much work work is i s needed n e e d e d to t o substantiate s u b s t a n t i a t e or o r alter a l t e r tthe h e above above hypothesis. hypothesis. Sub-Cretaceous S u b - C r e t a c e o u s Unconformities Unconformities s t r i k i n g unconfonnity, u n c o n f o r m i t y , in i n terl1iS t e r m s of time t i m e and a n d relief, r e l i e f , lies lies A st;rikiIig at a t th(! t h e base b a s e of of the t h e Dakota D a k o t a Formation F o r m a t i o n i nn the t h e Paria P a r i a area. area. The The unconformity u n c o n f o r m i t y in i n the t h e Pari.a P a r i a area a r e a represer,ts r e p r e s e n t s the t h e time t i m e of of three three unconformities u n c o n f o r m i t i e s and two f oorinations r m a t i o n s in i n the t h e Escalante--Lake E s c a l a n t e - L a k e Powell Powell region. region. At Escalante E s c a l a n t e the t h e EntrHda E n t r a d a Sandstone S a n d s t o n e is i s overlain o v e r l a i n unconformably unconformably by the t h e Sum:-nerville S u m m e r v i l l e Formation F o r m a t i o n "Jhich w h i c h is i s oVtrlain o v e r l a i n unconformably u n c o n f o r m a b l y by by :91 97 the orrison F ormation w h i c h iis s ooverlain v e r l a i n uunconformably n c o n f o r m a b l y by the the M Morrison Formation w'hich by the Dakota ormation. Dakota FFormation. FFigure i g u r e 21 ddiagramatically i a g r a m a t i c a l l y shows h e relationships relationships shows tthe f tthese h e s e uunconformities. nconformities. of 0 IIt t ccan a n bbe e rreadily e a d i l y sseen e e n tthat h a t tthe h e tectonic tectonic a c t i v i t y tthat h a t iis s rresponsible e s p o n s i b l e ffor o r tthese h e s e uunconformities n c o n f o r m i t i e s was generated activity was generated from tthe h e ssouthwest, o u t h w e s t , tthe h e ddirection i r e c t i o n of a j o r ssource o u r c e of h e Jurassic Jurassic from. of a m major of tthe formations. formations. The uunderstanding n d e r s t a n d i n g of of tthese h e s e uunconformities n c o n f o r m i t i e s iis s eessential s s e n t i a l for for correlation of JJurassic of tthe Paria with Lake c o r r e l a t i o n of u r a s s i c rrocks o c k s of he P a r i a aarea rea w i t h tthe he L a k e Powell Powell Carmel areas. areas. and Mt. Carmel The ggeologic of tthese e o l o g i c ssignificance i g n i f i c a n c e of h e s e uunconformities n c o n f o r m i t i e s iis s not not e n t i r e l y uunderstood n d e r s t o o d bbut u t tthey h e y are a r e pprobably r o b a b l y related r e l a t e d tto o the t h e uplifts uplifts entirely s o u t h w e s t w a r d and between b e t w e e n tthe h e Mesocordilleran Mesocordilleran H i g h l a n d s and ^ the the southwestward Highlands a n Mogollon Highlands. Highlands. Mogollon V a r i o u s names including including N a v a j o Highlands H i g h l a n d s and and Various Navajo Mojavia appear a p p e a r in i n the t h e literature. literature. Mojavia T h e s e highlands h i g h l a n d s first f i r s t supplied supplied These s e d i m e n t s , mostly m o s t l y volcanic, v o l c a n i c , during d u r i n g Chinle C h i n l e time. time. sediments, f i r s t major major The first p r o v a b l e influx i n f l u x of of sediments s e d i m e n t s from from the t h e Mojave Mojave Highlands H i g h l a n d s are a r e in i n the the provable of the t h e Carmel C a r m e l Formation F o r m a t i o n although a l t h o u g h some of of the the Judd Hollow Tongue of Navajo may have h a v e come from from that t h a t direction. direction. Navajo T h r o u g h most m o s t of of the the Through J u r a s s i c the t h e highlands h i g h l a n d s supplied s u p p l i e d sediments s e d i m e n t s to t o the t h e Pa.ria. P a r i a and and Jur.assic s u r r o u n d i n g areas a r e a s including i n c l u d i n g the t h e volcanics v o l c a n i c s in i n the t h e Carmel. Carmel. surrounding But But d u r i n g latest l a t e s t Jurassic J u r a s s i c time t i m e the t h e uplift u p l i f t of of the t h e highlands h i g h l a n d s become more more dU1;ing i n t e n s e and the t h e great g r e a t Salt S a l t 1iJash Wash (Hember (Member of of Morrison M o r r i s o n Formation) F o r m a t i o n ) fan fan intense d e v e l o p e d — S u m m e r v i l l e and equivalents e q u i v a l e n t s and part p a r t of of the t h e Entrada E n t r a d a were were deyeloped--Sununerville removed ,,,est w e s t of of the t h e Kaiparowits K a i p a r o w i t s Plateau. Plateau. Then the t h e great g r e a t Hesocordilleran Mesocordilleran ° r Sevier S e v i e r Uplift U p l i f t which w h i c h took t o o k place p l a c e in I n the t h e Upper Upper Cretaceous C r e t a c e o u s truncated truncated or 98 tthe he M o r r i s o n nnear e a r tthe h e Echo o n o c l i n e ((Peterson P e t e r s o n and a l d r o p , 11965, 9 6 5 , pp.. 58) 58) }lorrison Echo M Monocline and W Waldrop, and d tthe h e EEntrada n t r a d a nnear e a r Skutumpah Skutumpah and and ssupplied u p p l i e d ssediments e d i m e n t s ffor o r the the n cretaceous of tthe Colorado C r e t a c e o u s FFormations o r m a t i o n s of he C o l o r a d o Plateau. Plateau. Cretaceous C r e t a c e o u s System System Dakota D a k o t a Formation Formation The D Dakota was named named ffor The a k o t a FFormation o r m a t i o n was o r eexposures x p o s u r e s aalong l o n g the the M issouri R i v e r iin n D akota C ounty, N e b r a s k a , bby y Meek Missouri River Dakota County, Nebraska, Meek and and Hayden ((1862, 1 8 6 2 , pp.. 4419-20)-1 9 - 2 0 ) — tthe h e tterm erm D a k o t a ( ? ) was i r s t uused s e d iin n the the Dakota(?) was ffirst K a i p a r o w i t s rregion e g i o n bby y G r e g o r y and 1 9 3 1 , pp.. 995). 5). Kaiparowits Gregory and Moore Moore ((1931, Later Later ggeologists e o l o g i s t s hhave a v e ssince i n c e removed h e qquery u e r y eeven v e n tthough h o u g h relationships relationships removed tthe w i t h tthe h e ttype y p e section s e c t i o n aare r e still s t i l l nnot ot w o r k e d oout. ut. with worked The D a k o t a of of Dakota the K a i p a r o w i t s rreg e g iion o n iis s much o u n g e r than t h a n tthe he D a k o t a at a t tthe h e type type the Kaiparmvits much yyounger Dakota section. section. M o s t , if i f nnot o t all a l l of of the the D a k o t a of of the t h e southern s o u t h e r n Colorado Colorado Most, Dakota P l a t e a u is i s Late L a t e Cretaceous C r e t a c e o u s although a l t h o u g h opinion o p i n i o n aabout b o u t the t h e age a g e varies varies Plateau from publication p u b l i c a t i o n to t o publication. publication. from I n the t h e Colorado C o l o r a d o Plateau P l a t e a u region r e g i o n the t h e Dakota D a k o t a is i s generally g e n e r a l l y less less In t h a n 200 fC2t f e e t thick t h i c k ,, commonly less l e s s than t h a n 100 feet f e e t thick t h i c k and locally locally than absent. absent. The Dakota D a k o t a shows a regional r e g i o n a l trend t r e n d of of thickening t h i c k e n i n g towards t o w a r d s the the west in i n sGuthwestern s o u t h w e s t e r n Utah U t a h (Lmvrence, ( L a w r e n c e , 1965, 1 9 6 5 , p. p . 83 8 3). ), It I t also a l s o coarsens coarsens in i n that t h a t direction d i r e c t i o n towards t o w a r d s the t h e Cretaceous C r e t a c e o u s uplifts. uplifts. Throughout T h r o u g h o u t the t h e Kaiparm.,its K a i p a r o w i t s regi r e g i oon n several s e v e r a l units u n i t s can c a n be be r o u g h l y correlated c o r r e l a t e d from area a r e a to t o area. area. ;roughly I n the t h e Lees L e e s Ferry F e r r y area area In P h o e n i x (1963, ( 1 9 6 3 , p. p . 36-38) 3 6 - 3 8 ) recogni r e c o g n i zzes e s a lO low e r basal b a s a l conglomerate c o n g l o m e r a t e ar.d and an an Phoenix \>ler u p p e r , incomplete i n c o m p l e t e sandstone-Llludstone s a n d s t o n e - m u d s t o n e unit u n i t \'lith w i t h traces t r a c e s of coal. coal. upper, P a r i aa Pari Mt.Carmel Mt. C a r m e l E scalante Escalante DAKOTA D AKOTA FFM M NAVAJO SS Figure Diagram~l F i g u r e 2L 2 1 . -..D i a g r a m *tic t i c section s e c t i o n from Nt. Mt. Carmel C a r m e l to t o Escalante, E s c a l a n t e , Utah Utah showing showing relationships r e l a t i o n s h i p s of of the t h e tlll~e t h r e ee r.>a m ajor j o r unconf u n c o n form o r mities i t i e s bet,,;een between the t h e Entra E n t r a dda a Sandstone S a n d s t o n e aa nnd d the t h e Dakota D a k o t a Forma F o r m ation. t i o n , (Nodified ( M o d i f i e d from from Thompson and a n d Stokes S t o k e s ,~ in i n press) press) 100 100 P e t e r s o n and W a l d r o p (1965, ( 1 9 6 5 , p. p . 59-60), 5 9 - 6 0 ) , working w o r k i n g in i n the t h e Wahweap Basin Basin peterson Waldrop a r e a , recognize r e c o g n i z e a lower l o w e r conglomerate, c o n g l o m e r a t e , Inedial m e d i a l lenticular l e n t i c u l a r sandstone, sandstone, area, u p p e r carbonaceous c a r b o n a c e o u s mudstone m u d s t o n e and and coal c o a l zone z o n e which w h i c h bbecomes e c o m e s very very and upper f o s s i l i f e r o u s at a t the t h e top. top. fossiliferous In I n tthe h e Paria P a r i a area a r e a tthe h e Dakota D a k o t a is i s 178 feet f e e t thick t h i c k ",here w h e r e the the hogback crosses c r o s s e s the t h e Paria P a r i a River. River. hogback I n the t h e southern s o u t h e r n part p a r t of of the t h e mapped mapped In a r e a , the t h e Dakota D a k o t a forms f o r m s a broad, b r o a d , irregular, i r r e g u l a r , cliffy c l i f f y bbench, e n c h , bbut u t the the area, o u t c r o p quickly q u i c k l y narrows n a r r o w s along a l o n g the t h e back b a c k of of the t h e Cockscomb where w h e r e it it outcrop forms a conspicuous c o n s p i c u o u s hogback h o g b a c k (fig. ( f i g . 22). 22). forms The D Dakota a k o t a consists c o n s i s t s of of a bbasal, a s a l , discontinuous d i s c o n t i n u o u s conglomerate, conglomerate, c o m p l e x l y bedded b e d d e d sandstone s a n d s t o n e unit, u n i t , a very v e r y complex c o m p l e x cyclic c y c l i c sandstonesandstonea complexly mudstone-coal mudstone-coal s e q u e n c e , and an uupper p p e r fossiliferous f o s s i l i f e r o u s sandstone s a n d s t o n e with with sequence, i n t e r b e d d e d thin t h i n coal c o a l streaks. streaks. interbedded Because B e c a u s e of of its i t s complex c o m p l e x lithology l i t h o l o g y and lenticular l e n t i c u l a r bbedding e d d i n g it it is i s difficult d i f f i c u l t to t o correlate c o r r e l a t e tthe h e various v a r i o u s uunits n i t s of of the t h e Dakota D a k o t a over over t h a n a short s h o r t distance, d i s t a n c e , however, however, w i t h some exceptions e x c e p t i o n s the t h e four four more than with u n i t s rreferred e f e r r e d tto o above a b o v e can c a n bbe e seen s e e n at a t numerous n u m e r o u s outcrops o u t c r o p s and are are units of some uuse s e in i n the t h e discussion d i s c u s s i o n of of tthe h e Dakota. Dakota. of a s a l conglomerate c o n g l o m e r a t e v arie a r i e ss considerably c o n s i d e r a b l y in i n tthickness h i c k n e s s from from The bbasal place missing p l a c e to t o place p l a c e and is i s compJ.etely completely m i s s i n g in i n some areas. areas. It I t is i s lightlight- brm-m and lenticular with mudstone, brown lenticular w i t h interbedde i n t e r b e d d e dd carbona c a r b o n a cceous eous m u d s t o n e , sandstone, sandstone, and siltstone. siltstone. The pebbles and range p e b b l e s are a r e mostly m o s t l y ",ell w e l l rounded r o u n d e d and r a n g e up to to i n c h e s in i n diamet d i a m e t ee r. r. 3 inches M o s t l y they t h e y an~ a r e sedimentary--chert, s e d i m e n t a r y — c h e r t , limestone, limestone, Hostly q u a r t z i t e , and silicified s i l i c i f i e d !llUdstone. mudstone. quartzite, i n t e r b e d d e d sandstone s a n d s t o n e shows shows The interbedded l o w - a n g l e cross c r o s s stratification s t r a t i f i c a t i o n and l eenticular n t i c u l a r bedding; b e d d i n g ; the t h e mudstone mudstone lo~v-angle and siltstone s i l t s t o n e is i s olive o l i v e ggrr eeeen n and and forms f o r m s bboth o t h a matrix m a t r i x and pebble p e b b l e···free -free 101 bbeds. eds. Coal with C o a l sstreaks t r e a k s aare r e aassociated ssociated w i t h tthe h e latter. latter. The llenticular one of of tthe main The e n t i c u l a r ssandstone a n d s t o n e uunit n i t iis s one he m a i n hogback hogback fformers o r m e r s of of tthe he D Dakota. akota. A All l l tthe h e bbeds e d s aare r e llenticular--much e n t i c u l a r — m u c h like like the pringdale S a n d s t o n e Member h e Moenave ormation. the SSpringdale Sandstone l1ember of of tthe Noenave FFormation. The unit The unit ccontains o n t a i n s llenticular e n t i c u l a r and avy-bedded w e l l - s o r t e d ssandstone a n d s t o n e tthat h a t ranges ranges and w wavy-bedded well-sorted from i n e tto o ccoarse o a r s e ggrained. rained. from ffine The ccolor o l o r iis s ttawny a w n y yyellow-gray e l l o w - g r a y and and ttypical y p i c a l of r e t a c e o u s fformations o r m a t i o n s iin n tthe he W e s t e r n Interior. Interior. of Upper Upper C Cretaceous Western The sandstone s a n d s t o n e iis s oover v e r 95 ppercent e r c e n t qquartz u a r t z and and ccontains o n t a i n s ssubangular u b a n g u l a r to to subrounded vvitreous i t r e o u s ggrains r a i n s tthat h a t are a r e iis s ccemented emented w i t h calcite. calcite. subrounded \vith Locally Locally i r o n - r i c h zzones o n e s form o n c r e t i o n s of r o n ccaprock a p r o c k tthat hat w e a t h e r bright bright iron-rich form cconcretions of iiron weather red (due (due tto o ccoal o a l tthat h a t hhas a s bbeen e e n bburned). urned). red A l l bbeds e d s ccontain o n t a i n smallsmallAll s c a l e ccross r o s s stratification s t r a t i f i c a t i o n and and bbedding e d d i n g that t h a t rranges a n g e s from from tthin h i n to to scale thick. thick. Many of h e uunits n i t s ccontain o n t a i n ppaper-ti"iin a p e r - t h i n ddiscontinuo"Jc i s c o n t i n u o u s streaks streaks of tthe of carbonaceous c a r b o n a c e o u s material. material. of L o c a l l y tthe h e lenticular l e n t i c u l a r ssandstone a n d s t o n e unit unit Locally h a s been b e e n removed removed by b y erosion. erosion. has The sandstone-mudstone-coal s a n d s t o n e - m u d s t o n e - c o a l uunit n i t is i s the t h e thickest t h i c k e s t unit u n i t of of the the Dakota. Dakota. South,.,rest S o u t h w e s t of of Brigham B r i g h a m Plains P l a i n s between b e t w e e n tthe h e Cottonwood C o t t o n w o o d Canyon Canyon Road and the t h e Paria P a r i a River R i v e r where w h e r e the t h e unit u n i t was studied s t u d i e d in i n detail, detail, a cyclic c y c l i c pattern p a t t e r n of of sediment s e d i m e n t ation a t i o n ,vas was seen. seen. At the t h e base b a s e of of the t h e cycle cycle is i s a lenticular-b l e n t i c u l a r - b eedded d d e d ,, micaceous m i c a c e o u s sandstone s a n d s t o n e similar s i m i l a r to t o the t h e above. above. This T h i s grades g r a d e s up into i n t o a poorly p o o r l y sorted s o r t e d thin-bedded, t h i n - b e d d e d , olive-gray o l i v e - g r a y sandstone sandstone and siltstone s i l t s t o n e sequence s e q u e n c e that t h a t contains c o n t a i n s abundant a b u n d a n t tracks) t r a c k s , trails, t r a i l s , and and bur~ows b u r r o w s as a s well w e l l as a s some poorly p o o r l y preserved p r e s e r v e d pelecypods. pelecypods. This T h i s unit unit g r a d e s up into i n t o a dark-gray d a r k - g r a y or o r black b l a c k fissile f i s s i l e shale s h a l e coataining containing grades a b u n d a n t carbonaceous c a r b o n a c e o u s material m a t e r i a l and coal. coal. abundant The topmost t o p m o s t cycle c y c l e has h a s aa c o a l seam 2 to t o 3 feet f e e t thick t h i c k and the t h e third t h i r d from the t h e top t o p cycle c y c l e (usually (usually Coal 102 102 which tthe h e bbasal a s a l ccycle) y c l e ) ccontains o n t a i n s aa ccoal o a l bbed e d 3 tto o 5 ffeet e e t tthick h i c k iin n w h i c h is is llocated o c a t e d aan n aabandoned b a n d o n e d ccoal oal m i n e ((fig. f i g . 223). 3). mine On ttop o p of h e ccoal o a l is is of tthe a narrow n a r r o w band s i l t s t o n e and shale s h a l e tthat h a t cchanges h a n g e s ssharply, h a r p l y , perhaps perhaps band of of siltstone unconformably, \.;rith unconf o r m a b l y , iinto n t o tthe h e ooverlying v e r l y i n g ccycle ycle w i t h a bbasal a s a l lenticular lenticular sandstone. sandstone. The a s a l ssand a n d of h e ttop-most o p - m o s t ccycle y c l e ccontains o n t a i n s several several The bbasal of tthe species of tthe marine s p e c i e s of he m a r i n e ppeleycopd e l e y c o p d IInoceramus. noceramus. Host of of tthe Most h e cycles cycles are and tthree make up up tthe a r e 20 tto o 25 ffeet e e t tthick h i c k and h r e e oor r ffour o u r ccycles y c l e s make h e entire entire uunit. nit. The uuppermost most p p e r m o s t uunit n i t iis s one one of of the the m o s t cconspicuous o n s p i c u o u s marker marker beds Kaiparowits and pprobably beds of of tthe he K a i p a r o w i t s rregion e g i o n and r o b a b l y can c a n bbe e ttraced r a c e d into into surrounding of tthe s u r r o u n d i n g aareas; r e a s ; tthis h i s iis s tthe h e ooyster y s t e r bbed e d at a t the t h e ttop o p of h e Dakota Dakota (originally by Gregory ( o r i g i n a l l y conside c o n s i d e rred e d Tropic T r o p i c Shale S h a l e by G r e g o r y and and 1'loore, M o o r e , 1931, 1931, p. Dakota p . 95, 9 5 , but b u t now classified c l a s s i f i e d as as D a k o t a by Lawrence, L a w r e n c e , 1965, 1 9 6 5 , pp.. 710) 6 ) .• The u n i t is i s a grayish-orange g r a y i s h - o r a n g e sandstone sandstone w i t h fist-sized f i s t - s i z e d ppelecypods. elecypods. unit with The ~,., g e n e r a inc1udeOstrea;Exogxra i n c l u d e O s t r e a , E x o g y r a ,, and Gryphaea. Gryphaea. genera I n pplaces l a c e s tthe h e oysters oysters In t h e main m a i n mass m a s s of of the t h e unit u n i t and the t h e sand s a n d is is a m atrix. form the matrix. unit The unit w e a t h e r s to t o a knobby, k n o b b y , oyster-strewn o y s t e r - s t r e w n ledge l e d g e beloH b e l o w the t h e ssoft o f t Tropic T r o p i c Shale; Shale lveathers t h e Dako D a k ota t a is i s steeply s t e e p l y dipping d i p p i n g it i t is i s a hogback h o g b a c k former. former. where the Lawrence (1965, ( 1 9 6 5 , p. p , 84-85) 8 4 - 8 5 ) gives g i v e s the t h e foll f o l l oowing w i n g account a c c o u n t of of the the Lawrenc.e paleontology: paleontology: "Near " N e a r the t h e base b a s e of of th'2 t h e fossiliferous f o s s i l i f e r o u s zone z o n e there there is (?) - bu:;:-Ymvs i s a thin t h i n bed b e d of of cyLLndr:Lcal c y l i n d r i c a l ,verm worm(?) b u r r o w s . A very very f o s s i l i f e r o u s bed b e d containing c o n t a i n i n g .2~trea O s t r e a p:c~dentia p r u d e n t i a is i s several several fossiliferous feet (?) bed. f e e t above a b o v e t hhe e worm worm(?) b e d . - On the t h e west w e s t side s i d e of of the the Kaiparo"Jits K a i p a r o w i t s Plateau P l a t e a u the t h e Ostre::tJ? O s t r e a p ruderttiu. r u d e n t i a bed b e d is is separated s e p a r a t e d fro'TI. from the t h e bottom b o t t o m of th t h e upp2r u p p e r sands s a n d s ttone o n e by by a t h i n - mudstone m u d s t o n e bed. bed. S e v e r a l feet f e e t above a b o v e tne t h e .Q.s O str~!!. trea thin Several 'Et.~denti~ p r u d e n t i a there t h e r e i ssaa zone zone- ,\Tit w i t h}: abundant a b u n d a n t 1:~j\yra E x o g y r a -coltirilbella; columbella; b e d containing c o n t a i n i n g -E::":~3J E x o g yrr a ol o l iJ.ssp p oot'l_~ n e nn ss ii sG is i s at a t the t h e top t o p of of a bed u p p e r ss andstone a n d s t o n e . 0.!.'L G r yph p h aa e_~ ea p n l~.v!.b e w beL e rrr ~:!: y i is i s :La i n -the t h e top t o p two two upper f e e t of of the t h e upper u p p e r s ands a n d s tone t o n e in i n some places. places, These feet These l>larine M a r i n e shale s h a l e and a n d claystone; claystone; bentonitic. bentonitic. E x t r e m e l y fossillf~rous fossiliferous m a r i n e sandstone; sandstone; Extremely marine upper u p p e r 8 feet f e e t is i s ooyster y s t e r bed. bed. ,... 11'1 ... Q ... 11'1 Coal; several Coal; s e v e r a l inches i n c h e s tto o 2 feet f e e t thick. thick. Black B l a c k fissile f i s s i l e shale. shale. Interbedded I n t e r b e d d e d olive o l i v e s iiltstone, l t s t o n e , shale, s h a l e , tan tan sandstone; t h i n qedded. bedded. sandstone; thin Hedium-beddcd ....Ttl sandstone with Medium-bedded bro brown sandstone w i t h a few few silty wavy bedded; s i l t y and a n d shaly s h a l y bbeds; e d s ; wavy bedded; contains m a r i n e pelecypods p e l e c y p o d s •. contains marine Black B l a c k and a n d gray g r a y carbonaceous c a r b o n a c e o u s fissile f i s s i l e shale shale with w i t h a few coal c o a l streaks. streaks. ...'" N IInterbedded n t e r b e d d e d olive o l i v e siltstone, s i l t s t o n e , shale, s h a l e , tan tan sandstone. sandstone. B r o w n - t o - g r a y wavy-bedded w a v y - b e d d e d sandstone s a n d s t o n e with with Brown-to-gray few slIt s i l t and a n d shale s h a l e beds. beds. > Coal; Coal; 3 feet f e e t thick; thick; Bla~k B l a c k fissile f i s s i l e shale. shale. ,...'" Q II'l abandoned a b a n d o n e d ccoal o a l mine. mine. I n t e r b e d d eed d olive o l i v e siltstone, s i l t s t o n e , shale, s h a l e , tan tan Interbedd sandstone. sandstone. Brown and a n d light-tan l i g h t - t a n ssandstone; andstone? I3rOlln b e dds, s , wavy bedded; bedded; be c o a l streaks. streaks. coal 11'1 '" e n t i cular cular llenti few ssilt i l t bbeds e d s and and fe'!-1 Lenticular L e n t i c u l a r coal c o a l beds b e d s aand n d streaks. streaks. Conglomerllt pebbles C o n g l o m e r a t e~,; p e b b l e s up tto o several several inches; channels inches; c h a n n e l s ccut u t iin n Entrada} Entrada; t o 12 fea f e e t of of rel1ef~ relief. up to L i g h t - c o llored o r e d sandstone sandstone w i t h vari v a r i colored colored Light-co with silt s i jit, bbeds. eds. Figure F i g u r e 23. 2 3 , "--Genera — G e n e r allii szce e dd s~ction s e c t i o n of of the t h e Dal,ota D a k o t a For.mat F o r m a t iion o n iin n tthe h e southsouth­ e a s t e r n corner c o r n e r of of the t h e map Hl"ea a r e a sho"ling s h o w i n g cyclic c y c l i c rrepgtlon e p i t i o n of lithologies. eastern of llthologies. 104 fossiliferous f o s s i l i f e r o u s bbeds e d s are a r e associated a s s o c i a t e d with w i t h tthe h e upper upper sandstone westward s a n d s t o n e and and ddisappear isappear w e s t w a r d where w h e r e tthe h e sandstone sandstone iintertongues ntertongues w i t h bbeds e d s of of mudstone." mudstone." with This T h i s uupper p p e r sandstone s a n d s t o n e bbed e d is i s aabout b o u t 15 feet f e e t thick. thick. The bed bed t h a t contains c o n t a i n s the t h e Gryphaeanewberryi G r y p h a e a n e w b e r r y i is i s quite q u i t e ssilty i l t y and and completely completely that transitional w i t h tthe h e ooverlying verlying T r o p i c Shale S h a l e tthrough h r o u g h a tthickness h i c k n e s s of of transitional with Tropic s e v e r a l feet. feet. several F o s s i l s ccollected o l l e c t e d from from tthe he D a k o t a Formation F o r m a t i o n during during Fossils Dakota t h i s study s t u d y are a r e listed l i s t e d below: below: this Ammonites Ammonites Fragment wyomirtgensis F r a g m e n t cf~priortocyc1us c f . P r i o n o c y c l u s Wyoming ens i s Fragment F r a g m e n t unidentified unidentified Pelecypods Pelecypods Ostreapruderttia Gryphaeartewberryi Ostrea prudentia Gryphaea newberryi Q. •2.* congesta eongesta IInocerarr'lus n o c e r a m u s ·labidatus labidatus II .. .fragilis O. 0_. soleniscus soleniscus • fragilis Trigonarcaobliqua EXC?8..Y.ra E x o g y r a C<?h. c o l ui1lm1bbella ella T r i g o n a r c a o b l i q u a (?) (?) Barbatia nlirortema E.. suborbictilata E suborbiculata B arbatia m i r o n e m a (?) (?) E. · oli _E, o l i s i~ortertsis iponensis HO:::ili ::ubes (?) Worm t u b e s ( ? ) Using evidence collected by Averitt, Lmvrence (1965, U s i n g e v i d e n c e c o l l e c t e d by A v e r i t t , Lawrence (1965, p. 86) states that much of the Dakota of the Kaiparowits region is p . 86) s t a t e s t h a t much of t h e D a k o t a of t h e K a i p a r o w i t s r e g i o n i s Early Cretaceous (Aptian), but Phoenix (1963, p. 37) using evidence Early Cretaceous ( A p t i a n ) , but Phoenix ( 1 9 6 3 , p . 37) u s i n g evidence furnished by Craig states that the Dakota of the Paria, Cannonville, f u r n i s h e d by C r a i g s t a t e s t h a t t h e D a k o t a of t h e P a r i a , Cannonville, and Lees Ferry areas is Late Cretaceous. Apparently more data are and L e e s F e r r y a r e a s i s L a t e C r e t a c e o u s . A p p a r e n t l y more d a t a are needed to 8.::curately date the Dakota. needed t o a c c u r a t e l y d a t e t h e Dakota. The environm2nt of the Dakota Formation is complex: the The e n v i r o n m e n t of t h e D a k o t a F o r m a t i o n i s c o m p l e x : the lower part is fluvial, the middle pa!.-t fluvial and marine, and t.he lower p a r t i s f l u v i a l , t h e middle part: f l u v i a l and m a r i n e , and the upper part marine. The Dakota was deposited over a large area and upper p a r t m a r i n e . The D a k o t a was d e p o s i t e d o v e r a l a r g e a r e a and the area of deposition subsided very slmv1y. The thin, discontinuous, t h e a r e a of d e p o s i t i o n s u b s i d e d v e r y s l o w l y . The t h i n , discontinuous, but persistent basal conglomerate reflects vigorous erosion and b u t p e r s i s t e n t b a s a l c o n g l o m e r a t e r e f l e c t s v i g o r o u s e r o s i o n and minor deposition; this is quite sjJuilar to the Shinarump and the minor d e p o s i t i o n ; this is quite similar discussion given it. applies here. discussion given i t applies here. t o t h e S h i n a r u m p and the After the gr avel episode, sand- After the gravel episode, sand- 103 ios lladen a d e n rrivers ivers ccrisscrossed r i s s c r o s s e d tthe h e aarea; r e a ; ttheir h e i r cchannel h a n n e l ddeposits e p o s i t s aare r e seen seen iin n tthe h e llenticular e n t i c u l a r ssandstone a n d s t o n e uunit. nit. A h i s ttime i m e tthe h e Cretaceous Cretaceous Att tthis sseas eas w e r e ttransgressing r a n s g r e s s i n g from h e nnorth o r t h and a s t and e l t a s and and were from tthe and eeast and ddeltas sstrand-line t r a n d - l i n e ddeposits e p o s i t s ddeveloped. eveloped. A o n f l i c t bbetween etween m a r i n e and A cconflict marine ccontinental o n t i n e n t a l cconditions o n d i t i o n s ddeveloped e v e l o p e d and x t e n s i v e swamps o r d e r e d the the and eextensive swamps bbordered many bbays a y s and s t u a r i e s of h e sseaway. eaway. and eestuaries of tthe F i n a l l y cconditions o n d i t i o n s became became Finally sstable, t a b l e , ssubsidence u b s i d e n c e and and ddeposition eposition w e r e vvery e r y sslight, l i g h t , and h e energy energy were and tthe vvery e r y llow; o w ; vvery e r y ffine i n e ssand, a n d , ssilt, i l t , and i n a l l y ffissile issile m u d s t o n e were were and ffinally mudstone deposited. deposited. IIf f tthe h e pproper r o p e r cconditions o n d i t i o n s ppersisted, e r s i s t e d , ccoal o a l ddeveloped e v e l o p e d in in t h e extensive e x t e n s i v e swamps. the An iincrease n c r e a s e iin n eenergy n e r g y aaccompanied c c o m p a n i e d by fluvial by fluvial a r i n e pprocesses r o c e s s e s ddeposited e p o s i t e d sand s a n d aacross c r o s s tthe h e fformer o r m e r s\vamp--the swamp—the and m marine c y c l e repeated. repeated. cycle end of At tthe h e end of the t h e cyclic c y c l i c deposition d e p o s i t i o n tthe h e sea s e a ma.de made a steady steady t r a n s g r e s s i o n across a c r o s s tthe h e aarea. rea. transgression Muddy water w a t e r cconditions o n d i t i o n s developed developed h e sea s e a moved across a c r o s s former f o r m e r swamps and alluvial a l l u v i a l pplains l a i n s and and as tthe c r e a t e d ideal i d e a l environments e n v i r o n m e n t s for f o r tthe h e large l a r g e oyster o y s t e r ppopulation o p u l a t i o n that that created developed. developed. t h e sea s e a moved westwar w e s t w a r dd,, the t h e sandstone s a n d s t o n e deposition deposition As the c e a s e d and the t h e shallow s h a l l o w ma m arine r i n e Tropic T r o p i c Sha S h a le l e was deposited. deposited. ceased Tropic T r o p i c Shale Shale T r o p i c Shale S h a l e 'vas was named by Greg G r e g ory o r y and Moore (1931, ( 1 9 3 1 , p. p . 98) 98) The Tropic for f o r exposures e x p o s u r e s near n e a r Tropic, T r o p i c , Utah, U t a h , in i n the t h e uppe u p p e r Pa P aria r i a River R i v e r Valley. Valley. The Tropic ward T r o p i c gradually g r a d u a l l y th t h i cckens k e n s eastward; e a s t w a r d ; west westw a r d it i t grades g r a d e s into i n t o aa s a n d Btone s t o n e faci f a c i eess (Lawrence, ( L a w r e n c e , 1965, 1 9 6 5 , p. p . 88). 88). sand T r o p i c is i s 605 f eee e t thick t h i c k in i n lmver l o w e r Cottonwood C o t t o n w o o d Canyon and and The Tropic 106 eestDnates s t i m a t e s aat t oother t h e r llocalities o c a l i t i e s show e r y llittle i t t l e vvariance a r i a n c e throughout throughout show vvery tthe h e mapped rea. mapped aarea. B o t h ccontacts o n t a c t s of h e TTropic r o p i c aare r e cconformable o n f o r m a b l e and Both of tthe ggradational r a d a t i o n a l and a n bbe e rreadily e a d i l y ppicked i c k e d on e r i a l pphotos. hotos. and ccan on aaerial The lower The lower ccontact o n t a c t hhas a s bbeen e e n ddiscussed--the i s c u s s e d — t h e uupper p p e r ccontact o n t a c t iis s pplaced l a c e d aat t tthe h e base base of h e ffirst irst m a s s i v e ssandstone, a n d s t o n e , ggenerally e n e r a l l y 40 o 60 e e t tthick h i c k at at of tthe massive 40 tto 60 ffeet tthe h e bbase a s e of h e ooverlying verlying S traight C l i f f s FFormation. ormation. of tthe Straight Cliffs The Tropic The Tropic Shale s aan n eextremely x t r e m e l y weak o r m a t i o n tthat h a t fforms o r m s ddesolate e s o l a t e low hills Shale iis weak fformation low hills and l o p e s bbeneath e n e a t h tthe he S traight C liffs F ormation. and sslopes Straight Cliffs Formation. IIn n Cottonwood Cottonwood Canyon h e r e tthe h e fformation o r m a t i o n ddips i p s at a t 35 ddegrees, e g r e e s , iit t fforms o r m s a broad broad Canyor. w where s t r i k e vvalley a l l e y bbetween e t w e e n two hhogback-forming o g b a c k - f o r m i n g fformations o r m a t i o n s (fig. ( f i g . 22). 22). strike L i t h o l o g i c a l l y tthe he T r o p i c iis s oone n e of of tthe he m o s t uuniform n i f o r m ddeposits e p o s i t s in i n the the Lithologically Tropic most P a r i a area. area. Paria M o d e r a t e environmental e n v i r o n m e n t a l changes c h a n g e s have h a v e caused c a u s e d sslight l i g h t color color Moderate c h a n g e s about a b o u t 300 feet f e e t below b e l o w tthe h e top. top. changes The lower l o w e r half h a l f of of the t h e formation f o r m a t i o n is i s a dark d a r k gray, g r a y , laminated, laminated, b e n t o n i t i c claystone c l a y s t o n e and mudstone m u d s t o n e that t h a t weathers w e a t h e r s to t o a greenish-gray greenish-gray bentonitic o r silver-gray s i l v e r - g r a y "popcorn-textured" " p o p c o r n - t e x t u r e d " surface. surface. or S e v e r a l inches i n c h e s to t o aa Several f o o t below b e l o w this t h i s surface s u r f a c e fresh f r e s h material m a t e r i a l can c a n be b e broken b r o k e n out o u t into i n t o rounded rounded foot chunks c h u n k s that t h a t clearly c l e a r l y show the t h e thin t h i n laminations--the l a m i n a t i o n s — t h e rock r o c k splits s p l i t s into into flat f l a t surfaces s u r f a c e s along a l o n g these t h e s e lwnillations. laminations. The upper u p p e r part p a r t of the t h e Tropic T r o p i c Shale S h a l e is i s a meditm-brown medium-brown claystone claystone that t h a t contains c o n t a i n s pyrite p y r i t e nodules, n o d u l e s , shark s h a r k teeth, t e e t h , fish f i s h scales, s c a l e s , and shell shell f r a g m e n t s (Lm.renee, ( L a w r e n c e , 1965, 1 9 6 5 , p. p . 86-87). 86-87). fragments At 514 feet f e e t above a b o v e the t h e base, b a s e , the the f i r s t of of a sequence s e q u e n c e of fine-grained, f i n e - g r a i n e d , thin, t h i n , poorly-sorted, p o o r l y - s o r t e d , tan t a n sandsand­ first s t o n e s appear. appear. stones T h e s e sandstones s a n d s t o n e s are a r e cross-stratified, c r o s s - s t r a t i f i e d , contain c o n t a i n ripple ripple These l a m i n a t i o n s and and ,,,ronn(?) worm(?) tubes, t u b e s , and and increase i n c r e a s e in i n .number number and and thickness thickness laminations 107 t o w a r d s the t h e ttop o p of of the t h e Tropic. Tropic. towards c o n t a c t is i s placed p l a c e d at a t the t h e base base The contact of massive of the t h e first first m a s s i v e sandstone s a n d s t o n e (which ( w h i c h is i s generally g e n e r a l l y 40 to t o 60 feet feet thick) Cliffs t h i c k ) at a t the t h e base b a s e of of the t h e Straight Straight C l i f f s Formation. Formation. At a few few feet f e e t above a b o v e the t h e bbase a s e of of the t h e Tropic T r o p i c is i s the the extremely e x t r e m e l y fossiliferous f o s s i l i f e r o u s concretion c o n c r e t i o n zzone o n e tthat h a t contains c o n t a i n s flattened flattened limestone l i m e s t o n e nnodules o d u l e s up tto o several s e v e r a l feet f e e t in i n diameter. diameter. f o s s i l s are a r e found f o u n d in i n these t h e s e concretions. concretions. fossils Many well w e l l preserved preserved T h r o u g h o u t the t h e rest r e s t of of Throughout the t h e lower l o w e r part p a r t of of the t h e Tropic, T r o p i c , fresh f r e s h rock, r o c k , when split, s p l i t , yields y i e l d s numerous numerous white w h i t e impressions i m p r e s s i o n s of of tthe h e pelecypod p e l e c y p o d Irtoc~ramus. Inoceramus. Reds Beds in i n the t h e lower lower part p a r t of of the the medium-brown medium-brown claystone c l a y s t o n e yield y i e l d numerous n u m e r o u s white w h i t e L~pressions impressions of Selwynbc~raSl\Tbllgari of "dwarfed" " d w a r f e d " ·S e l w y n o c e r a s w o l l g a r i Fossils F o s s i l s found f o u n d in i n the t h e Paria P a r i a area area are a r e listed l i s t e d below: below: Ce C ep11alopods phalopods Baculites B a c u l i t e s gracilis gracilis Meto M e t oicocerasswallovi icoceras swallovi Selwynoceras S e l w y n o c e r a s \voolgari woolgari A l l o c r i o c e r a s sp. sp. Allocrioceras Pelecypods Pelecypods . Exogyra? Exogyra? 1i1Ocerainus I n o c e r a m u s labiatus labiatus 1. fragiHs I. fragilis Lucina L u c i n a subundata subundata ---C o r b u l a Kanabensis Kanabensis Corbula Gastropods Gastropods Lanatia L u n a t i a concinna concinna Gyn)i(fE;s G y r o i d e s cf-:-~-G~-conr c f . G. c o n radi adi Yurritella T u r r i t e l l a vJhltei whitei ?PleurotcmaHitzi ?Pleurotoma H i t z 1 The Tropic Hemb er of T r o p i c correlates c o r r e l a t e s with w i t h the t h e Tununk Tununk Member of tthe h e !:-fancos Mancos Sha.le Henry S h a l e of of the the H e n r y }fountains M o u n t a i n s region. region. The age a g e of of both b o t h these t h e s e units units is i s firmly f i r m l y established e s t a b l i s h e d as a s early e a r l y Late L a t e Cretaceous C r e t a c e o u s (late ( l a t e Cenomanian Cenomanian and ,early e a r l y Turonian). Turonian). 108 108 The llower of tthe Tropic Shale was ddeposited The o w e r ppart a r t of he T ropic S h a l e was e p o s i t e d iin n aan n open, open, marine sshallow hallow m a r i n e eenvironment n v i r o n m e n t .. The llarge amount of of cclastic The a r g e amount l a s t i c material material marine from tthe west and ssouth. was bbrought r o u g h t iinto n t o tthe he m a r i n e bbasin a s i n from he w e s t and outh. During During Tropic formed tto llate ate T r o p i c ttime i m e a bbarrier a r r i e r formed o tthe h e eeast a s t rrestricting e s t r i c t i n g the the Tropic T r o p i c ssea. ea. Pyrite P y r i t e iindicates n d i c a t e s a rreducing e d u c i n g eenvironment; n v i r o n m e n t ; a large large amount of kkaolinite amount of a o l i n i t e ssuggests u g g e s t s iit t was sslightly l i g h t l y aacidic c i d i c ((Lawrence, L a w r e n c e , 1965, 1965, pp.. 889). 9). Tropic and ddeltas of the As tthe he T r o p i c ssea e a rregressed, e g r e s s e d , bbeaches e a c h e s and e l t a s of the S t r a i g h t Cliffs Cliffs F ormation w e r e deposited. deposited. Straight Formation were Hnt'.f Straight Cliffs Straight C l i f f s Formation Formation Gregory G r e g o r y and and Moore (1931, ( 1 9 3 1 , p. p . 91) applied a p p l i e d the t h e term t e r m Straight Straight C l i f f s Sandstone S a n d s t o n e for f o r exposures e x p o s u r e s aalong l o n g the t h e Straight S t r a i g h t Cliffs C l i f f s escarpment escarpment Cliffs s o u t h of of Escalante, E s c a l a n t e , Utah. Utah. south W a l d r o p and P e t e r s o n (1965, ( 1 9 6 5 , p. p . ry2.-63) 62-63) Hal<lrop Peterson proposed p r o p o s e d tthe h e term t e r m Straight S t r a i g h t Cliffs C l i f f s Formation F o r m a t i o n bbecause e c a u s e of of the t h e quantity quantity of shale s h a l e and coal c o a l at a t many localities. localities. of L i k e most m o s t Upper Upper Cretaceous Cretaceous Like u n i t s , the t h e Straight S t r a i g h t Cliffs C l i f f s becomes b e c o m e s increasingly i n c r e a s i n g l y marine m a r i n e and and sandy units, an s h a l y in i n an Easterly e a s t e r l y direction, d i r e c t i o n , most m o s t of of the t h e Straight S t r a i g h t Cliffs C l i f f s is is shaly t h e time-equivalent t i m e - e q u i v a l e n t of of the t h e Mancos Shale S h a l e of of the t h e San Juan J u a n Easin B a s i n and and the M o u n t a i n s region r e g i o n (P ( Pee terson, t e r s o n , 1969). 1969). Henry Mountains P e t e r s o n (19 ( 1 9 669 9 )) divided d i v i d e d the t h e Straight S t r a i g h t Cliffs C l i f f s Formation F o r m a t i o n into into Pei::e::-:son f o u r formal f o r m a l r.lembers. members. four T h e s e members are a r e easily e a s i l y recognized r e c o g n i z e d in i n the the These P arr ia i a area a r e a and are a r e in i n 'a.scendir..g s c e n d i n g order o r d e r tr..e t h e Tibb T i b b e t Canyon Hember Member,, the the Pa. Smoky RQllo~'l H o l l o w 1·relil.ber Member,, the t h e John J o h n Henry H e n r y Hember, Member, and t hhe e Drip D r i p Tank Tank member. mem.ber. 109 109 ^ ^ g f ^ C Canyon a n v o n Member The T Tibbet Canyon Member of Formation i b b e t Canyon of tthe h e Straight S t r a i g h t Cliffs Cliffs F o r m a t i o n is is a s a l member of tthe h e formation f o r m a t i o n tthroughout h r o u g h o u t tthe h e Kaiparowits K a i p a r o w i t s region. region. the bbasal member of I t is i s 100 feet f e e t thick t h i c k in i n tthe h e Paria P a r i a area a r e a and forms f o r m s a cliff c l i f f or o r hogback, hogback, It l o w e s t escarpment e s c a r p m e n t of of the the B righam P l a i n s (fig. ( f i g . 22). 22), the lowest Brigham Plains The Tibbet T i b b e t Canyon Canyon Member is i s a ggrayish-orange r a y i s h - o r a n g e tto o yellowish-gray, yellowish-gray, f i n e to t o medium-grained m e d i u m - g r a i n e d sandstone s a n d s t o n e with with m i n o r , tthin hin m u d s t o n e layers. layers. fine minor, mudstone S o r t i n g is i s generally g e n e r a l l y fair; f a i r ; some bbeds e d s aare re w e l l sorted. sorted. Sorting well The llower o w e r part part of the t h e member iis s generally g e n e r a l l y thin t h i n tto o medium edded w i t h ripple ripple of medium bbedded with l a m i n a t i o n s , rripple ipple m a r k s , small s m a l l two-inch-deep t w o - i n c h - d e e p channels channels w i t h cut c u t and and laminations, marks, with f i l l structures, s t r u c t u r e s , and and abundant a b u n d a n t burrows, b u r r o w s , tracks, t r a c k s , trails, t r a i l s , and worm(?) worm(?) fill tubes. tubps. The uupper p p e r ppart a r t of of the t h e member ecomes m o r e massive; m a s s i v e ; troughtroughmember bbecomes more c r o s s stratifications s t r a t i f i c a t i o n s are a r e seen. seen. type cross o w e r contact c o n t a c t is i s gradational gradational The llmver i n t e r t o n g u e d with w i t h tthe h e Tropic T r o p i c Shale; S h a l e ; the t h e uupper p p e r contact c o n t a c t is i s sharp sharp and intertongued but p r o b a b l y conformable c o n f o r m a b l e and pplaced l a c e d at a t tthe h e llowest o w e s t shale s h a l e or o r coal c o a l in in but probably t h e Smoky Hollow H o l l o w Member. Member. the The only o n l y fossils f o s s i l s (other ( o t h e r tthan h a n those t h o s e mentioned m e n t i o n e d above) a b o v e ) found f o u n d in i n the th T i b b e t Canyon i n tthe h e Paria P a r i a area a r e a aare r e several s e v e r a l ppoorly o o r l y preserved preserved Tibbet Canyon Member in i n o c e r a m i d ( ? ) ppelecypods. elecypods. inoceramid(?) M a r i n e fossils f o s s i l s found f o u n d elsewhere e l s e w h e r e correlate correlate Harine t h e Tibbet T i b b e t Canyon Canyon Member w i t h tthe he B l u e Hill H i l l Shale S h a l e Member of the the the Hember ''lith Blue Member of C a r l i l e Shale S h a l e (Turonian) ( T u r o n i a n ) in i n tthe h e standard s t a n d a r d rreference e f e r e n c e ffor o r tthe h e Western Western Carlile I n t e r i o r (Peterson, ( P e t e r s o n , 1969, 1 9 6 9 , p. p . J6). J6). Interior !noky Saoky Hollow H o l l o w Hember Member The Smoky H Hollow Cliffs o l l o w Member of of tthe h e Straight Straight C l i f f s Forma.tion F o r m a t i o n is is 110 s n d and shale s h a l e sequence s e q u e n c e with w i t h local l o c a l coal. coal. a sand p t h r o u g h o u t the. K a i p a r o w i t s rregion. egion. throughout the Kaiparowits c a n be b e traced traced The member can I t fforms o r m s a slope s l o p e and s t e p sequence sequence It and step t h e ccliff-forming l i f f - f o r m i n g Tibbet T i b b e t Canyon Canyon Member unconformably above the Member and unconformably u n d e r l i e s tthe h e John John H e n r y Member. underlies Henry The member i s 217 feet f e e t tthick h i c k aalong l o n g the the member is Brigham Plains P l a i n s Jeep J e e p Road. Road. Brigham The Smoky Hollmv H o l l o w Member is i s an a n orangish-gray o r a n g i s h - g r a y carbonaceous carbonaceous mudstone with w i t h several s e v e r a l 88 - to t o 12-foot-thick 1 2 - f o o t - t h i c k grayish-orange g r a y i s h - o r a n g e sandstones. sandstones. mudstone The mudstone m u d s t o n e (often ( o f t e n talus t a l u s covered) c o v e r e d ) is i s generally g e n e r a l l y sandy--some s a n d y — s o m e of of iit t is is r e s i s t a n t enough e n o u g h tto o form form low low cliffs c l i f f s (fig. ( f i g . 22). 22). resistant Much of i t is is of it carbonaceous and tthree c a r b o n a c e o u s and h r e e oorr four f o u r thin t h i n ((1-5 1 - 5 iinches n c h e s tthick) h i c k ) ccoal o a l seams seams were seen. seen. The sandstone s a n d s t o n e iis s ppoorly o o r l y sorted, s o r t e d , cross c r o s s stratified, s t r a t i f i e d , and and contains minor c o n t a i n s many m i n o r uunconformities. nconformities. The grain g r a i n size s i z e is i s coarser c o a r s e r than than that t h a t of of tthe h e uunderlying n d e r l y i n g Tibbet T i b b e t Canyon Canyon Member. Member. Hollow Member has The uupper-most p p e r - m o s t sandstone s a n d s t o n e of of tthe h e Smoky H o l l o w Member has been called c a l l e d the t h e calico c a l i c o bbed e d by e t e r s o n (1969, ( 1 9 6 9 , pp.. JJ7). 7). been by PPeterson I tt is i s about about I f e e t thick t h i c k aalong l o n g tthe h e Brighom B r i g h a m Plains P l a i n s JJeep e e p Road and i s a coarse c o a r s e to to 20 feet and is c o n g l o m e r a t i c s aandstone n d s t o n e 'vith w i t h blue-gray blue-gray m udchips. conglomeratic mudchips. The calico c a l i c o bed bed c o n t a i n s crossc r o s s - s tratif t r a t i f i ieedd sandstone s a n d s t o n e and and fluvial-type f l u v i a l - t y p e channels. channels. contains Severa of the ember S e v e r a l of of tthe h e s aand n d s ttone o n e unit u n i t ss of t h e Smoky Hollow Hollow M Member can be traced t r a c e d a rround o u n d the t h e Brigham B r i g h a m Plains P l a i n s on aerial a e r i a l pphotogr h o t o g r aaphs p h s and are a r e useful u s e f u l in i n correlation. correlation. Although A l t h o u g h no fossils f o s s i l s d iagnostic i a g n o s t i c of of age age have bbeen Member, iit e e n found f o u n d in i n tthe h e Smoky Hollow Hollow Member, t is i s pprobably r o b a b l y middle middle Turonian T u r o n i a n in i n age a g e (Pet ( P e t e r ssoon, n , 1969, 1 9 6 9 , pp.. J9). J9). John Henry Henry Meni.b~.£ Member ~hn The John J o h n Henr H e n r yy Member i s a slope s l o p e aand c l i f f - f o r m i n g uunit n i t that that Mer:: ber is nd cliff-forming III Ill unconf o r m a b l y unconformably u n d e r l i e s the t h e Drip D r i p Tank Member. underlies u n c o n f o r m i t y at at The unconformity b a s e of of tthe h e John J o h n Henry Henry Hember Member is i s discussed d i s c u s s e d in i n detail d e t a i l by Peterson Peterson the base (1969, p. p . JlO-J14) J 1 0 - J 1 4 ) and apparently a p p a r e n t l y represents r e p r e s e n t s the t h e span s p a n of of time t i m e as as shown in i n tthe h e uupper p p e r ppart a r t of of the t h e Carlile C a r l i l e Shale S h a l e and and the t h e lower l o w e r part p a r t of of the Niobrara N i o b r a r a Formation F o r m a t i o n of of the t h e standard s t a n d a r d reference r e f e r e n c e of of the t h e Western W e s t e r n Interior. Interior. The John Henry John H e n r y Member forms f o r m s a series s e r i e s of of steps s t e p s and and talustaluscovered Plains covered slopes s l o p e s below b e l o w the t h e Brigham Brigham P l a i n s where w h e r e it i t is i s 570 feet f e e t thick. thick. Were it i t nnot o t for f o r the t h e unconformity, u n c o n f o r m i t y , the t h e John J o h n Henry Henry Member would would be difficult Hollow Member--both d i f f i c u l t to t o separate s e p a r a t e from from the t h e Smoky H ollow M e m b e r — b o t h have have similar s i m i l a r lithologies. lithologies. The bbasal a s a l unit u n i t of of the t h e John J o h n Henry Henry Member is i s aa very v e r y coarse c o a r s e grained, g r a i n e d , yellowish-orange, y e l l o w i s h - o r a n g e , poorly-sorted p o o r l y - s o r t e d conglomeratic conglomeratic sandstone s a n d s t o n e about a b o u t 24 feet f e e t thick. thick. The unit u n i t is i s hhighly i g h l y cross c r o s s stratified s t r a t i f i e d with with t r u n c a t i o n s ; it i t is i s well w e l l ccem~nted e m e n t e d with w i t h iron i r o n oxidz o x i d e and and fo~s f o r m s ua many truncations; cliff c l i f f or o r ledge. ledge. The medial m e d i a l sandstone s a n d s t o n e beds b e d s of of tthe h e John J o h n Henry Henry Member are are s i m i l a r but b u t finer f i n e r grained g r a i n e d vJith w i t h much rripple i p p l e lamination. lamination. similar Several Several uppermost sandstone s a n d s t o n e units u n i t s become conglomeratic c o n g l o m e r a t i c with w i t h both b o t h rounded rounded uppermost a n g u l a r sedimentary s e d i m e n t a r y rock r o c k fragments f r a g m e n t s up to t o 1/4 1/4 inch i n c h diameter. diameter. and angular u d s t o n e of of the t h e John J o h n Henry Henry M Member c o n t a i n s abundant a b u n d a n t minor minor The m mudstone ember contains c o a l streaks. streaks. coal Most t h e fine-g f i n e - g rraaiined n e d uunits n i t s appear a p p e a r to t o be b e massive. massive. Nost of of the of tthe Many of h e sandstones s a n d s t o n e s of of the t h e John J o h n Henry H e n r y Member form form key k e y beds beds t h a t are a r e traceable t r a c e a b l e for f o r several s e v e r a l miles m i l e s or o r more m o r e (fig. ( f i g . 24). 24). that A l t h o u g h no economic e c o n o m i c coal c o a l deposits d e p o s i t s are a r e found f o u n d in i n the t h e John John Although Henry Member in where i n the t h e Paria P a r i a area, a r e a , to t o the t h e nnorth o r t h and east east w h e r e the the member was deposited d e p o s i t e d in i n a fluctuating f l u c t u a t i n g marine m a r i n e and continental c o n t i n e n t a l environment, environment, coal c o a l is i s very v e r y iimportant. mportant. IIn n these t h e s e areas a r e a s a fevl few diagnostic d i a g n o s t i c fossils fossils ( P e t e r s o n , 1969, 1 9 6 9 , p. p . J17) J 1 7 ) correlate c o r r e l a t e the t h e John John H e n r y Member w i t h the the · (Peterson, Henry Member -.;vith 112 112 fiddle ~ddle d uupper p p e r pparts a r t s of h e NNiobrara i o b r a r a FFormation o r m a t i o n ((late l a t e Coniacian, Coniacian, and of tthe a n S a n t o n i a n , and a r l y Campanian). Campanian). Santonian, and eearly nDrip r i p Tank Tank Member - The D Drip r i p Tank Tank Member, Member, tthe h e ttop-most o p - m o s t uunit n i t of of tthe h e Straight Straight Cliffs F o r m a t i o n , iis s a ccliff-forming l i f f - f o r m i n g ssandstone a n d s t o n e tthat h a t ssupports u p p o r t s and Cliffs Formation, uunderlies n d e r l i e s tthe he B righam P lains. Brigham Plains. Along h e ssouth o u t h and e a s t ssides i d e s of of Along tthe and east Brigham P l a i n s tthe h e member orms a m a s s i v e ccliff l i f f sseveral e v e r a l hundred hundred Brigham Plains member fforms massive feet Cottonwood Creek f e e t high h i g h (fig. ( f i g . 224); 4 ) ; aalong long C ottonwood C r e e k iit t fforms o r m s a prominent prominent hogback, hogback, tthe h e bbackbone a c k b o n e of of tthe h e Cockscomb. Cockscomb. The mapped mapped area a r e a lacks l a c k s the t h e uupper p p e r 20 to t o 40 ffeet e e t of of the t h e Drip Drip u t tthe h e entire e n t i r e thickness t h i c k n e s s of h e member is i s measured measured Tank Member bbut of tthe e s t i m a t e d to t o bbe e 380 to t o 400 feet. feet. and estimated l i t h o l o g y is i s similar s i m i l a r to to The lithology t h e sandstone s a n d s t o n e in i n the t h e rest r e s t of of the t h e formation. formation. the I t consists c o n s i s t s of of grayishgrayishIt w h i t e to t o tan, t a n , poorly p o o r l y sorted, s o r t e d , massive, m a s s i v e , cross-stratified, c r o s s - s t r a t i f i e d , conglomeratic conglomeratic white sandstone. sandstone. of the t h e sedimentary s e d i m e n t a r y rock r o c k fragments f r a g m e n t s are a r e up to t o 1/2 1/2 Some of i n c h in i n diameter. diameter. inch S e v e r a l beds b e d s are a r e stained s t a i n e d dark-brown d a r k - b r o w n to t o black b l a c k with with Several i r o n oxidE!; o x i d e ; they t h e y ring r i n g ~vhen when struck s t r u c k with w i t h a hammer. hammer. iron Most of of the t h e cross c r o s s stratifications s t r a t i f i c a t i o n s are a r e of of the t h e small s m a l l scale scale Host t r o u g h type--channe t y p e - — c h a n n eIs l s and minor m i n o r dias d i a s tterns e m s are a r e conm common t h r o u g h o u t. t. trough lOn throughou The The becomes thinner t h i n n e r at a t the t h e top t o p and the t h e grain g r a i n size s i z e decreases. decreases. bedding becOi1les b a s a l contact c o n t a c t is i s arbitrarily a r b i t r a r i l y placed p l a c e d at a t the t h e tope t o p e of of the the The basal last l a s t mudstOIle m u d s t o n e in i n the t h e John J o h n Henry H e n r y Hember. Member. The contact c o n t a c t with w i t h the t h e overlying overlying 101ahweap Wahweap Form:ltion F o r m a t i o n is i s grad~tional g r a d a t i o n a l and in i n places p l a c e s the t h e two interfinger interfinger ( P e t e r s o n , 1 9 6 9 , p. p . J18). J18). (Peterson,1969, - 113 Diagnostic D i a g n o s t i c fossils f o s s i l s have h a v e not n o t bbeen e e n found f o u n d in i n the t h e Drip D r i p Tank Tank o r the t h e overlying o v e r l y i n g Wahweap--but Wahweap—but the the D r i p Tank Tank is i s probably probably Member or Drip c o r r e l a t i v e with w i t h the t h e Emery Sandstone S a n d s t o n e Member of of the t h e Mancos Shale S h a l e in in correlative c e n t r a l Utah U t a h and Point P o i n t Lookout L o o k o u t Sandstone S a n d s t o n e in i n tthe h e San San Juan J u a n Basin Basin central ( P e t e r s o n , 1969, 1 9 6 9 , pp.. J20). J20). (Peterson, p p p o s i t i o n a l Environments Environments Depositional As tthe h e Tropic T r o p i c seas s e a s retreated r e t r e a t e d a classic c l a s s i c regressive r e g r e s s i v e marine marine sequence w·as was developed d e v e l o p e d across a c r o s s the t h e Kaiparowits K a i p a r o w i t s region. region. sequence The lower l o w e r part part of of the t h e Tibbet. T i b b e t Canyon Member was deposited d e p o s i t e d in i n a near-shore, n e a r - s h o r e , shallow shallow m a r i n e environment, e n v i r o n m e n t , but b u t towards t o w a r d s tthe h e ttop o p of of the t h e member the t h e energy energy marine i n c r e a s e d and a mixed m i x e d environment e n v i r o n m e n t of of deltas, d e l t a s , bbeaches, e a c h e s , bars, b a r s , and and increased r i v e r s formed. formed. rivers D u r i n g Smoky Hollow H o l l o w deposition d e p o s i t i o n fluvial fluvial During conditions cond~tions p e r s i s t e d in i n the t h e Paria P a r i a area a r e a and and much of of the t h e Kaiparowits K a i p a r o w i t s region, r e g i o n , but but persisted m i l e s to t o the t h e northeast, n o r t h e a s t , marine m a r i n e conditions c o n d i t i o n s still s t i l l existed. existed. a few miles formed bbetween e t w e e n the t h e strand s t r a n d line l i n e and the t h e intense i n t e n s e fluvial fluvial Large swamps formed a c t i o n to\-lards t o w a r d s the t h e southwest s o u t h w e s t nearer n e a r e r the t h e source s o u r c e area. area. action I n some areas areas In c o a l developed. developed. coal n c o n f o r m i t y was created c r e a t e d before b e f o r e the t h e next n e x t marine m a r i n e transgression transgression An uunconfonnity deposited d e p o s i t e d the t h e John J o h n Henry H e n r y Member (Peterson, ( P e t e r s o n , 1969, 1 9 6 9 , p. p . J15). J15). This T h i s member member is i s ppredominantly r e d o m i n a n t l y non-marine n o n - m a r i n e in i n tthe h e southwestern s o u t h w e s t e r n Kaiparowits K a i p a r o w i t s region-region— the and predominantly t h e Paria P a r i a area, a r e a , and p r e d o m i n a n t l y marine m a r i n e in i n the t h e northeastern northeastern Kaiparowits K a i p a r o w i t s region----along r e g i o n — a l o n g tthe h e Straight S t r a i g h t Cliffs C l i f f s escarpment e s c a r p m e n t (Peterson," (Peterson, 1969, p. p . JI5). J15). E..xtensive E x t e n s i v e swamps formed formed between b e t w e e n advances a d v a n c e s of of sandstone sandstone that t h a t THere w e r e bbrought r o u g h t on by uplift u p l i f t in i n the t h e source s o u r c e area; a r e a ; some very v e r y good good 114 ii4 ccoal o a l ddepcsits eposits w e r e formed n some reas. were formed iin some aareas. A l t h o u g h ppart a r t of the Although of the John n tthe h e PParia a r i a aarea r e a iis s sshallow hallow m a r i n e , tthe h e most most John Henry Henry Member Member iin marine, pprevalent r e v a l e n t eenvironments n v i r o n m e n t s aare r e ffluvial, l u v i a l , fflood l o o d pplain, l a i n , llagoonal, a g o o n a l , and ppaludal. aludal. The oungest m a r i n e rrocks o c k s of he P a r i a aarea r e a were were The yyoungest marine of tthe Paria ddeposited e p o s i t e d dduring u r i n g JJohn o h n Henry time. Henry time. The D Drip Tank Member Member iis was llaid The r i p Tank s a ffluvial l u v i a l uunit n i t tthat h a t was a i d down in in a continental c o n t i n e n t a l bbasin a s i n that t h a t deepened d e e p e n e d tto o the the w est. west. T h i s basin b a s i n lay l a y at a t the the This f o o t of he S e v i e r oor r IIron ron S p r i n g s uplift. uplift. foot of tthe Sevier Springs Tertiary and Q Quaternary T e r t i a r y and u a t e r n a r y Deposits Deposits Unconsolidated and consolidated of various U n c o n s o l i d a t e d and c o n s o l i d a t e d ssedimentary e d i m e n t a r y rrocks o c k s of various o r i g i n s aare re w i d e l y distributed d i s t r i b u t e d over o v e r tthe h e bbedrock e d r o c k of he P a r i a area. area. origins widely of tthe Paria c a n bbe e divided d i v i d e d into i n t o two groups; g r o u p s ; ddune, u n e , talus, t a l u s , landslide, l a n d s l i d e , sand, sand, These can a l l u v i a l fan f a n and and ppediment e d i m e n t deposits d e p o s i t s derived d e r i v e d from from nnearby e a r b y sedimentary sedimentary and alluvial r o c k s ; and stream s t r e a m deposits d e p o s i t s of of sand s a n d and gravel g r a v e l tthat h a t border b o r d e r streams streams rocks; and cap 1m., low bbuttes u t t e s and hills h i l l s along a l o n g streams, s t r e a m s , the t h e sources s o u r c e s of of the t h e latter latter a r e more distant. distant. are I t is i s very v e r y difficult d i f f i c u l t to t o correlate c o r r e l a t e these t h e s e deposits deposits It r e g i o n a l l y (with ( w i t h the t h e ppossible o s s i b l e exception e x c e p t i o n of of the t h e Tertiary T e r t i a r y conglomerate conglomerate regionally t h a t may be b e related r e l a t e d to t o the t h e Parunuweap P a r u n u w e a p Formation) F o r m a t i o n ) so s o the t h e emphasis e m p h a s i s will will that d e s c r i p t i o n , distribution, d i s t r i b u t i o n , and a n d origin. origin. be on description, g e o l o g i c ages a g e s of of these t h e s e deposits d e p o s i t s can c a n be b e estimated e s t i m a t e d only only The geologic roughly r o u g h l y because b e c a u s e of of lack l a c k of of fossils f o s s i l s and lack l a c k of of r eegional g i o n a l correlation, correlation, however, h o w e v e r , their t h e i r relative r e l a t i v e ages a g e s can c a n be b e worked w o r k e d out o u t "lith w i t h some certainty. certainty. The alluvial a l l u v i a l fans, f a n s , pediments, p e d i m e n t s , and terraces t e r r a c e s were w e r e formed f o r m e d at a t a time time when the t h e cl:i..mate c l i m a t e was more m o r e humid, h u m i d , and they t h e y are a r e now undergoing u n d e r g o i n g dissection dissection 115 115 and erosion by m modern e r o s i o n by o d e r n arid a r i d processes. processes. The alluvial a l l u v i a l stream s t r e a m deposits, deposits, d e p o s i t s are a r e forming f o r m i n g today t o d a y and and are a r e the t h e results r e s u l t s of of the the sand, and dune deposits c l i m a t e and topography. topography. modern climate l a n d s l i d e s are a r e pprobably r o b a b l y interinter­ The landslides m e d i a t e in i n age--though a g e — t h o u g h a more m o r e humid humid climate c l i m a t e is i s favorable f a v o r a b l e to t o their their mediate f o r m a t i o n , they t h e y are a r e certainly c e r t a i n l y still s t i l l forming f o r m i n g at a t ppresent. resent. formation, The age a g e of of t h e Toreva-block T o r e v a - b l o c k landslides l a n d s l i d e s is i s more m o r e difficult d i f f i c u l t to t o establish. establish. the They They a r e covered c o v e r e d in i n ppart a r t by alluvium a l l u v i u m and and other o t h e r landslide l a n d s l i d e deposits d e p o s i t s and and are t h e r e f o r e ppredate r e d a t e these t h e s e deposits. deposits. therefore T e r t i a r y conglomerate c o n g l o m e r a t e is is The Tertiary p r o b a b l y related r e l a t e d to t o the t h e Parunuweap P a r u n u w e a p Formation F o r m a t i o n of of Pliocene P l i o c e n e age. age, probably Tertiary~Quaternary Cortglomerate-~Panintiweap Tertiary-Quaternary C o n g l o m e r a t e — - P a r u n u w e a p ((?) ?) Formation Formation One small s m a l l outcrop, o u t c r o p , about a b o u t half h a l f a mile m i l e south\ITest s o u t h w e s t of of the the c e m e t e r y nnear e a r Paria P a r i a (fig. ( f i g . 9) is i s the t h e only o n l y rremains e m a i n s of of a fluvial fluvial cemetery c o n g l o m e r a t e of of possible p o s s i b l e Pliocene P l i o c e n e age a g e that t h a t may correlate c o r r e l a t e vlith w i t h the the conglomerate F o r m a t i o n (Da1ness, ( D a l n e s s , 1969). 1969). Parunuweap Formation P a r u n u w e a p Formation F o r m a t i o n is is The Parunuweap w i d e l y distributed d i s t r i b u t e d along a l o n g streams s t r e a m s in i n southwestern s o u t h w e s t e r n Utah U t a h especially e s p e c i a l l y in in widely t h e Zion Z i o n rregion. egion. the c o n g l o m e r a t e in i n the t h e Paria P a r i a area a r e a is i s a wellwellThe conglomerate cemented red r e d conglomerate c o n g l o m e r a t e that t h a t caps c a p s a small s m a l l butte b u t t e of of the t h e Monitor Monitor cemented B u t t e Member of of the t h e Chinle C h i n l e Fonnation. Formation. Butte p e b b l e s range r a n g e up to to The pebbles s e v e r a l iinches n c h e s across; a c r o s s ; most m o s t are a r e disk-shape d i s k - s h a p e and triangular t r i a n g u l a r in i n outline. outline. several l a r g e r pebbles p e b b l e s 'ITere w e r e all a l l derived d e r i v e d from from the t h e Glen G l e n Canyon Group. Group. The larger The c o n g l o m e r a t e is i s cemented cemented w i t h a brick-red b r i c k - r e d silt s i l t matr-ix m a t r i x (the ( t h e color c o l o r of conglomerate with t h e Moenkopi Fo~mation F o r m a t i o n or o r pparts a r t s of of the t h e Moni M o n itor t o r Butte). Butte). the Coarse Coarse m a t e r i a l includes i n c l u d e s quartz q u a r t z sand s a n d g rains, r a i n s , che c h e rt r t pebbles, p e b b l e s , ppetrified e t r i f i e d wood material from tthe h e Chinle, C h i n l e , cobbles c o b b l e s from from the t h e Moenave, M o e n a v e , Kayenta, K a y e n t a , and Navajo Navajo from 116 Formations, F o r m a t i o n s , and other o t h e r miscellaneous m i s c e l l a n e o u s sedimentary s e d i m e n t a r y rock r o c k ffragments. ragments. No v o l c a n i c pparticles a r t i c l e s were w e r e seen. seen. volcanic About t o 15 feet f e e t of of tthe h e conglomerate c o n g l o m e r a t e remains. remains. About 12 to IItt displays displays p r i m i t i v e bedding b e d d i n g and nnumerous u m e r o u s channels c h a n n e l s with w i t h 1 to t o 2 ffeet e e t of relief. primitive of relief. e n t i r e uunit n i t is i s very v e r y well w e l l cemented c e m e n t e d and lies l i e s unconformably u n c o n f o r m a b l y on the the The entire Monitor Butte. Butte. Monitor e l i e f developed d e v e l o p e d on o n tthe h e Monitor Monitor B u t t e iis s not not The rrelief Butte v e r y great; g r e a t ; the t h e contact c o n t a c t is i s a rolling r o l l i n g surface s u r f a c e with w i t h 6 iinches n c h e s tto o a foot foot very elief. of rrelief. of The total t o t a l area a r e a of of outcrop o u t c r o p is i s several s e v e r a l . hundred h u n d r e d square s q u a r e yards. yards. The altitude a l t i t u d e of of the t h e outcrop o u t c r o p is i s 5015 feet f e e t -— 295 ffeet e e t above above the t h e ppresent r e s e n t Paria P a r i a River R i v e r and a n d almost a l m o s t 200 feet f e e t above a b o v e the t h e terrace-· terrace-· pediment pediment deposits d e p o s i t s along a l o n g the t h e back b a c k of of the t h e Cockscomb. Cockscomb. Fifteen F i f t e e n miles miles down river of this r i v e r in i n the t h e lower l o w e r Paria P a r i a Canyon Canyon more outcrops o u t c r o p s of this conglomerate a r e present. present. c o n g l o m e r a t e are These of aabout T h e s e are a r e at a t an a n elevation e l e v a t i o n of b o u t 4800 feet f e e t or o r 400 feet f e e t above a b o v e the t h e present p r e s e n t Paria P a r i a River R i v e r at a t that t h a t location. location. c o n g l o m e r a t e is i s undoubtedly u n d o u b t e d l y fluvial f l u v i a l and related r e l a t e d tto o tthe h e PliocenePlioceneThe conglomerate P l i e s t o c e n e drainage d r a i n a g e system s y s t e m of of the t h e area. area. P1iestocene T h a t tthese h e s e two ooutcrops u t c r o p s are are That along the t h e present present P a r i a River R i v e r indicates i n d i c a t e s that t h a t the t h e Faria P a r i a drainage d r a i n a g e system system along Paria was well w e l l established e s t a b l i s h e d in i n Pliocene-Pleistocene P l i o c e n e - P l e i s t o c e n e time t i m e along a l o n g tthis h i s ppart a r t of of i t s course. course. 'its F u r t h e r comments comments on tthe h e significance s i g n i f i c a n c e of of tthis h i s conglomerate conglomerate Further a r e given g i v e n in i n the t h e section s e c t i o n on o n geomorphology. geomorphology. are Terrace T e r r a c e and Pedini.elitDeecisits Pediment D e p o s i t s t h e back b a c k of of tthe h e Cockscomb south s o u t h of tthe he P aria R i v e r the the Along the Paria River steeply s t e e p l y dipping d i p p i n g strata s t r a t a of of the t h e San Rafael R a f a e l Group, G r o u p , tthe h e Dakota D a k o t a Formation, Formation, and Tropic T r o p i c Sha.le S h a l e arc: a r e truncated t r u n c a t e d and overlain o v e r l a i n by b y a vvery e r y gently g e n t l y dipping, dipping, ' 117 bedded bedded deposit d e p o s i t of of sand s a n d and and gravel. gravel. The average a v e r a g e elevation e l e v a t i o n of of the the b a s e of of this t h i s deposit d e p o s i t is i s slightly s l i g h t l y more more tthan h a n 4800 feet. feet. base IIt t consists consists of sedimentary s e d i m e n t a r y ppebbles e b b l e s and and cobbles c o b b l e s rranging a n g i n g tto o several s e v e r a l feet f e e t in in of diameter. diameter. a v e r a g e pebble p e b b l e is i s aabout b o u t 1 iinch n c h in i n diameter. diameter. The average The d e p o s i t s are a r e composed l t e r n a t i n g bbeds e d s of of cconglomerate o n g l o m e r a t e (with ( w i t h sand sand deposits composed of of aalternating silt m a t r i x ) , fine f i n e sand, s a n d , and silt. silt. and silt matrix), c o n s o l i d a t e d and i s cross c r o s s stratified. stratified. consolidated and is s e c o n d a r y calcite. calcite. secondary The uunit n i t iis s weakly weakly A l s o ppresent r e s e n t aare r e llenses e n s e s of of Also A l t h o u g h much of of the t h e bbedding e d d i n g iindicates n d i c a t e s fluvial fluvial Although d e p o s i t i o n , ppebbles e b b l e s nnear e a r tthe h e Cockscomb Cockscomb aare r e almost a l m o s t eentirely n t i r e l y from from the the deposition, Navajo Sandstone S a n d s t o n e -— ppebbles e b b l e s on tthe h e Tropic T r o p i c Shale S h a l e are a r e mostly m o s t l y derived derived Navajo from tthe he D akota F o r m a t i o n and and T r o p i c Shale. Shale. from Dakota Formation Tropic T h i s distribution d i s t r i b u t i o n of This l o c a l l y derived d e r i v e d ppebbles e b b l e s seems tto o point p o i n t tto o a ppediment-type e d i m e n t - t y p e origin. origin. locally The ttop o p of of tthese h e s e dcieposits e p o s i t s iis s bblanketed lanketed w i t h a rrecent e c e n t sand s a n d ccover o v e r 80 so with t h e thickness t h i c k n e s s of of the t h e deposits d e p o s i t s are a r e ddifficult i f f i c u l t tto o m e a s u r e bbut u t it i t probably probably the measure a p p r o a c h e s 100 ffeet e e t near n e a r tthe h e Cockscomb. Cockscomb. approaches At the t h e ttime i m e of d e p o s i t i o n , the t h e Paria Paria R i v e r occupied o c c u p i e d a broad broad of deposition, River f l o o d - p l a i n at a t rroughly o u g h l y tthe h e eelevation l e v a t i o n of of the t h e terraces. terraces. flood-plain climate The climate h a n it i t is i s ttoday o d a y and e r o s i o n was m o r e rrapid. apid. was more more humid humid tthan and erosion more Fluvial Fluvial e d i m e n t processes p r o c e s s e s ttruncated r u n c a t e d tthe h e soft s o f t San San R a f a e l and Cretaceous and ppediment Rafael and Cretaceous s e d i m e n t s and and ext e x t eensiv n s i v ee pediments p e d i m e n t s and terraces w e r e developed. developed. sediments and terraces were P e r h a p s the t h e alternating a l t e r n a t i n g fine f i n e and c o a r s e deposits d e p o s i t s indicate i n d i c a t e a fluctuating fluctuating Perhaps and coarse c l i m a t e or o r periods p e r i o d s of o r e extensive e x t e n s i v e fluvial f l u v i a l aaction. ction. climate of m more As tthe h e climate climate became more arid a r i d and h e bbase a s e level l e v e l was llm.,rered, o w e r e d , tthe h e deposits d e p o s i t s were were and tthe d i s s e c t e d and and partially p a r t i a l l y covered c o v e r e d with w i t h sand s a n d deposits. deposits. dissected 118 118 L a n d s l i d e and alus D e p o s i t s and T o r e v a - b l o c k s Landslide and T Talu8 Dep08itsartdToreva~blocks - Though by by no no means means rrare, Though a r e , llandslide a n d s l i d e ddeposits e p o s i t s aare r e nnot o t aas s common iin n tthe he P a r i a aarea r e a aas s m i g h t bbe e eexpected. xpected. Paria might ttalus a l u s ddeposits. eposits. P a r i a aarea. rea. Paria The a n bbe e ssaid a i d for for The same ccan Two ttypes y p e s of a n d s l i d e ddeposits e p o s i t s aare r e ffound o u n d iin n the the of llandslide The ffirst i r s t iis s a ppoorly o o r l y sorted s o r t e d rrubble u b b l e tthat h a t llies i e s at a t the the foot of liffs. foot of ccliffs. T h e s e ddeposits e p o s i t s formed a s s e s of sedimentary These formed when when m masses of sedimentary rock bbroke r o k e loose l o o s e from c l i f f and h a t t e r e d aas s tthey h e y fell. fell. rock from a cliff and sshattered They are They are h e ffoot o o t of of tthe h e Cockscomb Cockscomb w h e r e ttheir h e i r movement most common carunon aatt tthe where movement was f a c i l i t a t e d by h e pplastic l a s t i c nnature a t u r e of of tthe he C h i n l e Formation. Formation. facilitated by tthe Chinle The second s e c o n d ttype y p e of of landslide l a n d s l i d e ddeposit e p o s i t is i s tthe h e Toreva-block. Toreva-block. T o r e v a - b l o c k s are a r e formed formed when a llarge a r g e block b l o c k of of sedimentary s e d i m e n t a r y rock rock Toreva-blocks br.eaks b r e a k s lloose o o s e from from a cliff, c l i f f , slides s l i d e s downward, and and rotates r o t a t e s but b u t does does not not break b r e a k up as a s ddoes o e s a typical t y p i c a l landslide. landslide. large l a r g e enough e n o u g h to t o bbe e mapped. mapped. Two Toreva-blocks T o r e v a - b l o c k s are are The largest l a r g e s t one, o n e , almost a l m o s t 2000 feet f e e t long, long, consists c o n s i s t s of of Moenave and Kayenta K a y e n t a Formations F o r m a t i o n s and is i s related r e l a t e d to t o the the f a u l t s at a t that t h a t locality. locality. numerous faults s e c o n d , smaller s m a l l e r Toreva-block Toreva-block A second, i s locat l o c a t e'3d d 2 miles m i l e s south s o u t h of of Gingham Skirt S k i r t Butte. Butte. is T h i s block b l o c k is is This f e e t long l o n g and is i s also a l s o composed of of Moenave and Kayenta--it K a y e n t a — i t too too 1000 feet i s located l o c a t e d near n e a r a fault. fault. is B o t h the t h e Toreva-block T o r e v a - b l o c k and landslide l a n d s l i d e deposits deposits Both a r e partially p a r t i a l l y covered c o v e r e d by alluvium a l l u v i u m and talus. talus. are p r o b a b l y formed f o r m e d at at They probably t i m e when the t h e climate c l i m a t e was more m o r e humid (Phoenix ( P h o e n i x , 1963, 1 9 6 3 , p. p , 40). 40). a time t a l u s deposits d e p o s i t s are a r e mapped as a s landslide l a n d s l i d e deposits d e p o s i t s because because The talus of the t h e difficulty d i f f i c u l t y of of separating s e p a r a t i n g the t h e two when they t h e y are a r e covered c o v e r e d by by of o r alluvium a l l u v i u m as a s i s ofte o f t e nn the t h e case c a s e in i n the t h e Paria P a r i a area a r e a .. sand or Talus Talus d e p o s i t s are a r e well w e l l displayed d i s p l a y e d along a l o n g t hhe e southern s o u t h e r n end e n d of of Brigham B r i g h a m Plains Plains depOSits 119 ii9 where o u s e - s i z e d bblocks l o c k s of traight C liffs F o r m a t i o n hhave a v e tumbled tumbled where hhouse-sized of SStraight Cliffs Formation down oover Tropic Shale. down v e r tthe he T ropic S hale. Although A l t h o u g h tthis h i s ddeposit e p o s i t iis s ffairly a i r l y large large mapped. iit t iis s nnot o t ddense e n s e eenough n o u g h tto o bbe e m apped. Other O t h e r ttalus a l u s ddeposits e p o s i t s aare r e found found Adairville Canyon nnear and on on tthe west of Fivemile iin n A d a i r v i l l e Canyon e a r tthe h e dditch, i t c h , and he w e s t sside i d e of Fivemile Valley of tthe Cockscomb. V a l l e y aalong l o n g tthe h e bbase a s e of he C ockscomb. These T h e s e ddeposits e p o s i t s aare r e forming forming a t present. present. at A l l u v i a l Fan Deposits Alluvial FartDeposits Alluvial well of the A l l u v i a l ffan a n deposits d e p o s i t s aare re w e l l developed d e v e l o p e d at a t tthe h e ffoot o o t of the h e r e tthey h e y cover c o v e r tthe h e soft soft T r i a s s i c strata. strata. Cockscomb w where Triassic T h e s e deposits deposits These c o n s i s t of o o r l y - s o r t e d , angular a n g u l a r fragments f r a g m e n t s of of sedimentary s e d i m e n t a r y rrock o c k and and consist of ppoorly-sorted, sand. sand. They aare r e coarser c o a r s e r nnear e a r the t h e Cockscomb and and become i n e r (with (with They become ffiner f l u v i a l characteristics) c h a r a c t e r i s t i c s ) away from from it. it. more fluvial Sand Gulch G u l c h and Pvobinson Sand and Robinson Creek Creek flow f l o w down the t h e middle m i d d l e of of this t h i s deposit d e p o s i t and hhave a v e cut c u t down into into t h e alluvial a l l u v i a l fan f a n deposits d e p o s i t s as a s much as a s 15 feet. feet. the o n e time t i m e these these At one d e p o s i t s were w e r e more extensive e x t e n s i v e in i n the t h e western w e s t e r n part p a r t of of tthe h e map area area deposits but b u t have h a v e be2n b e e n eroded e r o d e d by stream s t r e a m rejuvenation. rejuvenation. Most of of tthe h e alluvial alluvial f a n deposits d e p o s i t s of of the t h e Paria P a r i a area a r e a are a r e densely d e n s e l y covered covered w i t h sage s a g e and have have fan with s c a t t e r i n g s of of pinyon p i n y o n and jjuniper u n i p e r trees. trees. scatterings Fluvial F l u v i a l Deposits Deposits All A l l the t h e major m a j o r stream s t r e a m courses c o u r s e s of of the t h e Paria P a r i a ar2a, a r e a , both b o t h perennial perennial i n t e r m i t t e n t , are a r e choked c h o k e d \vith w i t h alluvium. alluvium. and intermittent, of the t h e streams s t r e a m s in in Many of the t h e area. area, are a r e subject s u b j e c t to t o violent v i o l e n t flashfloods f l a s h f l o o d s and during d u r i n g these t h e s e periods periods the t h e amount of of material m a t e r i a l in i n transport t r a n s p o r t is i s significant. significant. The flashfloods flashfloods 120 129 material ddie i e qquickly u i c k l y ddropping r o p p i n g ttheir h e i r ssuspended uspended m a t e r i a l aalong l o n g tthe h e sstream t r e a m sides sides and bbottom. and ottom. Although A l t h o u g h tthe h e ffluvial l u v i a l ddeposits e p o s i t s uundoubtedly n d o u b t e d l y contain contain by aa layer ffluvial l u v i a l sstructures, t r u c t u r e s , tthe h e ddeposits e p o s i t s aare r e ggenerally e n e r a l l y ccovered o v e r e d by layer of vvery and a few few sscattered of e r y ffine i n e ssilt i l t oor r ssand a n d and c a t t e r e d cobbles. cobbles. Most ffluvial many aare Most l u v i a l ddeposits e p o s i t s aare r e pprobably r o b a b l y qquite u i t e tthin; h i n ; many r e less less tthan h a n ffive i v e ffeet e e t tthick. hick. Along tthe Paria River Along he P aria R i v e r tthe h e aalluvium l l u v i u m iis s probably probably of 20 ffeet and aatt no pplace on tthe h e oorder r d e r of e e t tthick h i c k and l a c e iis s bbedrock e d r o c k exposed exposed i n tthe h e bot b o t ttom. om. in )ci Wind Deposits Wind Deposits Large, L a r g e , ttowering, o w e r i n g , extensive e x t e n s i v e ssand a n d dune d u n e deposits d e p o s i t s are a r e rrare a r e on t h e Colorado Colorado P lateau. the Plateau. T h i s may seem a pparadox a r a d o x in i n a lland a n d of sandstone This of sandstone e r s i s t a n t winds w i n d s bbut u t erosion e r o s i o n is i s too t o o vviolent i o l e n t and large l a r g e low-lying low-lying and ppersistant f l a t areas a r e a s are a r e uncommon. flat small s m a l l sand s a n d deposits. deposits. But h e pplateau lateau But tthe pprovince r o v i n c e is i s covered c o v e r e d by by many In Paria I n the the P a r i a area a r e a tthese h e s e deposits d e p o s i t s are a r e corrmon common in West Cove, i n Fivemile F i v e m i l e Valley, V a l l e y , West C o v e , and on on the t h e Brigham B r i g h a m Plains. Plains. Most Most of t h e sand, s a n d , though t h o u g h \vind w i n d transported, t r a n s p o r t e d , is i s stabalized s t a b a l i z e d by vegetation v e g e t a t i o n and and the i s less l e s s than t h a n 20 feet f e e t thick, t h i c k , and individual i n d i v i d u a l deposits d e p o s i t s rarely r a r e l y exceed exceed is s e v e r a l acres a c r e s in i n area. area. several F a i r l y extensive e x t e n s i v e sand s a n d deposits d e p o s i t s are a r e seen seen Fairly Brigham Plains P l a i n s bu b u t most m o s t of of these t h e s e are a r e only o n l y a fe~;r few £f eeet e t thick t h i c k and and on Brigham a l m o s t all a l l t.he t h e dunes d u n e s are a r e stabilized s t a b i l i z e d by vegetation v e g e t a t i o n and are a r e rew'orked reworked almost rains. by summer rains. d e p o s i t s are a r e composed of of fine-grained, f i n e - g r a i n e d , palepaleThe deposits o r a n g e , quartz q u a r t z sandstone s a n d s t o n e derived d e r i v e d from the t h e Glen G l e n Canyon and San Rafael Rafael orange, G r o u p s , and the t h e Cretaceous C r e t a c e o u s sandstones. sandstones. Groups, STRUCTURE The sstructure of tthe Paria somewhat aatypical 6f The t r u c t u r e of he P a r i a aarea r e a iis s somewhat t y p i c a l . Of C olorado P l a t e a u sstructure~ tructure. Colorado Plateau The m o s t iimpressive m p r e s s i v e ddifference i f f e r e n c e iis s the the most amount a u l t i n g , sshearing, h e a r i n g , and r a c t u r i n g aassociated ssociated w i t h the the amount of of ffaulting, and ffracturing with East aibab m onocline East K Kaibab monocline ((pI. p i . 33). ) . Where r o s s e s the the w'here U. S. Highway Highway 89 ccrosses Cockscomb h e ssouthern o u t h e r n eedge d g e of h e map aarea r e a aalmost l m o s t aall l l of the Cockscomb aatt tthe of tthe of the Chinle of tthe Moenave aare C h i n l e and and ppart a r t of h e Moenave r e ffaulted a u l t e d oout u t _and and tthe h e vertical vertical d i s p l a c e m e n t ddue u e tto o ffaulting a u l t i n g iis s aalmost l m o s t 1600 1600 feet. feet. displacement The ttotal o t a l amount amount of structural s t r u c t u r a l rrelief e l i e f bbetween e t w e e n tthe h e ccrest r e s t of of tthe he K a i b a b uupwarp p w a r p on of Kaibab Fivemile M o u n t a i n and he K a i p a r o wits i t s bbasin a s i n aatt tthe h e southern s o u t h e r n end end of of Fivemile Mountain and tthe Kaiparowt h e Brigham Brigham P l a i n s is i s about a b o u t 7000 feet; f e e t ; this t h i s ooccurs ccurs w i t h i n a distance distance the Plains within of 6 m iles. of miles. B o t h the t h e amount of faulting f a u l t i n g and the t h e total t o t a l structural structural Both amount of r e l i e f are a r e considerably c o n s i d e r a b l y more m o r e than t h a n previous p r e v i o u s workers w o r k e r s had h a d thought. thought. relief Folding Folding · EastKaibabU~ E a s t K a i b a b UpWarp The East E a s t Kaibab K a i b a b upwarp, u p w a r p , which w h i c h forms f o r m s the t h e Kaibab K a i b a b Plateau, P l a t e a u , is is an asymmetrical a s y m m e t r i c a l anticline a n t i c l i n e that t h a t plunges p l u n g e s in i n a northerly n o r t h e r l y direction. direction. It It is i s convenient c o n v e n i e n t to t o refer r e f e r to t o this t h i s structure s t r u c t u r e in i n the t h e Paria P a r i a area a r e a as a s the the Fivemile F i v e m i l e Hountain M o u n t a i n anticline; a n t i c l i n e ; the t h e structure s t r u c t u r e is i s clearly c l e a r l y exposed e x p o s e d at at Fivemile F i v e m i l e Mountain. Mountain. The trace t r a c e of of the t h e axial a x i a l plain p l a i n enters e n t e r s the t h e map arp.a area j u s t south s o u t h of of Sand Gulch G u l c h and leaves l e a v e s the t h e area a r e a jjust u s t west w e s t of of Paria. Paria. just a x i s plunges p l u n g e s northward n o r t h w a r d at a t about a b o u t 900 feet f e e t per p e r 4 miles m i l e s between b e t w e e n U. S. S. The axis t h e foot f o o t of of the t h e Vermilion V e r m i l i o n Cliffs C l i f f s (a ( a dip d i p of about a b o u t 33 Highway 89 and the degrees). degrees). 122. 122. Kaibab The uuplift p l i f t iis s bbest e s t eexpressed x p r e s s e d iin n tthe he K a i b a b FFormatio~ o r m a t i o n where where conform tto tthe h e rresistant e s i s t a n t llimestones i m e s t o n e s conform o tthe h e sstructure; t r u c t u r e ; iin n tthe h e softer softer of tthe Hoenkopi and and C Chinle Formations, sstrata t r a t a of h e Moenkopi hinle F o r m a t i o n s , eerosion r o s i o n hhas a s masked masked of tthe tthe h e eeffects f f e c t s of h e aanticline. nticline. The K Kaibab upwarp ccontinues The a i b a b upwarp o n t i n u e s northward northward Glen Canyon Group Group and and ggradually iin n tthe he G l e n Canyon r a d u a l l y ddies i e s oout u t iin n tthe h e Cretaceous Cretaceous strata Paria Valley and M Hoore, s t r a t a iin n tthe h e uupper pper P aria V a l l e y ((Gregory G r e g o r y and o o r e , 11931, 9 3 1 , pp.. 123). 123). The F Fivemile Hountain ivemile M o u n t a i n aanticline n t i c l i n e iis s aasymmetrical--the s y m m e t r i c a l — t h e west west f l a n k generally g e n e r a l l y ddips i p s lless e s s tthan h a n 5 ddegrees e g r e e s and s eexpressed x p r e s s e d aas s far far flank and iis west Johnson C reek. west aass Johnson Creek. e a s t e r n llimb i m b ssteepens t e e p e n s rrapidly a p i d l y with with The eastern d i p s cchanging h a n g i n g from e g r e e s tto o 20 ddegrees e g r e e s in i n lless e s s tthan han a m i l e and dips from 2 ddegrees mile from 20 degrees d e g r e e s up tto o 60 degrees d e g r e e s in i n aa~other n o t h e r mile. mile. from The ffold o l d ddies i e s out out m i l e s east e a s t of of the t h e Paria P a r i a River. River. a few miles East E a s t Kaibab K a i b a b Honocline M o n o c l i n— ,e E a s t Kaibab K a i b a b monocline m o n o c l i n e is i s one of of the t h e major m a j o r structural structural The East elements e l e m e n t s of of the t h e Colorado C o l o r a d o Plateau; Plateau; it i t defines d e f i n e s the t h e western w e s t e r n margin margin of of the t h e Paria P a r i a Platfonfi P l a t f o r m (Plateau) ( P l a t e a u ) and Kaiparowits K a i p a r o w i t s basin. basin. dominates d o m i n a t e s the t h e Paria P a r i a area a r e a and forms f o r m s the t h e Cockscomb. The structure structure In I n the t h e Paria P a r i a area area the t h e structu. s t r u c t u rree is i s a single s i n g l e monoclinal m o n o c l i n a l flexure, f l e x u r e , but b u t in i n the t h e Grand Grand Canyon Canyon r e g i o n to t o the t h e south s o u t h it i t has h a s several s e v e r a l branches b r a n c h e s (Babenroth ( B a b e n r o t h and Strahler, Strahler, region 1945). 1945). t o t a l structural s t r u c t u r a l relief r e l i e f betHeen b e t w e e n Fivemi1e F i v e m i l e Hountain M o u n t a i n and and The total t h e Brigham Plains P l a i n s is i s ab a b out o u t 7000 feet. feet. the Most of of the t h e f oolding l d i n g (and faulting) f a u l t i n g ) of of the t h e East E a s t Kaibab K a i b a b Nonocline Monocline Host t a k e s pl p l aace c e within w i t h i n a zone z o n e one o n e mile m i l e ~·lide. wide. takes g e n t l e r than t h a n the t h e synclin3l s y n c l i n a l bend. bend, gentler a n t i c l i n a l bend b e n d is is The anticlinal t h e anticlinal a n t i c l i n a l bend, b e n d , dips dips Along the 123 change from from a few few degrees d e g r e e s tto o about a b o u t 10 degrees d e g r e e s in i n a little l i t t l e less l e s s than t h a n aa m i l e and and from from 10 degrees d e g r e e s to t o maximum dip d i p (about ( a b o u t 45 to t o 60 degrees) d e g r e e s ) in in mile t h r e e - q u a r t e r s of of a mile. mile. three-quarters A l o n g the t h e synclinal s y n c l i n a l bend b e n d dips d i p s change c h a n g e from from Along o r more degrees d e g r e e s tto o approximately a p p r o x i m a t e l y 10 degrees d e g r e e s in i n several s e v e r a l hundred hundred 45 or y a r d s and from from 10 degrees d e g r e e s to t o 2 or o r 3 degrees d e g r e e s in i n several s e v e r a l hundred h u n d r e d more more yards yards. yards. T h i s sharper s h a r p e r synclinal s y n c l i n a l bend b e n d is i s common on many of of the t h e larger larger This m o n o c l i n e s of of tthe h e Colorado Colorado P l a t e a u (Kelley, ( K e l l e y , 1955a, 1 9 5 5 a , p. p . 794). 794). monoclines Plateau The large l a r g e amount amount of of shearing s h e a r i n g and and faulting f a u l t i n g of of tthe h e East E a s t Kaibab Kaibab monocline Paria m o n o c l i n e in i n the the P a r i a area a r e a (which ( w h i c h will w i l l be b e discussed d i s c u s s e d later) l a t e r ) is is definitely d e f i n i t e l y atypical, a t y p i c a l , tthough h o u g h nnot o t uunique, n i q u e , of of plateau p l a t e a u monoclines. monoclines. The narrowness n a r r o w n e s s or o r abruptness a b r u p t n e s s of of tthe h e monocline m o n o c l i n e is i s spectacular; s p e c t a c u l a r ; the t h e entire entire section s e c t i o n from from Permian P e r m i a n to t o Cretaceous C r e t a c e o u s is i s exposed e x p o s e d across a c r o s s its i t s flank f l a n k in in l e s s tthan h a n 3 miles. miles. less The geologic g e o l o g i c outcrop o u t c r o p pattern p a t t e r n of of the t h e rrocks o c k s along a l o n g the t h e East East o n o c l i n e is i s unique; u n i q u e ; the t h e rocks r o c k s outside o u t s i d e of of and and on both b o t h sides s i d e s of Kaibab m monocline t h e structure s t r u c t u r e along a l o n g its i t s entire e n t i r e 150 miles m i l e s length l e n g t h dip d i p to t o the t h e north n o r t h and and the t h u s the t h e monocline m o n o c l i n e is i s iinvolved n v o l v e d in i n pprogre r o g r e ssively s s i v e l y younger y o u n g e r strata s t r a t a in in thus t h a t direction. direction. that T h i s off-sets o f f - s e t s tthe h e geolog g e o l o g ic i c outcrop o u t c r o p pattern p a t t e r n of of all all This t h e formations f o r m a t i o n s 30 to t o 40 miles m i l e s to t o the t h e nnorth o r t h on tthe he w e s t , or o r uplifted uplifted the west, s i d e of of tthe h e monocline. monocline. side r o c k s tto o the t h e east e a s t of of the the m o n o c l i n e dip d i p northward n o r t h w a r d more more The rocks monocline steeply s t e e p l y than t h a n th2 t h e rocks r o c k s to t o the t h e vlest--this w e s t — t h i s [;lay may account a c c o u n t for f o r the t h e follow·ing following s t r u c t u r a l features. features. structural F i r s t this t h i s would would pproduce r o d u c e a shearing s h e a r i n g force force First parallel monocline p a r a l l e l to t o the t h e strike s t r i k e of of the the m o n o c l i n e whhich i c h might m i g h t be b e responsible responsible f o r the t h e intensive i n t e n s i v e shearing s h e a r i n g and fracturing f r a c t u r i n g in i n tthe he N a v a j o Sandstone. Sandstone. for Navajo Second Second 124 124 thiS h i s may account a c c o u n t for f o r the t h e faults f a u l t s that t h a t branch b r a n c h off o f f the t h e main m a i n Cockscomb Cockscomb t f a u l t and hhave a v e anomalous a n o m a l o u s uup-thrown p - t h r o w n eastern e a s t e r n bblocks l o c k s and a n d therefore therefore fault r e p e a t formations f o r m a t i o n s or o r members in i n an a n east-west e a s t - w e s t section. section. repeat F i v e large large Five f a u l t s of of tthis h i s type t y p e ooccur c c u r in i n tthe h e map area. area. faults The East E a s t 'Kaibab K a i b a b monocline m o n o c l i n e trends t r e n d s north n o r t h 10 degrees d e g r e e s east e a s t through through most of of the the P a r i a area. area. Paria N o r t h of of the t h e Paria P a r i a River R i v e r it i t bbends e n d s to t o the the North e a s t and trends t r e n d s north n o r t h 30 degrees d e g r e e s eeast a s t for f o r a few few m i l e s and then t h e n returns returns east miles t o the t h e north n o r t h 10 degrees d e g r e e s east e a s t trend. trend. to IIn n spite s p i t e of of several s e v e r a l other o t h e r such such bends the of the t h e East E a s t Kaibab K a i b a b monocline m o n o c l i n e north n o r t h of t h e Arizona A r i z o n a border, b o r d e r , is i s perhaps perhaps t h e straightest s t r a i g h t e s t of of the t h e plateau p l a t e a u monoclines. monoclines. the I t may bbe e significant significant It t h a t the t h e East E a s t Kaibab K a i b a b monocline m o n o c l i n e is i s pparallel a r a l l e l tto o the t h e Paunsaugunt, P a u n s a u g u n t , Sevier, Sevier, that H u r r i c a n e and Grand Wash f a u l t s and tthe h e spacing s p a c i n g bbetween e t w e e n these these Hurricane and Grand \oJash faults s t r u c t u r e s is i s fair.ly f a i r l y even. even. structures I n addition, a d d i t i o n , the t h e branching b r a n c h i n g of of the the In f a u l t ssystem y s t e m is i s simila s i m i l a r to t o the t h e bbranching r a n c h i n g displayed d i s p l a y e d by by Cockscomb fault t h e s e faults, f a u l t s , especially e s p e c i a l l y the t h e Sevier S e v i e r and and Hurricane H u r r i c a n e faults. faults. these PariaPl P a r i a P l aattfo~'-Kaip f o r m ~ K a i p a rr6\\Tits owits Basin Basin N e a r l y flat-lying f l a t - l y i n g rocks r o c k s to t o the t h e east e a s t of t h e East E a s t Kaibab K a i b a b monocline monocline Nearly of the a r e ppart a r t of of the t h e Par P a r i aa pplatform l a t f o r m and K a i p a rowits r o w i t s bbasin a s i n sstructural tructural are Kaip elements. elements. I t is i s convenient c o n v e n i e n t tto o rrefer e f e r to t o the t h e rrocks o c k s under u n d e r tthe h e Brigham Brigham It Plains of tthe Kaip P l a i n s as a s bbeing e i n g ppart a r t of he K a i p a rowits r o w i t s bbasin a s i n and and the t h e rest r e s t of of the the nearly Pari n e a r l y flat-lying f l a t - l y i n g r oocks c k s .as a s bbeing e i n g ppart a r t of of the the P a r i aa platform. platform. The PParia where a r i a pla p l a ttform f o r m ex e x ttends e n d s iinto n t o northern n o r t h e r n Arizona Arizona w h e r e iit t forms forms th~ the p,qria P a r i a Pl P l a tteau. eau. The rocks r o c k s dip d i p gently g e n t l y to t o the t h e north n o r t h bbut u t are a r e otherwise otherwise s t r u c t u r a l l y uundisturb n d i s t u r b eed. d. structurally E a s t and He West C o v e s and and the the C l a r k Bench are East stCove. Clark Bench are 125 part p a r t of of the t h e Paria P a r i a platform. platform. Because B e c a u s e it i t lacks l a c k s a synclinal s y n c l i n a l axis a x i s iit t is is a t r u e platform p l a t f o r m and not n o t a syncline. syncline. true P a r i a pplatform l a t f o r m iis s bbordered o r d e r e d on The Paria t h e west w e s t by b y the the E a s t Kaibab K a i b a b monocline, m o n o c l i n e , on the t h e east e a s t by b y tthe h e Echo the East m o n o c l i n e , on the t h e north n o r t h by the t h e Kaiparowits K a i p a r o w i t s basin, b a s i n , and a n d on o n tthe h e south south monocline, t h e Vermilion V e r m i l i o n Cliffs C l i f f s and Grand Grand Canyon Canyon uplift. uplift. by the The Kaiparowits K a i p a r o w i t s basin, b a s i n , which w h i c h underlies u n d e r l i e s the t h e Brigham B r i g h a m Plains Plains t h e Kaiparowits K a i p a r o w i t s pplateau, l a t e a u , is i s a structural s t r u c t u r a l basin b a s i n that t h a t iis s crossed crossed and the s e v e r a l small, s m a l l , northwest-trending n o r t h w e s t - t r e n d i n g synclines s y n c l i n e s aand n d anticlines a n t i c l i n e s just just by several e a s t of of the the P a r i a area. area. east Paria s t r u c t u r a l l y lowest l o w e s t area a r e a iin n the the The structurally K a i p a r o w i t s bbasin a s i n is i s several s e v e r a l miles m i l e s northeast n o r t h e a s t of of the t h e Paria P a r i a aarea r e a in in Kaiparowits the t h e headwaters h e a d w a t e r s of of Wahweap and Last L a s t Chance Chance Creeks C r e e k s (Gregory ( G r e g o r y and and Moore, Moore, 1 9 3 1 , p. p . 121). 121). 1931, Faulting Faulting FiVemileVall~'y""yati.lt Fivemile Valley F a u l t . Zone The Fivemile F i v e m i l e Valley V a l l e y fault f a u l t zone z o n e is i s defined d e f i n e d hhere e r e as a s a system. system of nnormal o r m a l faults f a u l t s iin n southern s o u t h e r n Fivemile Fivemile V a l l e y along a l o n g t1le the w e s t edge edge of Valley west of the t h e Cockscomb. Cockscomb, of of the t h e faulting f a u l t i n g is i s seen s e e n in i n the the C h i n l e and Most of Chinle F o r mat a t ions i o n s although a l t h o u g h the t h e zone z o n e ppasses a s s e s into i n t o the t h e Cockscomb Cockscomb Moenkopi Form f a u l t zone z o n e which w h i c h involves i n v o l v e s younger y o u n g e r rocks. rocks. fault m a j o r i t y of of tthe h e faults faults The majority i n Fivemile F i v e m i l e Valley V a l l e y are a r e covered c o v e r e d by alluvium a l l u v i u m and their t h e i r eexistence x i s t e n c e is is in i n f e r r e d from from the t h e map ppattern a t t e r n and and the t h e structural s t r u c t u r a l cross c r o s s sections. sections. inferred The main and is m a i n fault f a u l t lie l i e ss in i n tthe h e Chinle C h i n l e Formation F o r m a t i o n and i s partially partially expo where e x p o sse e dd in i n the t h e area a r e a of of the t h e prospect p r o s p e c t ppit i t approximate a p p r o x i m a t e lly y w h e r e U. S. S. Highvi:a.y scomb. Highway 89 crOS c r o s s3,2 e sS the t h e Cock Cockscomb. The ~vest and the w e s t block b l o c k is i s uupthrown p t h r o w n and the 126 126 Shnabkaib and h e Moenkopi o r m a t i o n aare r e faulted faulted and Upper Upper Red Red Members Members of of tthe ~10enkopi F Formation Shnabkaib aagainst g a i n s t tthe he K ayenta F o r m a t i o n ; tthe h e tthrow h r o w of h e ffault a u l t iis s between between Kayenta Formation; of tthe 1000 and 1600 ffeet e e t aat t tthe h e pprospect r o s p e c t ppit. it. 1000 and 1600 The ault m erges w i t h the the The ffault merges with Cockscomb a u l t zzone one a m i l e tto o tthe h e north. north. Cockscomb ffault mile The oother major one of of tthe The ther m a j o r ffault a u l t iin n tthis h i s zzone o n e iis s one h e five five with ffau1~s a u l t s iin n tthe h e map area area w i t h tthe h e eeast a s t bblock l o c k uupthrown. pthrown. This T h i s fault fault and rrepeats Middle Red, uunderlies n d e r l i e s tthe h e oold l d hhighway i g h w a y and e p e a t s tthe he M iddle R e d , Shnabkaib, S h n a b k a i b , and and Upper Red Members Members of of tthe Moenkopi FFormation. Upper h e Moenkopi ormation. Both major B oth m a j o r ffaults a u l t s are are s t r i k e - p a r a l l e l faults. faults. strike-parallel The FFivemile Valley The ivemile V a l l e y ffault a u l t zzone o n e ccontinues o n t i n u e s tto o tthe h e ssouth o u t h where where the t h e tthrow h r o w of of the t h e fault f a u l t iincreases. ncreases. At At several s e v e r a l localities l o c a l i t i e s the t h e Kaibab Kaibab Fonnation F o r m a t i o n is i s faulted f a u l t e d against a g a i n s t tthe h e Kayenta K a y e n t a Formation. Formation. Cockscomb FFault a u l t System System The entire e n t i r e length l e n g t h of of the t h e Cockscomb on the t h e map area a r e a is i s cut c u t by by f a u l t s and sheer s h e e r zones z o n e s that t h a t parallel p a r a l l e l the t h e strike. strike. faults S e v e r a l faults faults Several b r a n c h off o f f and either e i t h e r parallel p a r a l l e l or o r veer v e e r off o f f the t h e main m a i n trunk t r u n k fault. fault. branch m a i n fault f a u l t has h a s an upthrown u p t h r o w n west w e s t block b l o c k but b u t several s e v e r a l branch b r a n c h faults faults The main o p p o s i t e throws. throws. have opposite South S o u t h of of the t h e triangulation t r i a n g u l a t i o n station, s t a t i o n , VABM VABM Cox, the t h e main m a i n fault fault t h e Kayenta-Navajo K a y e n t a - N a v a j o boundary. boundary. marks the of throw t h r o w is i s estimated estimated The amount of to t o be b e several s e v e r a l hundred h u n d r e d feet f e e t or o r greater. greater. Several S e v e r a l smaller s m a l l e r faults f a u l t s of of unknown thrm·] t h r o w parallel p a r a l l e l the t h e main m a i n fault. fault. m a j o r fault f a u l t is i s responsible r e s p o n s i b l e for f o r Notch N o t c h Canyon. Canyon. A major T h i s is i s one one This of the t h e faults f a u l t s with w i t h the t h e east e a s t block b l o c k upthrown--the u p t h r o w n — t h e Moenave and a n d Kayenta Kayenta of F o r m a t i o n s are a r e repeated. repeated. Formations f a u l t is i s well w e l l exposed, e x p o s e d , the t h e throw t h r o w ii.ss The fault 127 a b o u t 400 feet. feet. about I n the t h e area a r e a of of the t h e VABM VABM Cox, several s e v e r a l faults f a u l t s branch branch In off the t h e main m a i n ttrunk r u n k but b u t their t h e i r tthrow h r o w is i s undeterminable. undeterminable. off North N o r t h of of VABM VABM Cox the t h e faults f a u l t s are a r e more m o r e obscure o b s c u r e but b u t their their l o c a t i o n is i s marked m a r k e d by p r o m i n e n t north-south n o r t h - s o u t h valleys v a l l e y s in i n the t h e Cockscomb. Cockscomb. location by prominent S l o t Canyon is i s tthe h e major m a j o r valley v a l l e y of of this t h i s type. type. Slot t h r o w of of these these The throw f a u l t s is i s probably p r o b a b l y on the t h e order o r d e r of of several s e v e r a l hhundred u n d r e d feet. feet. faults faults Two faults b r a n c h off o f f to t o the the w e s t about a b o u t 2 miles m i l e s south s o u t h of of Gingham Skirt S k i r t Butte--one Butte—one branch west f a u l t trends t r e n d s southwest s o u t h w e s t and and the t h e other o t h e r trends t r e n d s northwest. northwest. fault T h e s e are are These two of of the t h e faults f a u l t s with w i t h the t h e east e a s t block b l o c k on on the t h e uup p tthrown h r o w n side. side. The The f a u l t s repeat r e p e a t the t h e Moenave Formation F o r m a t i o n and and have h a v e an a n estimated e s t i m a t e d maximum faults throw of of several s e v e r a l hundred h u n d r e d feet. feet. throw The Cockscomb fault f a u l t system s y s t e m continues c o n t i n u e s across a c r o s s the t h e Paria P a r i a River River and again a g a i n tthe h e amount amount of of throw t h r o w cannot c a n n o t be b e accurately a c c u r a t e l y detE!rmined d e t e r m i n e d bbut u t when the Navajo measured the N a v a j o was m e a s u r e d in i n Shurtz S h u r t z Gorge, G o r g e , only o n l y 1031 1 0 3 1 feet f e e t ccould o u l d be be measured m e a s u r e d so s o approximately a p p r o x i m a t e l y 800 feet f e e t has h a s been b e e n faulted f a u l t e d out. out. An iinteresting n t e r e s t i n g and well w e l l exposed e x p o s e d fault f a u l t is i s seen s e e n at a t the t h e mouth m o u t h of Shurtz S h u r t z Gorge. Gorge. This T h i s is i s the t h e only o n l y known reverse r e v e r s e fault f a u l t in i n tthe h e Paria P a r i a area. area. f a u l t zone z o n e cuts c u t s the t h e Thousand Thousand Pockets P o c k e t s Tongue of of the t h e Navajo Navajo The fault S a n d s t o n e and c o n s i s t s of of s everal e v e r a l faults f a u l t s tthat h a t appar a p p a r ently e n t l y bbranch r a n c h from from Sandstone and consists t h e main m a i n fault. fault. the f a u l t pplane l a n e dips d i p s aabout b o u t 70 ddegrees e g r e e s to t o the t h e west w e s t and and The fault t h e Thousand Thousand Pockets P o c k e t s Tongue hhas a s overidden o v e r i d d e n the t h e Paria P a r i a River R i v e r Member of the tthe h e Carmel Carmel Formation F o r m a t i o n and loca l o c a lly l l y has h a s caused c a u s e d it i t to t o be b e overturned. overturned. F u r t h e r south s o u t h the t h e fault f a u l t hhas a s cut c u t out o u t the t h e Judd J u d d Hollmv H o l l o w Tongue. Tongue. Further The The of throw t h r o w on this t h i s f.ault f a u l t is i s unknown u t it i t is i s pprob r o b aably b l y less l e s s than than unknown bbut amount of feet. 100 feet. 11'28 28 JJust u s t nnorth o r t h of he m o u t h of hurtz G o r g e aan n uunexposed n e x p o s e d fault fault of tthe mouth of SShurtz Gorge eevfdently v i d e n t l y bbranches r a n c h e s off h e ffault a u l t jjust u s t ddescribed. escribed. off tthe ffault ault w i t h aan n aanomalous n o m a l o u s uupthrown p t h r o w n eeast a s t sside. ide. with eeffects f f e c t s tthe he C armel F ormation. Carmel Formation. T h i s iis s tthe h e fifth fifth This T h i s ffault a u l t apparently apparently This The h r o w aas s shown y the the The Maximum Maximum tthrow shown bby ccross-section r o s s - s e c t i o n iis s aabout b o u t 200 e e t ((pl. p i . 2). 2). 200 ffeet A phenomenon phenomenon of of tthe Cockscomb, tthat known shared A h e Cockscomb, h a t iis s aas s ffar a r aas s known shared with Echo m monocline and reef-like oonly nly w i t h tthe h e Echo o n o c l i n e tto o tthe h e eeast, a s t , aare r e tthe h e vveins e i n s and reef-like masses of ccalcite and llocally m a s s e s of a l c i t e and o c a l l y ssilica i l i c a tthat h a t aare r e cconcentrated o n c e n t r a t e d iin n the the Navajo SSandstone Navajo a n d s t o n e ((Phoenix, P h o e n i x , 1963, 1 9 6 3 , pp.. 449). 9). These of ccrushed T h e s e bbodies o d i e s of r u s h e d and cemented N Navajo Sandstone miles cemented avajo S a n d s t o n e may bbe e up tto o several several m i l e s iin n length length although a l t h o u g h many are a r e short, s h o r t , ddiscontinuous i s c o n t i n u o u s zzones. ones. width of tthe The w i d t h of h e veins veins l i k e w i s e vvaries; a r i e s ; iindividual n d i v i d u a l bbodies o d i e s aaverage v e r a g e aabout b o u t 50 feet f e e t iin n width width likewise bbut u t several s e v e r a l bbodies o d i e s may form o n e of r u s h e d rack r o c k aal~ost l m o s t hhalf a l f a mile mile form a zzone of ccrushed wide. wide. system. system. T h e s e rreef-like e e f - l i k e bbodies o d i e s closely c l o s e l y pparallel a r a l l e l tthe h e Cockscomb Cockscomb fault fault These I t is i s not n o t known w h e t h e r any any vertical v e r t i c a l displacement d i s p l a c e m e n t has h a s taken taken It \{hether p l a c e along a l o n g these t h e s e rreefs. eefs. place a r e coincident c o i n c i d e n t with w i t h known f a u l t s in in Some are knmm faults which vertical v e r t i c a l movement movement has h a s taken t a k e n place. place. which These T h e s e reef-like r e e f - l i k e mas m a s ses s e s of of crushed c r u s h e d Navajo N a v a j o Sandstone S a n d s t o n e have have r e c e i v e d 'Jery v e r y little l i t t l e study. study. received P h o e n i x (1963) ( 1 9 6 3 ) discusses d i s c u s s e s the t h e reefs r e e f s of Phoenix the t h e Lees L e e s Ferry F e r r y area a r e a and suggests s u g g e s t s a possible p o s s i b l e origin. origin. That T h a t these t h e s e reefs reefs are a r e associated a s s o c i a t e d with w i t h faulting f a u l t i n g is i s fairly f a i r l y certain, c e r t a i n , but b u t the t h e lack l a c k of of such such structures s t r u c t u r e s in i n other o t h e r monoclinef> m o n o c l i n e s is i s perplexing. perplexing. be responsible r e s p o n s i b l e for f o r this. this. Several S e v e r a l factors f a c t o r s may may The Navajo N a v a j o Sandstone S a n d s t o n e is i s thicker t h i c k e r over o v e r these these t\"o two monoclines m o n o c l i n e s than t h a n it i t is i s over o v e r most m o s t of of the t h e other o t h e r monoclines. monoclines. The The Navaj Navajo0 in i n the t h e western w e s t e r n Colorado C o l o r a d o Plateau P l a t e a u province p r o v i n c e is i s some\olhat somewhat of of aa 129 g e o l o g i c oddity. oddity. geologic I t is i s a homogenous sandstone s a n d s t o n e over o v e r 1700 feet f e e t thick thick It w i t h almost a l m o s t a lack l a c k of of horizontal h o r i z o n t a l bbedding e d d i n g planes. planes. with I n addition a d d i t i o n much In of the t h e jjointing o i n t i n g seems to t o bbe e unrelated u n r e l a t e d to t o present p r e s e n t structure. structure. of When 1Vhen s u c h a uunit n i t is i s subjected s u b j e c t e d to t o tectonic t e c t o n i c forces, f o r c e s , there t h e r e are a r e nno o natural natural such p l a n e s along a l o n g ,vhich w h i c h breakage b r e a k a g e or o r slippage s l i p p a g e ccan a n take t a k e pplace l a c e and the planes and the rresults e s u l t s may bbe e a bbroken r o k e n and shattered s h a t t e r e d shear s h e a r zone. zone. z o n e s would would Such zones be susceptible s u s c e p t i b l e tto o later later m i n e r a l i z a t i o n and siliceous s i l i c e o u s replacement. replacement. mineralization s m a l l copper c o p p e r deposit d e p o s i t is i s located l o c a t e d in i n one o n e of of these t h e s e shear s h e a r zones z o n e s along along A small t h e crest c r e s t of of the t h e Cockscomb. Cockscomb. the The position monoclines p o s i t i o n of of the t h e East E a s t Kaibab K a i b a b and and Echo m o n o c l i n e s may also also be important i m p o r t a n t in i n localizing l o c a l i z i n g the t h e siliceous s i l i c e o u s reef r e e f masses. m a s s e s . . Both B o t h are are located l o c a t e d on the t h e western w e s t e r n edge e d g e of of the t h e Colorado C o l o r a d o Plateau P l a t e a u near n e a r the t h e transitransi­ tion with t i o n zone zone w i t h the t h e ,Basin B a s i n and Range province; p r o v i n c e ; Kelley K e l l e y (1955b) ( 1 9 5 5 b ) considers considers the t h e East E a s t Kaibab K a i b a b monocline m o n o c l i n e to t o be b e tthe h e western w e s t e r n edge e d g e of of the t h e Colorado Colorado Plateau P l a t e a u tectonic t e c t o n i c province. province. Therefore T h e r e f o r e the t h e tectonic t e c t o n i c stresses s t r e s s e s applied applied to more t o the t h e East E a s t Kaibab K a i b a b and Echo monoclines m o n o c l i n e s are a r e probably probably m o r e severe s e v e r e than than forces f o r c e s eelse~Jhere l s e w h e r e in i n the t h e plateau p l a t e a u and this t h i s may account a c c o u n t for f o r the t h e shearing shearing in Navajo. i n tthe he N avajo. The faults with f a u l t s associated associated w i t h the t h e East E a s t Kaibab K a i b a b monocline monocline indicate i n d i c a t e th.s.t t h a t stresses s t r e s s e s were w e r e severe s e v e r e and both b o t h compressional c o m p r e s s i o n a l and and ttensional e n s i o n a l forces f o r c e s were w e r e involved. involved. Until m o r e work w o r k is i s done d o n e on on these these Until more rreef-like e e f - l i k e zones z o n e s of of crushed c r u s h e d and and cemented c e m e n t e d sandstone, s a n d s t o n e , their t h e i r origin o r i g i n and and s i g n i f i c a n c e ",·ill w i l l r eemain m a i n in i n doubt d o u b t •. significance . Rcad Road Creek C r e e k Faults Faults Two pparallel, a r a l l e l , arc-shaped a r c - s h a p e d faults f a u l t s cut c u t the t h e Hoenkopi Moenkopi and Chinle Chinle Formations of tthe F o r m a t i o n s in i n the t h e nnorthwest o r t h w e s t corner c o r n e r of h e map al"ea. area. Both B o t h faults f a u l t s are are 1130 30 uupthrown p t h r o w n on he w est. on tthe west. P a r t s of o t h ffaults a u l t s aare r e aactually c t u a l l y closely closely Parts of bboth sspaced paced m u l t i p l e ffaults a u l t s bbut u t iin n eeach a c h ccase a s e tthe h e eeastern-most a s t e r n - m o s t fault fault multiple major amount of of ddisplacement. hhas a s tthe he m a j o r amount isplacement. The W Western Road C Creek The e s t e r n Road r e e k fault fault hhas a s a maximum i s p l a c e m e n t of l m o s t 200 e e t and he E a s t e r n Road maximum ddisplacement of aalmost 200 ffeet and tthe Eastern Creek a u l t hhas a s a maximum i s p l a c e m e n t of l m o s t 400 eet. Creek ffault maximum ddisplacement of aalmost 400 ffeet. f a u l t zzones o n e s hhave a v e a ttotal o t a l llength e n g t h of e s s tthan han 4 m iles. fault of lless miles. Both Both The Eastern The Eastern Road C r e e k fault f a u l t hhas a s several s e v e r a l bbranches r a n c h e s aatt iits t s nnorthern o r t h e r n eend; n d ; these these Creek bbranches r a n c h e s die d i e oout u t as a s small small m onoclines w i t h ttotal o t a l ddisplacement i s p l a c e m e n t of less monoclines with of less tthan h a n 10 ffeet. eet. The ddip i p of h e bbeds e d s immediately i m m e d i a t e l y tto o tthe he w e s t of of the the of tthe west W e s t e r n Road Creek C r e e k fault f a u l t iincreases n c r e a s e s from from about a b o u t 2 degrees d e g r e e s tto o almost almost Western 5 degrees d e g r e e s as a s the t h e fault f a u l t is i s approached. approached. B o t h faults f a u l t s are a r e clearly clearly Both e x p o s e d — w h e r e tthey h e y are a r e cut c u t by Road Creek C r e e k and and its i t s tributaries t r i b u t a r i e s the the exposed--where f a u l t plane p l a n e is i s clearly c l e a r l y seen s e e n (fig. ( f i g . 2). 2). fault Joints Joints Most of of the t h e jjoints o i n t s of of the t h e Paria P a r i a area a r e a are a r e seen s e e n in i n the t h e Glen Glen G r o up. up. Canyon Gro o n l y other o t h e r formation f o r m a t i o n displaying d i s p l a y i n g a jjoint o i n t system system The only i s the t h e Kaibab K a i b a b Fonnation. Formation. is j o i n t s visible v i s i b l e in i n the t h e Kaibab K a i b a b are are The joints a i s c e r n a b l e only o n l y on aerial a e r i a l photographs p h o t o g r a p h s and and a re r e not n o t apparent a p p a r e n t in i n the the discerne.ble field. field. The joints j o i n t s trend t r e n d north n o r t h 40 4 0 °0 west. west. I n a ffew p l a c e s the t h e dr d rainage ainage In ew places p a t t e r n on Fivemile F i v e m i l e Mountain o u n t a i n is i s slightly s l i g h t l y affected a f f e c t e d and a stream s t r e a m may may pattern f o l l o w a joint j o i n t for f o r a few yards y a r d s but b u t for f o r the t h e most m o s t part p a r t the t h e joints j o i n t s do do fellow n o t af a f f eect c t the t h e erosion e r o s i o n pattern. pattern. not The j o i n t s in i n t1:l t h ee Glen G l e n Canyon Group are a r e quite q u i t e prominent p r o m i n e n t and and Th e joints l o c a l l y control c o n t r o l the t h e dr d r ainage. ainage. locally W i n g ate t e Sandstone S a n d s t o n e is i s highly highly The Hinga 131 ffractured r a c t u r e d bby y sseveral e v e r a l ssets e t s of l o s e l y sspaced p a c e d jjoints o i n t s bbut u t bbecause e c a u s e the the of cclosely W i n g a t e ccrops r o p s oout u t iin n a ssteep t e e p ccliff, l i f f , tthe h e ttrend r e n d of h e s e jjoints o i n t s could could Wingate of tthese nnot o t bbe e aaccurately ccurately m easured. measured. The pringdale S a n d s t o n e Member the The SSpringdale Sandstone Member of of the Moenave o r m a t i o n iis s jjointed o i n t e d tthough h o u g h nnot o t sso o iintensely n t e n s e l y aas s tthe h e Wingate-Wingate— Moenave FFormation aagain g a i n tthe h e ttrend r e n d ccould o u l d nnot o t bbe e aaccurately c c u r a t e l y ddetermined. etermined. The Navajo The Navajo S a n d s t o n e iis s ccut u t by s e v e r e d ssystems y s t e m s of l o s e l y spaced s p a c e d jjoints o i n t s which which Sandstone by severed of cclosely llocally o c a l l y ccontrol o n t r o l tthe h e eerosion r o s i o n ppattern. attern. The s t r i k e and d i p of h e joint joint The strike and dip of tthe pplanes lanes w ere m e a s u r e d iin n tthe h e vvicinity i c i n i t y of h e ccopper o p p e r deposit d e p o s i t in i n the the were measured of tthe Cockscomb. T h r e e sets s e t s of o i n t s aare r e ppresent resent w i t h tthe h e following following Three of jjoints with s t r i k e s and and dips: dips: strikes 0 N10°E d i p 70 7 0 °oE 60°W d i p 6IoNE, 61°NE, N35°E dip d i p lOoSE. 10°SE. NIOoE dip w dip E,, N N 60 N o r t h of of tthe he P a r i a River R i v e r in i n tthe h e Rush Rush Beds the t h e jjointing o i n t i n g of of tthe h e Navajo Navajo North Paria pproduces r o d u c e s "slick " s l i c k rock" r o c k " country c o u n t r y with w i t h many weirdly-shaped w e i r d l y - s h a p e d rrocks o c k s and and n a r r o w slot s l o t canyons. canyons. narrow Slumping Slumping Slumping S l u m p i n g (plastic ( p l a s t i c deformation d e f o r m a t i o n or o r flowage f l o w a g e or o r beds) b e d s ) occurs occurs m a i n l y in i n the t h e Chinle C h i n l e Formation F o r m a t i o n although a l t h o u g h some beds b e d s in i n the t h e Carmel Carmel mainly F o r m a t i o n are a r e also a l s o affected. affected. Formation of the t h e slumping s l u m p i n g in i n the t h e Chinle Chinle Some of o c c u r r e d shortly s h o r t l y after a f t e r deposition d e p o s i t i o n but b u t most m o s t of of the t h e deformation d e f o r m a t i o n is is occurred a s s o c i a t e d with w i t h structure s t r u c t u r e and weathering. weathering. associated When the t h e Chinle C h i n l e is i s wet wet I-Jhen t h e clays c l a y s swell s w e l l and the t h e formation f o r m a t i o n is i s extremely e x t r e m e l y weak and plastic. plastic. the N o r t h of of the t h e tmmsite t o w n s i t e of of Paria P a r i a vlhere w h e r e slumping s l u m p i n g is i s viell w e l l exposed, exposed, North f o l d i n g and flowage f l o w a g e have h a v e taken t a k e n place. place. folding T h e s e structures s t r u c t u r e s seem to to These h a v e very v e r y little l i t t l e effect e f f e c t on the t h e overlying o v e r l y i n g Glen Canyon Group. Group, have Faults Faults b r a n c h i n g off o f f the t h e Cockscomb die d i e out o u t rapidly r a p i d l y in i n the t h e Chinle C h i n l e and many many branching 132 132 ppass a s s iinto n t o a sslumped l u m p e d zzone. one. T h e s e aare r e ffavorable a v o r a b l e aareas r e a s ffor o r TorevaTorevaThese Glen Canyon Group. bblock l o c k fformation o r m a t i o n iin n tthe h e ooverlying verlying G l e n Canyon Group. A few few bbeds Carmel Formation and locally A e d s iin n tthe he C armel F o r m a t i o n aare r e sslumped l u m p e d and locally masses of ssediment ssandstone a n d s t o n e ccylinders, y l i n d e r s , ccylindrically y l i n d r i c a l l y sshaped haped m a s s e s of e d i m e n t that that with ppenetrate e n e t r a t e aadjacent d j a c e n t sstrata, t r a t a , aare r e aassociated ssociated w i t h tthis h i s sslumping. lumping. Most of tthe Carmel of h e ssl~~ping l u m p i n g iin n tthe he C a r m e l ttook o o k pplace l a c e dduring u r i n g oor r sshortly h o r t l y after after ddeposition. eposition. Periods of Deformation P e r i o d s of Deformation Nany of of tthe Paleozoic Mesozoic Many he P a l e o z o i c and and M e s o z o i c fformations o r m a t i o n s eexhibit x h i b i t facies facies Paria oor r tthickness h i c k n e s s cchanges h a n g e s in i n tthe he P a r i a area. area. This T h i s indicates i n d i c a t e s tthat h a t the the area Has affected by some form of ttectonic a r e a was a f f e c t e d by form of e c t o n i c activity a c t i v i t y iin n aalmost l m o s t every every pperiod e r i o d from r e c a m b r i a n tto o R ecent. from PPrecambrian Recent. a j o r Mesozoic M e s o z o i c and and early early The m major Cenozoic C e n o z o i c stnlctural s t r u c t u r a l events e v e n t s are a r e summarized s u m m a r i z e d iin n Table T a b l e 4 and and figure f i g u r e 25 h e relationships r e l a t i o n s h i p s between b e t w e e n continental c o n t i n e n t a l and a n d marine m a r i n e uunits n i t s and and shows tthe the t h e numerous n u m e r o u s shorelines s h o r e l i n e s developed d e v e l o p e d near n e a r the t h e Paria P a r i a area a r e a during d u r i n g the the time t i m e represented r e p r e s e n t e d by b y the t h e rocks r e c k s exposed e x p o s e d at a t the t h e surface. surface. Pre·-Dakota P r e - D a k o t a Deformation Deformation Periods P e r i o d s of of regional r e g i o n a l tectonic t e c t o n i c activity a c t i v i t y are a r e represented r e p r e s e n t e d by by major m a j o r unconformities. unconformities. The three t h r e e major m a j o r unconformities u n c o n f o r m i t i e s are a r e the the P e r m o - T r i a s s i c , the t h e Moenkopi-Chinle, M o e n k o p i - C h i n l e , and the t h e Entrada-Dakota. Entrada-Dakota. Permo-Triassic, All All t h r e e unconformities u n c o n f o r m i t i e s show a significant s i g n i f i c a n t break b r e a k in i n deposition d e p o s i t i o n and aa three m a j o r change c h a n g e in i n environment e n v i r o n m e n t and rock r o c k type. type. major t h e Entrada-Dakota Entrada-Dakota Only the o r Sub-Cretaceous S u b - C r e t a c e o u s unconformity u n c o n f o r m i t y is i s accompanied a c c o m p a n i e d by angular a n g u l a r discordance. discordance. or 133 post-Dak6taDef6rmation Post-Dakota Deformation The major m a j o r pperiods e r i o d s of of deformation d e f o r m a t i o n hhave a v e taken t a k e n place p l a c e since s i n c e the the deposition d e p o s i t i o n of of the t h e Dakota D a k o t a Formation. Formation. Regional R e g i o n a l features f e a t u r e s have h a v e been been d a t e d fairly f a i r l y accurately a c c u r a t e l y bbut u t local l o c a l faults f a u l t s and and folds f o l d s are a r e more more dated d i f f i c u l t tto o date. date. difficult Flat-lying F l a t - l y i n g sediments s e d i m e n t s of of the t h e Lower Lower Eocene E o c e n e Hasatch W a s a t c h Formation Formation t r u n c a t e the t h e gently g e n t l y dipping d i p p i n g Upper Upper Cretaceous· C r e t a c e o u s Kaiparowits K a i p a r o w i t s Formation Formation truncate at Mountain a t Cannan Cannan M o u n t a i n about a b o u t 25 miles m i l e s north n o r t h of of Paria P a r i a thereby t h e r e b y ddating a t i n g the the K a i b a b upliftu p l i f t - East E a s t Kaibab K a i b a b monocline m o n o c l i n e as a s latest l a t e s t Cretaceous-earliest Cretaceous-earliest Kaibab Tertiary. Tertiary. T h i s age a g e (which ( w h i c h correlates c o r r e l a t e s with w i t h other o t h e r Rocky Rocky Mountain Mountain This uuplifts) p l i f t s ) is i s ppresumably r e s u m a b l y tthe h e same throughout t h r o u g h o u t the t h e entire e n t i r e length l e n g t h of of the the monocline. monocline. After A f t e r the t h e folding f o l d i n g of of tthe h e monocline, m o n o c l i n e , Tertiary T e r t i a r y stream s t r e a m and and lake lake d e p o s i t s truncated t r u n c a t e d tthe h e folded f o l d e d bbeds. eds. deposits IIt t was on these t h e s e Tertiary Tertiary s e d i m e n t s tthat h a t the t h e ancestral a n c e s t r a l drainage d r a i n a g e ppattern a t t e r n of of the t h e Colorado C o l o r a d o Plateau Plateau sediments developed. developed. Hunt ( 1 9 5 6 , 1969) 1969) presents p r e s e n t s thorough t h o r o u g h treatments t r e a t m e n t s on the the Hunt (1956, h i s t o r y of of the t h e Colorado C o l o r a d o River R i v e r drainage d r a i n a g e system. system. history The second s e c o n d major m a j o r post-Dakota p o s t - D a k o t a structural s t r u c t u r a l event e v e n t tto o directly directly a f f e c t tthe h e Paria P a r i a area a r e a was the t h e uuplift p l i f t and nortlmard n o r t h w a r d tilting t i l t i n g of of the the affect C o l o r a d o Plateau P l a t e a u provence. provence. Colorado T h i s uuplift p l i f t bbegan e g a n as a s early e a r l y as a s the the This P a l e o c e n e and and Eocene E o c e n e and is i s still s t i l l continuing c o n t i n u i n g today t o d a y (Hunt, ( H u n t , 1969, 1 9 6 9 , p. p. Paleocene 67). 67). T h i s tilting t i l t i n g and and uplifting u p l i f t i n g is i s responsible r e s p o n s i b l e for f o r the t h e entrenching entrenching This of tthe h e streams, s t r e a m s , efficient e f f i c i e n t drainage d r a i n a g e system, s y s t e m , and and the t h e sculpturing s c u l p t u r i n g of of the the of c l i f f s , mesas, m e s a s , and and plateaus. plateaus. cliffs, Unit PARIA WEST .. " ~ '" ' . EAST . .. ' Ksj . '( - "t- • . . :.:. .. .~ ,", .. .. . ... . ( ::.:....,.: . , ' Kss ~ " (q,r' Kst Kt . .' Kd Jee Jee lee Jew Jes Jcp Jnt Je j nn AQUEOUS ?:' . I .... limo RtO (f) l- • '.. .'• .. j.:II:CUSIR./N£· .' 'li" IAL' • :--~" .-, ' 3~-- -=--.~<~~==~-~~.- low « a::- f-LU A '-i2 - ~. ~ ., .( . ' ' -" ~ . - . .;....,-. ~-"~=="'!===-<~=?=: .• .• . .• ." ~ c..d"- ~·.'" . .;. . ..... • • ( • - .- . _ooe2__.,. .F!-,.U. Y!,A.L ••• '.. , ... ... '/ ~ ... .... . .. " . • " : '. ' ..... . ' ... • . .~ ~ ____1._;_~~_:_~3_· _::J Fi f i 2;U:r.-0 g u r e 225. 5 . -~-~GG t~e nerall? n e r a l i z eedd dia d i a ggrram a m shov!ing s h o w i n g rel r e l aa ttioaships i o n s h i p s (ti ( t i mme e and a n d space) space) of r'a ~les marin':? of l at a t eest st P a l~ozoic l e o z o i c a nnd d M e sozo.ic ozoic m a r i n e tr t r aansg n s g rr.cssions e s s i o n s and a n d regreS regres­ f.ions Paria s i o n s and a n d tlh"! t h e mi m iggration r a t i o n of of environments e n v i r o n m e n t s ac a c r ooss s s tthe he P a r i a area. area. M 135 l3-5 AGE EVENT EVIDENCE Uplift U p l i f t of of Kaibab K a i b a b PlatPlate a u ; possible p o s s i b l e faulting faulting eau; a l o n g Cockscomb(?) Cockscomb ( ? ) along ( 1 9 6 9 ) : Damming of of Colorado Colorado Hunt (1969): R i v e r t o d e p o s i t B i d a h o c h i River to deposit Bidahochi Fm. i n N. Ariz. Ariz. in Development D e v e l o p m e n t of of faults faults of H i g h Plateaus P l a t e a u s and and of High western w e s t e r n Colo. C o l o . Plateau Plateau (may be b e related r e l a t e d to to Cockscomb faults) faults) Cockscomb Faults F a u l t s dated d a t e d by volcanics volcanics L a t e K-to K-to Late present (?) present(?) Uplift U p l i f t and northward northward t i l t i n g of of Colorado Colorado tilting Plateau Plateau R e g i o n a l ; canyon c a n y o n cutting, c u t t i n g , sculpsculp­ Regional; turing t u r i n g of of landscape landscape Late L a t e KEarly Early T Kaibab K a i b a b Uplift U p l i f t and and f o l d i n g of of East E a s t Kaibab Kaibab folding monocline monocline F l a t - l y i n g Eocene E o c e n e H.:3satch W a s a t c h strata strata Flat-lying g e n t l y dipping d i p p i n g La L a te te K on gently K K a i p a r o w i t s Fm. at a t Canaan Canaan Mtn. Mtn. Kaiparowits Late K Late K Uplift U p l i f t to t o west-conwest-con­ flict f l i c t between b e t w e e n marine marine c o n t . conditions conditions and cont. C l a s s i c marine m a r i n e regr r e g r e sssion; s i o n ; congl. congl, Classic i n units u n i t s of of Straight S t r a i g h t Cliffs, C l i f f s , Fm. in — iincrea n c r e a ssing i n g 2..11l amount of fluvial fluvial -C'un t of d e p o s i t s uup\lards--complex p w a r d s — c o m p l e x interinterdeposits ffingering i n g e r i n g of of marine-non-marine marine-non-marine deposits deposits Late K Late K Return R e t u r n to t o stable s t a b l e condcond­ itions marine itions m a r i n e invasion invasion from east. east. from C o a l in i n uupper p p e r Dakota, D a k o t a , 600 feet feet · Coal of marine m a r i n e Tropic T r o p i c Shale Shale of Upper JUpper JEarly K Early K Formation F o r m a t i o n of of subsubCre C r e taceous t a c e o u s unconuncon­ formiti f o r m i t i ees; s ; uplift u p l i f t to to southwest southwest A n g u l a r unconformity u n c o n f o r m i t y with w i t h local local Angular r ee lli i eeff of over o v e r 10 fe f e eet; t ; ab, a bssence ence of of Sum S u mmerville m e r v i l l e and and Morrison o r r i s o n ForFor­ m a t i o n s ; r eeg g iiona o n a l evidence; evidence; mations; bbasal a s a l conglomerate c o n g l o m e r a t e in i n Dakota Dakota Upper Upper J (Entrada) (Entrada) Unconf U n c o n formities o r m i t i e s separseparate a t e Entrada E n t r a d a members members Reg R e giona i o n a l evidence e v i d e n c e (Stokes ( S t o k e s and and Thompson, 1969) 1969) Upper Upper J (Entrada) (Entrada) Conflict C o n f l i c t between between "Great " G r e a t Sand Sand Pile" P i l e " and rred e d bbeds; eds; P a r i a area area Paria shoreline shoreline Entrad E n t r a d aa increases i n c r e a s e s in i n sand s a n d content content tto o sou s o u th-silty t h - s i l t y to t o north~vest; northwest; chang c h a n g ee of of sedimentary s e d i m e n t a r y structures; structures; rrapid a p i d facies f a c i e s and and thickness thickness changes changes Miocene Miocene T a b l e l: 1:— L a te te P m i a n through t h r o u g h Miocene M i o c e n e structural s t r u c t u r a l events e v e n t s of of Faria P a r i a area area Table - -La Pee rrmian a s evidenced e v i d e n c e d by t h e s e ddimentar i m e n t a r yy formations. formations. as by the 136 136 AGE AGE EVENT EVENT EVIDENCE EVIDENCE M i d d l e JJ Middle ((Cannel) Carmel) Continued C o n t i n u e d uuplift p l i f t to to and w west. Conssouth o u t h and est. fflect l e c t bbetween e t w e e n "Great" "Great" Sand PPile and rred Sand i l e and e d beds beds and limestones; and limestones; PParia a r i a aarea r e a shoreline shoreline SSandstone a n d s t o n e and o n g l o m e r a t e in in and cconglomerate C a r m e l had o u r c e tto o ssouth o u t h and Carmel had ssource ssouthwest--probably o u t h w e s t — p r o b a b l y eroding eroding N a v a j o SSs.; s.; C a r m e l ssandy a n d y to to Navajo Carmel ssouth, o u t h , ssilty i l t y tto o north north Middle M i d d l e JJ Uplift of Mohavia-U p l i f t of Mohavia— hhighlands i g h l a n d s tto o southsouth­ west w est IIntertonguing n t e r t o n g u i n g of Carmel-Navajo of Carmel-Navajo — s o u r c e of a r m e l ttongue o n g u e to to --source of C Cannel w est; m a r i n e ssea e a occupies occupies west; marine ffore-deep ore-deep Late Trr L ate T (Kayenta) (Kayenta) Hinge H i n g e lline i n e iin n Paria Paria area area R a p i d ffacies a c i e s cchange h a n g e and thicken­ Rapid and thickeniing n g of K a y e n t a ; l i n e c o i n cides of Kayenta; line coincides rregionally egionally w i t h W i n g a t e M oenave with Wingate-Moenave ooverlap verlap Late Tr L a t e Tr (Glen (Glen Canyon) Slight S l i g h t ppositive o s i t i v e area area Moenave and bbetween e t w e e n Moenave Wingate W i n g a t e Basins Basins W i n g a t e tthickens h i c k e n s tto o northeast-northeast— 'iingate o ssouth; o u t h ; line l i n e of of overover­ Moenave tto l a p coincides coincides w i t h Kayenta K a y e n t a hinge hinge lap with line line Late L a t e Tr (Chinle(ChinleGlen CanCan­ yon) Period P e r i o d of of erosion erosion S h a r p change c h a n g e in i n sedj~entation; sedimentation; Sharp very m i n o r erosion; e r o s i o n ; regional regional very minor evidence evidence Late L a t e Tr Tr (ChInle) (Chinle) Volcanic V o l c a n i c episode e p i s o d e to to southwest southwest (157o) amount of of tuffaceous tuffaceous High (15'l~ m a t e r i a l in i n Shinarump S h i n a r u m p and Monitor Monitor material B u t t e Members of C h i n l e ; f irst Butte of Chinle; first eevide~lce v i d e n c e of of . Mohavia M o h a v i a in i n Mesozoic(?) Mesozoic(?) Middle(?) Middle (?) Tr Period P e r i o d of of erosion; erosion; new regime r e g i m e of of sedimentation sedimentation G r e a t lithologic l i t h o l o g i c and sedimentasedimentaGreat l o g i c a l change; c h a n g e ; major m a j o r channels channels logica c u t into i n t o i-1oenkopi; M o e n k o p i ; regional regional cut evidence evidence Early E a r l y Tr Tr (Moenkopi) Paria P a r i a area a r e a hinge h i n g e line, line, shoreline shoreline T h i c k e n i n g of of Hoenkopi Moenkopi to t o west; west; Thickening c h o u t of Timpovleap Timpoweap and Virgin Virgin p i nnchout n e a r Paria; Paria; near Late L a t e PP- Period P e r i o d of of erosion erosion No Upper Perm Tocks--Permorocks—PermoNo T r i a s s i c unconfotT.l.ity u n c o n f o r m i t y regional regional Triassic evidence evidence Table T a b l e l.--Continued 1.—Continued 137 The faulting f a u l t i n g along a l o n g tthe h e bboundary o u n d a r y faults f a u l t s to t o the t h e west w e s t such s u c h as as Paunsaugunt, tthe h e Sevier, Sevier, P a u n s a u g u n t , and Hurricane H u r r i c a n e Faults F a u l t s started s t a r t e d in i n early early Miocene Miocene and is i s still s t i l l active a c t i v e in i n the t h e Recent R e c e n t (Hunt, ( H u n t , 1956, 1 9 5 6 , p. p . 81, 8 1 , 84). 84). Whether tthese h e s e faults f a u l t s are a r e ttime i m e equivalents e q u i v a l e n t s to t o the t h e faulting f a u l t i n g along a l o n g the the Whether E a s t Kaibab K a i b a b Monocline M o n o c l i n e is i s uncertain u n c e r t a i n but b u t the t h e possibility p o s s i b i l i t y cannot c a n n o t be be East r u l e d out. out. ruled I n fact f a c t Hunt (1969, ( 1 9 6 9 , pp.. Ill, I l l , 113) cites c i t e s evidence e v i d e n c e that t h a t the the In K a i b a b Plateau P l a t e a u was uplifted u p l i f t e d 1000-1500 1 0 0 0 - 1 5 0 0 feet f e e t in i n the t h e Miocene M i o c e n e which which Kaibab rresulted e s u l t e d in i n the t h e damming of of the t h e Colorado C o l o r a d o River R i v e r and and the t h e deposition deposition of the t h e Bidahochi B i d a h o c h i Formation F o r m a t i o n in i n northeastern n o r t h e a s t e r n Arizona. Arizona. of T h i s uplift u p l i f t took took This pplace l a c e at a t about a b o u t tthe h e same ttime i m e the t h e boundary b o u n d a r y faults f a u l t s were w e r e active. active. I t is is It ppossible o s s i b l e that t h a t some of of tthe h e faulting f a u l t i n g in i n the the P a r i a area a r e a was active a c t i v e during during Paria tthe he M i o c e n e uplift u p l i f t of of the the K a i b a b Plateau P l a t e a u and and the t h e faulting f a u l t i n g to t o tthe h e west. west. Miocene Kaibab f a u l t s along a l o n g the t h e Cockscomb cannot c a n n o t be b e accurately a c c u r a t e l y dated d a t e d at a t present present The faults so further f u r t h e r conclusions c o n c l u s i o n s are a r e not n o t possible. possible. so Causes C a u s e s of of Defolmation Deformation Several S e v e r a l theories t h e o r i e s have h a v e been b e e n pproposed r o p o s e d to t o expla e x p l a iin n the t h e uplifts u p l i f t s of the t h e Colorado C o l o r a d o Plateau, P l a t e a u , especial e s p e c i a l lly y with w i t h their t h e i r asymmetrical a s y m m e t r i c a l form form and and b o r d e r i n g monoclines. monoclines. bordering o l d but b u t ppopular o p u l a r ttheory h e o r y a ttributes t t r i b u t e s the the An old monoclines m o n o c l i n e s tto o sed s e d iime m e nt n t aa rry y rocks r o c k s draped d r a p e d over o v e r normal n o r m a l faults f a u l t s in i n the the basement. basement. considered. considered. C o m p reession s s i o n aand s h o r t e n i n g in i n the t h e region r e g i o n were w e r e not not Compr nd shortening K e l l e y (1955a, ( 1 9 5 5 a , p. p . 79 7 9 8-799) 8 - 7 9 9 ) ex e x ppands a n d s o~ on an idea i d e a first first Kelley ppresented r e s e n t e d by Baker B a k e r (1935, ( 1 9 3 5 , pp.. 1500) 1500) tthat h a t relate r e l a t e ss tthe h e monoclines m o n o c l i n e s to to c o m p r e s s i o n a l forces f o r c e s ov o v e r ddee e e pp - s eeated a t e d tthrusts. hrusts. compressional northwestThe northwest- t r e n d i n g f aaults u l t s that t h a t branch b r a n c h off o f f tthe h e Eas E a s t Kaibab K a i b a b hlOl:ocline m o n o c l i n e are a r e similar similar trending 138 138 Lees which tto o ffaults a u l t s iin n tthe he L e e s FFerry e r r y aarea rea w h i c h PPhoenix h o e n i x ((1963, 1 9 6 3 , pp.. 54) 54) aattributes t t r i b u t e s tto o ccompressional o m p r e s s i o n a l fforces, o r c e s , ddiagonal i a g o n a l oor r pperpedicular e r p e d i c u l a r tto o the the of tthe ttrend r e n d of h e monocline. monocline. During and aafter of tthe monocline, D u r i n g and f t e r tthe h e fformation o r m a t i o n of he m o n o c l i n e , tensional tensional were masses fforces orces w e r e pperhaps e r h a p s rresponsible e s p o n s i b l e ffor o r tthe h e rreef-like eef-like m a s s e s of of and ccemented Navajo Sandstone. bbrecciated r e c c i a t e d and e m e n t e d rrock o c k iin n tthe he N avajo S andstone. That T h a t these these were shown by by tthe of the fforces orces w e r e ppresent r e s e n t rregionally e g i o n a l l y ccan a n bbe e shown h e eexistence x i s t e n c e of the bboundary o u n d a r y ffaults a u l t s tto o tthe he w est. west. IInability n a b i l i t y tto o ddate a t e tthe h e ccrushed r u s h e d and and s i l i c i f i e d ssandstone a n d s t o n e bbodies o d i e s pprohibits r o h i b i t s ttheir h e i r correlation correlation w i t h the the silicified with f a u l t s tto o tthe h e west. west. faults q GEOMORPHOLOGY Physiographic P h y s i o g r a p h i c Features Features The PParia a r i a area a r e a is i s located l o c a t e d on o n the t h e western w e s t e r n part p a r t of of the the C o l o r a d o Plateau P l a t e a u province p r o v i n c e (pl. ( p i . 44); ) ; to t o the t h e north n o r t h is i s the t h e Paria Paria Colorado A m p h i t h e a t e r and and the t h e High P l a t e a u s sub-province; s u b - p r o v i n c e ; to t o tthe h e east e a s t is i s the the Amphitheater High Plateaus C a n y o n l a n d s section s e c t i o n consisting c o n s i s t i n g of of the t h e Kaiparowits K a i p a r o w i t s rregion e g i o n and the the Canyonlands G l e n Canyon-Lees C a n y o n - L e e s Ferry F e r r y areas; a r e a s ; to t o the t h e south s o u t h is i s the t h e Paria P a r i a Plateau Plateau Glen t h e Grand Grand Canyon Canyon region; r e g i o n ; to t o the t h e west w e s t is i s tthe h e transition t r a n s i t i o n zone zone and the bbetween e t w e e n the t h e Colorado C o l o r a d o Plateau P l a t e a u and and the t h e Great G r e a t Basin. Basin. P a r i a area area The Paria h a s lland a n d forms f o r m s representative r e p r e s e n t a t i v e of of all a l l these t h e s e areas a r e a s but b u t most m o s t of of the the has pphysiography h y s i o g r a p h y is i s typical t y p i c a l of h e Canyonlands C a n y o n l a n d s section. section. of tthe A l l of of the the All l a n d f o r m s of of thG the P a r i a area a r e a are a r e directly d i r e c t l y related r e l a t e d to t o four f o u r key k e y factfact­ landfonlls Paria o r s — c l i m a t e , structure, s t r u c t u r e , bedrock, b e d r o c k , and and erosion. erosion. ors--climate, C l i m a t e , which w h i c h has has Climate, bbeen e e n discussed d i s c u s s e d earlier; e a r l i e r , is i s rrelatively e l a t i v e l y uuniform n i f o r m throughout t h r o u g h o u t the t h e area area and will w i l l not n o t be b e ddiscussed i s c u s s e d further f u r t h e r here, h e r e , bbut u t a number number of of various various and ppossibilities o s s i b i l i t i e s el1volving e n v o l v i n g the t h e other o t h e r three t h r e e factors f a c t o r s have h a v e pproduced r o d u c e d several several d i s t i n c t physiographic p h y s i o g r a p h i c units u n i t s in i n the t h e Paria P a r i a area. area. distinct T h e s e sub-divisions sub-divisions These a r e bbriefly r i e f l y described d e s c r i b e d and and their t h e i r relationship r e l a t i o n s h i p to t o tthe h e bedrock, bedrock, are s t r u c t u r e , and and erosion e r o s i o n are a r e discussed. discussed. structure, I n tthe h e southwest s o u t h w e s t quarter q u a r t e r of of the t h e map area a r e a at a t Fivemile F i v e m i l e Mountain Mountain In tthe h e resistant r e s i s t a n t strata s t r a t a of of the t h e Kaibab K a i b a b Formation F o r m a t i o n conform c o n f o r m tto o the t h e structure structure of the t h e Kaibab K a i b a b uupwarp. pwarp. of H e r e short, s h o r t , intermittent, i n t e r m i t t e n t , consequent c o n s e q u e n t streams streams Here hhave a v e cut c u t narrow n a r r o w step s t e p canyons c a n y o n s into i n t o the the K aibab. Kaibab. Only four f o u r streams streams Only c r o s s tthe h e Kaibab K a i b a b Upvla"rp upwarp over o v e r its i t s entire e n t i r e 150 mile m i l e length l e n g t h -— the the cross Colorado R i v e r , Buckskin B u c k s k i n (Kaibab) ( K a i b a b ) Gulch, G u l c h , Sand Sand Gulch, G u l c h , and the t h e Paria Paria Colorado River, 140 River. River. Sand Sand Gulch G u l c h heads h e a d s in i n the the V Vermilion e r m i l i o n Cliffs, C l i f f s , flows f l o w s in i n an open open valley v a l l e y across a c r o s s the t h e Triassic T r i a s s i c red r e d bbeds, e d s , cuts c u t s a narrow, n a r r o w , deep, d e e p , step step canyon c a n y o n in i n Fivemile F i v e m i l e Mountain, M o u n t a i n , is i s seemingly s e e m i n g l y consequent c o n s e q u e n t in i n Fivemile Fivemile Valley, V a l l e y , bbut u t then t h e n makes a right r i g h t angle a n g l e bend b e n d and and cuts c u t s through t h r o u g h the the Cockscomb, and Paria and finally f i n a l l y flmvs f l o w s in i n an a n open o p e n vvalley a l l e y to t o the the P a r i a River. River. a l l u v i a l fans f a n s at a t tthe h e foot f o o t of of the t h e Cockscomb Cockscomb and V e r m i l i o n Cliffs Cliffs The alluvial Vermilion o n c e covered c o v e r e d this t h i s ppart a r t of of Fivemile F i v e m i l e Mountain M o u n t a i n and superposed s u p e r p o s e d Sand once G u l c h across a c r o s s the t h e uplift. uplift. Gulch R e m n a n t s of of alluvium a l l u v i u m are a r e preserved p r e s e r v e d near near Remnants t h e rrim i m of of the t h e gulch. gulch. the I m m e d i a t e l y east e a s t of of Fivemile F i v e m i l e Mountain M o u n t a i n is i s Fivemile F i v e m i l e Valley, Valley, Immediately s t r i k e valley v a l l e y developed d e v e l o p e d in i n the t h e soft, s o f t , faulted f a u l t e d Noenkopi Moenkopi and Chinle Chinle a strike F ormations. Formations. Extensive R~tensive a l l u v i a l fan f a n deposits d e p o s i t s once o n c e filled f i l l e d the t h e valley valley alluvial bbut u t the t h e two main m a i n streams, s t r e a m s , Robinson R o b i n s o n and and Sand Sand Creeks, C r e e k s , are a r e now entrenched entrenched a b o u t tten e n feet f e e t into i n t o this t h i s aalluvitnTl l l u v i u m and have h a v e eroded e r o d e d much of of the the about p r e - e x i s t i n g deposits. deposits. pre-existing R i s i n g 500-800 5 0 0 - 8 0 0 feet f e e t above a b o v e Fivemile F i v e m i l e Valley V a l l e y is i s the t h e Cockscomb. Cockscomb. Rising South River S o u t h of of the t h e Paria Paria R i v e r the t h e Cockscomb consists c o n s i s t s of of four f o u r parts--the parts—the f o o t cons c o n s isting i s t i n g of of the t h e Chinle, Chinle, W i n g a t e , and and lower l o w e r Moenave 17ormations, Formations, foot Wingate, e d of t hhe e ragge r a g g e dd cliff c l i f f compos composed of the t h e uupper p p e r Moenave and and Kayenta K a y e n t a Formations, Formations, t h e cen c e n tra t r a l ridges r i d g e s composed composed of of fractur f r a c t u r eedd Navajo N a v a j o Sandstone, S a n d s t o n e , and the the the bbacks a c k s llope, o p e , hogbacks, h o g b a c k s , and and valle v a l l e yys s composed composed of of the t h e Navajo-Carmel Navajo-Carmel ttongues, o n g u e s , the t h e San Raf R a f ael a e l Group, G r o u p , and and the t h e Dakota D a k o t a Formation. Formation. Sand Gulch G u l c h cuts c u t s across a c r o s s the t h e Cockscomb in in m meandering e a n d e r i n g Catstairs Catstairs h i c h is i s 500 f.eet f e e t deep. deep. Canyon w whi~h m e a n d e r i n g pattern p a t t e r n rules r u l e s out out The meandering h e aad\v,n-d d w a r d e.ros e r o s ii oon n as a s the t h e method of canyon c a n y o n cutting. cutting. he method of C a t stairs s t a i r s Canyon Canyon Cat 1141 41 Cockscomb iin of iits ccrosses r o s s e s tthe h e Cockscomb n oone n e of t s llowest o w e s t aareas. reas. FFor o r aalmost lmost a mile Cockscomb iis of lless 5000 ffeet. m i l e tthe h e Cockscomb s aat t aan n eelevation l e v a t i o n of e s s tthan h a n 5000 eet. The Paria an eelevation of about ssmall m a l l cconglomerate o n g l o m e r a t e ooutcrop u t c r o p nnear ear P a r i a iis s aat t an l e v a t i o n of about 5000 ffeet Sand C Creek was ssuperimposed low sspot 5000 e e t sso o Sand r e e k was u p e r i m p o s e d aacross c r o s s tthis h i s low p o t in in tthe h e Cockscomb h e bbase a s e llevel e v e l was igher. Cockscomb when when tthe was much much hhigher. The once The once m e a n d e r i n g sstream t r e a m hhas a s ccut u t a ccanyon anyon w i t h a ggradient r a d i e n t of e e t per per meandering with of 200 200 ffeet m ile. mile. The Road reek B a d l a n d s iin n tthe h e nnorthwest o r t h w e s t ccorner o r n e r of h e area area Road C Creek Badlands of tthe cconstitutes o n s t i t u t e s tthe he m o s t ddissected i s s e c t e d aarea r e a on he m ap. most on tthe map. The r a i n a g e system system The ddrainage iis s cut c u t almost a l m o s t eentirely n t i r e l y iin n gently g e n t l y ddipping i p p i n g strata s t r a t a of h e Moenkopi of tthe F o r m a t i o n — y e t tthe h e aarea r e a iis s ccharacterized h a r a c t e r i z e d by l i f f s 200 feet f e e t high, high, Formation--yet by ccliffs n a r r o w slot s l o t canyons, c a n y o n s , and and the t h e complete c o m p l e t e removal r e m o v a l of h e once o n c e extensive extensive narrow of tthe a l l u v i a l fan f a n deposits. deposits. alluvial I t is i s significant s i g n i f i c a n t tthat h a t tthe h e ddrainage r a i n a g e divide divide It bbetween e t w e e n Road C r e e k and G u l c h coincides c o i n c i d e s almost a l m o s t pperfectly e r f e c t l y with with Creek and Sand Gulch tthe h e northern n o r t h e r n edge e d g e of of the t h e remaining r e m a i n i n g alluvial a l l u v i a l fan f a n deposits. deposits. All All t h e s e facts f a c t s indicate i n d i c a t e tthat h a t the t h e Road Creek C r e e k system s y s t e m has h a s bbeen e e n downcutting downcutting these r a p i d l y quite q u i t e recently. recently. rapidly T h i s downcutting d o w n c u t t i n g is i s rresponsible e s p o n s i b l e fo f o rr. some of of This t h e best b e s t ex e x posures p o s u r e s of of the t h e Moenkopi Formation F o r m a t i o n in i n southwestern s o u t h w e s t e r n Utah. Utah. the e r o s i o n of of the t h e Road Creek C r e e k Badlands B a d l a n d s is i s so s o vigorous v i g o r o u s that t h a t it i t is is The erosion now pirating p i r a t i n g the t h e northern n o r t h e r n reaches r e a c h e s of of Robinson R o b i n s o n Creek C r e e k which w h i c h flows flows s o u t h w a r d into i n t o Sand Gulch. Gulch. southward J u s t why such s u c h rapid r a p i d dcwncutting d o w n c u t t i n g should s h o u l d t aa kke e place p l a c e is i s not not Just clear. clear. p o s s i b l e explanation e x p l a n a t i o n is i s that t h a t the t h e thick, t h i c k , resistant, resistant, One possible c h a n n e l deposit d e p o s i t of of Shinarump S h i n a r u m p just j u s t ,,,est w e s t of of the t h e movie m o v i e set s e t created c r e a t e d aa channel w a t e r f a l l and caused c a u s e d Ro Road C r e e k to t o enter e n t e r t hhe e Par P a r ia i a River R i v e r as a s a hanging hanging waterfall a d Creek 142 vvalley. alley. t h e waterfall w a t e r f a l l rretreated e t r e a t e d to t o the t h e eastern e a s t e r n Road Creek C r e e k fault fault When the and and rreached e a c h e d tthe h e softer s o f t e r Moenkopi Moenkopi Formation, F o r m a t i o n , the t h e falls f a l l s immediately immediately disintegrated d i s i n t e g r a t e d and and base b a s e llevel e v e l was quickly q u i c k l y lowered l o w e r e d 50 to t o 100 feet. feet. Hmvever, H o w e v e r , this t h i s theory t h e o r y would would nnot o t explain e x p l a i n the t h e recent, r e c e n t , rapid rapid e r o s i o n along a l o n g a tributary t r i b u t a r y to t o Road Creek C r e e k that t h a t hhas a s cut c u t similar s i m i l a r slot slot erosion c a n y o n s at a t the t h e foot f o o t of of the t h e Cockscomb. canyons T h i s tributary t r i b u t a r y enters e n t e r s Road Road This C r e e k below b e l o w the t h e presumed p r e s u m e d waterfall. waterfall. Creek P a r i a River R i v e r enters e n t e r s the t h e map area a r e a at a t Paria; P a r i a ; it i t flows f l o w s in i n aa The Paria wide bbroad r o a d vvalley a l l e y one-half o n e - h a l f mile mile w i d e that t h a t is i s cut c u t in i n non-resistant n o n - r e s i s t a n t Chinle Chinle Formation. Formation. The V Vermilion e r m i l i o n Cliffs C l i f f s tower t o w e r 700-1000 7 0 0 - 1 0 0 0 feet f e e t above a b o v e the t h e valley. valley. i v e r crosses c r o s s e s the t h e Cockscomb in i n Shurtz S h u r t z Gorge, G o r g e , a narrow, n a r r o w , 8heersheerThe rriver walled Navajo w a l l e d ccanyon a n y o n cut c u t into i n t o tthe he N a v a j o Sandstone. Sandstone. It I t contains c o n t a i n s a few few meanders m e a n d e r s in i n Shurtz S h u r t z Gorge G o r g e and tthe h e hhistory i s t o r y of of its i t s forwation f o r m a t i o n is i s probably probably quite q u i t e similar s i m i l a r to t o the t h e hhistory i s t o r y of of Catstairs C a t s t a i r s Canyon Canyon though t h o u g h the t h e Paria P a r i a is is pprobably r o b a b l y much older. older. A f t e r leaving l e a v i n g Shurtz S h u r t z Gorge Gorge the t h e rriver i v e r enters e n t e r s Rockhouse R o c k h o u s e Valley; Valley; After hhere e r e bbedrock e d r o c k of of the t h e vvalley a l l e y is i s the t h e soft s o f t Tropic T r o p i c Shale, S h a l e , and and the t h e overlying overlying rresistant e s i s t a n t Straight S t r a i g h t Cliffs C l i f f s Formation F o r m a t i o n forms f o r m s the t h e Brigham Brigham Plains, P l a i n s , the t h e top top of w h i c h are a r e lOOO-BOO 1 0 0 0 - 1 3 0 0 feet f e e t above a b o v e the t h e river. river. of which r i v e r flows f l o w s up dip dip The river a t this t h i s point p o i n t and re-enters r e - e n t e r s younger, y o u n g e r , more resistant r e s i s t a n t rrocks o c k s and and again again at f l o w s in i n the t h e Hide, w i d e , steep-walled s t e e p - w a l l e d Adairville A d a i r v i l l e Canyon. Canyon. flows P a r i a flows flows The Paria t h r o u g h the t h e canyon c a n y o n for f o r about a b o u t 3 miles m i l e s bbefore e f o r e enCoU1ltering e n c o u n t e r i n g the t h e soft soft through C a r m e l Formation F o m a t i o n in i n East E a s t andl-lest and West Coves as a s it i t leaves l e a v e s the t h e map area. area. Canlel c r o s s e s the t h e Paria P a r i a River R i v e r in i n tthis h i s bbroad r o a d valley v a l l e y but? but 2 U. S. Highway Highway 89 crosses m i l e s sout.h s o u t h of of ~the t h e bridge b r i d g e the t h e rriver i v e r enters e n t e r s 11 a deep, d e e p , narrOvl n a r r o w canyon c a n y o n which which miles 143 143 Lees ccontinues o n t i n u e s tto o L e e s Ferry. Ferry. The Brigham Brigham PPlains The l a i n s aarea r e a iis s sstructurally t r u c t u r a l l y tthe h e llowest o w e s t but but on tthe map. ttopographically o p o g r a p h i c a l l y tthe h e hhighest i g h e s t aarea r e a on he m ap. 5914 ffeet 5914 e e t aabove b o v e ssea e a llevel. evel. IIts t s ssouthern o u t h e r n ttip i p is is The D Drip Tank Member Member of of tthe Straight The r i p Tank he S t r a i g h t Cliffs Cliffs Formation, which one of of tthe most F ormation, w h i c h iis s one he m o s t rresistant e s i s t a n t rrock o c k uunits n i t s iin n tthe h e Paria Paria aarea, r e a , pprotects r o t e c t s and a p s tthe h e uunderlying n d e r l y i n g hhard a r d and o f t rrock o c k and forms ' and ccaps and ssoft and forms tthe h e ssurface u r f a c e of h e pplains. lains. of tthe S t r e a m s aare r e slowly s l o w l y eeating a t i n g hheadward e a d w a r d into into Streams tthe h e Brigham l a i n s giving g i v i n g tthe h e aarea r e a aan n iirregular r r e g u l a r ooutline, u t l i n e , bbut u t very very Brigham PPlains llittle i t t l e ddovmcutting o w n c u t t i n g is i s ttaking a k i n g pplace l a c e on h e rresistant e s i s t a n t ssurface u r f a c e of of the the on tthe pplains. lains. The nnorthwestern o r t h w e s t e r n edge e d g e of of the t h e Brigham B r i g h a m Plains P l a i n s is i s involved i n v o l v e d in in monoclinal tthe he m o n o c l i n a l folding. folding. A beautiful b e a u t i f u l strike s t r i k e vv!llley, a l l e y , Cottonwood C o t t o n w o o d Canyon, Canyon, Format!c!!.. hhas a s :cormed formed ii inl tthe h e rre e l aatively t i v e l y soft s o f t Carrr..el Carmel F ormation. The Entrada Entrada a k o t a Formations F o r m a t i o n s form form rresistant e s i s t a n t hogbacks, h o g b a c k s , the t h e Tropic T r o p i c Shale S h a l e forms forms and D Dakota a n o t h e r strike s t r i k e valley v a l l e y (fig. ( f i g . 22), 2 2 ) , and the t h e Straight S t r a i g h t Cliffs C l i f f s Formation Formation another f o r m s the t h e main m a i n Cockscomb . hogback. hogback. forms Immediately ood Creek I m m e d i a t e l y ",est w e s t of of Cottom,7 Cottonx^ood C r e e k are a r e the t h e fantastic f a n t a s t i c Rush Rush Beds. Beds. T h i s is i s the t h e only o n l y large l a r g e area a r e a on the t h e map where w h e r e the t h e landforms l a n d f o r m s of of This t h e Nav N a vaj a j o0 a re r e typic t y p i c ally a l l y developed. developed. the H e r e the t h e Navaj N a v a j o0,, vlhich w h i c h dips d i p s 20-·40 20-40 Here d e g r e e s , is i s cut c u t by several s e v e r a l sys s y s ttems e m s of of v e rtica r t i c a l joi j o i nnts. ts. degrees, E r o s i o n along along Erosio' t h e s e jjoints o i n t s has h a s produced p r o d u c e d an a n area a r e a of needles, n e e d l e s , spires, s p i r e s , buttes, b u t t e s , potholes, potholes, these and slot s l o t canyons. canyons. The Rus Rushh Be Beds c o n t i n u e about a b o u t 10 miles m i l e s north; n o r t h ; some some ds continue of this t h i s area a r e a has h a s ne n e ver v e r been b e e n explored. explored. of The southern s o u t h e r n edge e d g e of the t h e map area a r e a east e a s t of of the t h e Cockscomb is is part p a r t of of the t h e Paria P a r i a pla p l a ttfo f o rrm m .. This T h i s are a r e a can c a n be b e divided d i v i d e d into i n t o 2 physiographic physiographic u n i t s — W e s t Cove and the t h e Dak D a kota-Trop o t a - T r o p i cc Deneh. Bench. units--Wes R ecent c e n t acce a c c elerated lerated Re i44 144 erosion e r o s i o n is i s rapidly r a p i d l y dissecting d i s s e c t i n g tthe h e terrace t e r r a c e deposits d e p o s i t s that t h a t once o n c e covered covered all Hest Cove exposing a l l of of West e x p o s i n g tthe h e vvaricolored a r i c o l o r e d strata s t r a t a of of the t h e Carmel C a r m e l and and Entrada F ormations. Entrada Formations. IIn n m o s t of of West C o v e , tthe h e rocks r o c k s aare r e nearly n e a r l y flat flat most West Cove, l y i n g except e x c e p t for f o r the the w e s t arm tthat h a t rreaches e a c h e s nnorth o r t h along a l o n g tthe h e Cockscomb, Cockscomb, lying west w h e r e the t h e dip d i p of of tthe h e rrocks o c k s changes c h a n g e s from o 3° in i n several s e v e r a l hundred hundred where from 30° tto ffeet e e t and s t r e a m hhas a s cut c u t a strike s t r i k e vvalley a l l e y iin n the the W i n s o r Member of of the the and a stream Winsor Carmel Formation. Formation. Carmel The Dakota-Tropic D a k o t a - T r o p i c bbench e n c h is i s developed d e v e l o p e d on nearly n e a r l y flat-lying flat-lying strata Dakota s t r a t a of of the the D a k o t a and Tropic T r o p i c Formations. Formations. Remnants of an R e m n a n t s of an old old erosion with e r o s i o n surface s u r f a c e (once ( o n c e ccovered overed w i t h tterrace e r r a c e and and pediment p e d i m e n t deposits) deposits) are a r e scattered s c a t t e r e d across a c r o s s tthis h i s bench. bench. Because B e c a u s e tthe h e rocks r o c k s ddip i p gently g e n t l y to to of the tthe h e north n o r t h the t h e southern, s o u t h e r n , oor r sstructurally t r u c t u r a l l y hhigh i g h sside i d e of t h e bbench e n c h is is d i s s e c t e d by nnumerous u m e r o u s short, s h o r t , nnarrow a r r o w ccanyons a n y o n s tthat h a t oopen p e n iinto n t o West dissected l,;'est and E a s t Coves and dairville C anyon. East and A Adairville Canyon. At the t h e nnorth o r t h edge e d g e of of tthe h e DakotaDakotaAt T r o p i c bench b e n c h is i s Rockhouse Rockhouse M e s a , an a n outlier o u t l i e r of of Straight S t r a i g h t Cliffs Cliffs Tropic Hesa, S a n d s t o n e on on the the w e s t side s i d e of of tthe he P a r i a River. River. Sandstone west Paria S u p e r p o s i t i o n of the Superposition of the Paria R i v e r apparently a p p a r e n t l y created c r e a t e d this t h i s ooutlier u t l i e r bbut u t iit t is i s improbably improbably Paria River t h a t the the P aria R i v e r was eever v e r at a t aan n elevation e l e v a t i o n higher h i g h e r tthan h a n the t h e present present that Paria River s u r f a c e of of the t h e Brigham B r i g h a m Plains. Plains. st!t:face G e o m o r p h i c History History Geomorphic No dir d i r eect c t eevidence v i d e n c e iis s available available w i t h vlhich w h i c h tto o rreconstruct e c o n s t r u c t the the ~\lith ppre-Pleistoc r e - P l e i s t o c eene n e geomorphic g e o m o r p h i c hhistory i s t o r y of of tthe he P a r i a area. area, Paria Soon after a f t e r the the Soon d e p o s i t i o n of of E o c e n e strata, s t r a t a , tthe he C o l o r aado do P l a t e a u was p l i f t e d and deposition Eocene Color Plateau ,laS u uplifted tilted. tilted. o c k s ((if i f ever e v e r ddeposited) eposited) w e r e removed h e area area Eocene rrocks were removed from from tthe 145 145 by epirogenic e p i r o g e n i c uupwarping p w a r p i n g of of tthe h e Kaibab K a i b a b uuplift. plift. What \~at effect e f f e c t the the Eocene rrocks had on tthe unknown bbut Eocene o c k s had h e local l o c a l drainage d r a i n a g e ppattern a t t e r n is i s unknown u t any any e f f e c t s would would hhave a v e bbeen e e n vvery e r y bbroad. road. effects By tthe h e end h e Miocene M i o c e n e the the end of of tthe P a r i a drainage d r a i n a g e ssystem y s t e m was pprobably r o b a b l y ddeveloped e v e l o p e d and h e llandscape a n d s c a p e of of Paria and tthe tthe h e area a r e a was ffairly a i r l y similar s i m i l a r to t o the t h e landscape l a n d s c a p e today. today. most The most c o m p l i c a t e d pperiod e r i o d in i n the t h e ggeomorphic e o m o r p h i c evolution e v o l u t i o n of he P a r i a aarea r e a took took complicated of tthe Paria pplace l a c e near n e a r tthe h e end end of h e Pliocene. Pliocene. of tthe c l i m a t e became o r e humid humid The climate became m more and a pperiod e r i o d of of vvalley a l l e y ffilling, i l l i n g , alluvial a l l u v i a l fan f a n deposition, d e p o s i t i o n , and pediment and pediment f o r m i n g took t o o k pplace. lace. forming T h e s e sediments s e d i m e n t s filled f i l l e d tthe h e valleys v a l l e y s and and lowlands lowlands These tto o almost a l m o s t tthe h e 5200 5200 foot f o o t contour c o n t o u r line. line. Much of of the t h e modern drainage modern drainage s y s t e m was ssuperimposed u p e r i m p o s e d from from tthis h i s llevel. evel. system S e v e r a l areas a r e a s aalong l o n g the the Several Cockscomb w e r e bbelow e l o w tthis h i s level l e v e l aallowing l l o w i n g streams s t r e a m s tto o f l1mV' o w across a c r o s s it. it. Cockscomb were The Pliocene-Pleistocene P l i o c e n e - P l e i s t o c e n e conglomerate c o n g l o m e r a t e was ddeposited e p o s i t e d at a t tthis h i s time. time. S e v e r a l pperiods e r i o d s of e r o s i o n and e r r a c e and e d i m e n t fformation o r m a t i o n followed-followed' Several of erosion and tterrace and ppediment m o s t of of the t h e rresulting e s u l t i n g ddeposits e p o s i t s are a r e now bbeing e i n g ddissected i s s e c t e d bby y tthe h e modern modern most c y c l e of e r o s i o n ; at a t ppresent r e s e n t vvery e r y llittle i t t l e ddeposition e p o s i t i o n is i s ttaking a k i n g place place cycle of erosion; i n the t h e Paria P a r i a area--the a r e a — t h e area a r e a is i s bbeing e i n g severely s e v e r e l y eroded. eroded. in MINERAL RESOURCES From time of a t i m e tto o time t i m e tthe h e Paria P a r i a aarea r e a hhas a s bbeen e e n tthe h e site s i t e of w i d e variety v a r i e t y of of m i n i n g and and m i n e r a l eexploration. xploration. wide mining mineral d a t e no deposits deposits To date of economic e c o n o m i c vvalue a l u e hhave a v e been b e e n found f o u n d aalthough l t h o u g h some uunusual n u s u a l mineralization mineralization of ddoes o e s occur o c c u r at a t several s e v e r a l localities. localities. a r g e t for for m o s t of of the the The ttarget most e x p l o r a t i o n has h a s bbeen e e n tthe h e Chinle Chinle F o r m a t i o n although a l t h o u g h tthe h e Navajo, Navajo, exploration Formation D a k o t a , and and Straight S t r a i g h t Cliffs Cliffs F o r m a t i o n s hhave a v e bbeen e e n tthe h e oobject b j e c t of of Dakota, Formations i n v e s t i g a t i o n also. also. investigation Gold Gold hhas Moenkopi and and Chinle Gold a s bbeen e e n rreported e p o r t e d from from the t h e Moenkopi Chinle Formations F o r m a t i o n s of of tthe h e Paria P a r i a area. area. Lawson (1913) of 4 to Lawson ( 1 9 1 3 ) rreports e p o r t s aan n assay a s s a y of to 5 CCGts c e n t s per p e r ton; t o n ; several s e v e r a l attempts a t t e m p t s have h a v e been b e e n made to t o recover r e c o v e r the t h e gold gold bbut u t aas s yyet e t no feasible, f e a s i b l e , economic e c o n o m i c method m e t h o d hhas a s bbeen e e n found. found. Mercury Mercury metal M e r c u r y iis s aanother n o t h e r glamour glamour m e t a l that t h a t hhas a s bbeen e e n rreported e p o r t e d in in ttrace r a c e a"lOunts a m o u n t s in i n tthe h e Chinle. Chinle. S e v e r a l ssamples a m p l e s from the L e e s Ferry Ferry Several from the Lees area w e r e a~malyzed n a l y z e d by the t h e ,,,illemite w i l l e m i t e screen s c r e e n ttest e s t b-DUt u t tthe h e rresults e s u l t s were were a;::e'l ~v'8re n e g a t i v e (Phoenix. ( P h o e n i x , 1963, 1 9 6 3 , pp., 58). 58). negative. M e r c u r y like l i k e ggold old w i l l probably probably Hercury will rremain e m a i n a curiosity. curiosity. Manganese HU!lganese Manganese deposits d e p o s i t s are a r e ffound o u n d in i n tthe h e Chinle C h i n l e and and are are more encom:<lging mercury. e n c o u r a g i n g ttl1an h a n the t h e ggold o l d or or m ercury. perhaps perhaps manganese A m a n g a n e s e ddeposit e p o s i t is is i47 147 west llocated o c a t e d about a b o u t 10 miles miles w e s t of of Paria P a r i a iin n Park P a r k Gulch Gulch (Buckskin ( B u c k s k i n Gulch) Gulch) and although a l t h o u g h the t h e deposit d e p o s i t contains c o n t a i n s estimated e s t i m a t e d reserves r e s e r v e s of of 70,000 7 0 , 0 0 0 tons tons of mine of 10 percent p e r c e n t ore, o r e , it i t hhas a s nnot o t bbeen e e n possible p o s s i b l e tto o ooperate p e r a t e tthe he m i n e at a t aa profit of nnear-by p r o f i t bbecause e c a u s e of of the t h e lack l a c k of e a r - b y water w a t e r and and a distance d i s t a n c e of of over over 100 miles m i l e s to t o the t h e nnearest e a r e s t rrailroad a i l r o a d ((Gregory, G r e g o r y , 1948, 1 9 4 8 , pp.. 216). 216). Scattered Scattered m a r b l e - s i z e d nodules n o d u l e s of of m a n g a n e s e are a r e common at a t various v a r i o u s locales locales marble-sized manganese t h r o u g h o u t tthe h e Chinle C h i n l e •. throughout . Copper Copper A small s m a l l copper c o p p e r deposit d e p o s i t is i s located l o c a t e d in i n the t h e Navajo N a v a j o Sandstone S a n d s t o n e on tthe h e Cockscomb near n e a r the t h e head h e a d of of Notch N o t c h Canyon. Canyon. pp.. 148) 148) report: report: G r e g o r y and and Moore (1931, (1931, Gregory "Prospecting Hoenkopi, " P r o s p e c t i n g for f o r copper c o p p e r in i n tthe he M o e n k o p i , Chinle, C h i n l e , and and N a v a j o Formations F o r m a t i o n s has h a s bbeen e e n carried c a r r i e d oon n at a t a number number of of pplaces l a c e s iin n the the Navajo Paria V a l l e y , and and some low-grade l o w - g r a d e copper c o p p e r ore o r e is i s said s a i d to t o hhave a v e been been Paria Valley, s h i p p e d from from tthe he H a t t i e Green Green m ine, 2 m iles w e s t of of A dairville". shipped Hattie mine, miles west Adairville". This This i s apparently a p p a r e n t l y the t h e same deposit d e p o s i t mentioned m e n t i o n e d above. above. is The Horkings w o r k i n g s include i n c l u d e a 5 foot f o o t square s q u a r e adit a d i t that t h a t runs r u n s east e a s t 100 100 yyards a r d s or o r more m o r e into i n t o the t h e Cockscomb. T h e r e is i s no mineralization m i n e r a l i z a t i o n in i n the the There w a l l rrock o c k of of this t h i s a dit d i t near n e a r its i t s mouth, m o u t h , however h o w e v e r many small s m a l l ppieces i e c e s of wall copper m i n e r a l s ar a r ee s ccattered a t t e r e d throughout t h r o u g h o u t tthe h e mine m i n e dump indicating i n d i c a t i n g the the copper minerals a d i t intercepted i n t e r c e p t e d tthe h e de d e posit p o s i t somewhere somewhere along a l o n g its i t s length. length. adit m a i n deposit d e p o s i t is i s exposed e x p o s e d in i n a small s m a l l ppit i t about a b o u t 20 feet f e e t in in The main d i a m e t e r and 10 feet f e e t deep. deep. diameter As tthis h i s pit p i t is i s located l o c a t e d east e a s t of of and and above above tthe h e adit, a d i t , apparently a p p a r e n t l y the t h e purpose p u r p o s e of of it i t Has was tto o intercept i n t e r c e p t tthe h e vvein e i n at at depth d e p t h in i n ora.er o r d e r tto o calculate c a l c u l a t e reserves. reserves. The Halls w a l l s of of the t h e pit p i t as a s well well 148 148 as with a s bbroken r o k e n ppieces i e c e s of of rock r o c k in i n the t h e bottom b o t t o m are a r e impregnated impregnated w i t h veins, veins, l u m p s , and a n d ppatches a t c h e s of of beautiful b e a u t i f u l blue b l u e and green g r e e n ccopper o p p e r minerals, minerals, lumps, chiefly c h i e f l y azurite a z u r i t e and and m malachite. alachite. The deposit d e p o s i t is i s associated a s s o c i a t e d with w i t h a zone zone of sheering s h e e r i n g and and several s e v e r a l reef-like r e e f - l i k e masses m a s s e s of of crushed c r u s h e d and and cemented cemented of N a v a j o Sandstone S a n d s t o n e are a r e in i n tthe h e aarea. rea. Navajo A l t h o u g h this t h i s one deposit deposit Although a p p a r e n t l y is i s not n o t economical e c o n o m i c a l at a t present, p r e s e n t , much of of tthe h e Cockscomb Cockscomb in in apparently t h e Paria P a r i a area a r e a and h e area a r e a to t o the t h e south s o u t h has h a s the t h e same structural structural the and tthe rrelationships e l a t i o n s h i p s and more detailed d e t a i l e d exploration e x p l o r a t i o n may sometime s o m e t i m e uncover uncover d e p o s i t s of of m o r e economic e c o n o m i c promise. promise. deposits more Uranium Uranium Paria No economic e c o n o m i c uuranium r a n i u m deposits d e p o s i t s hhave a v e been b e e n found f o u n d in i n the the P a r i a or or surrounding and VerIlLiliuIl s u r r o u n d i n g areas a r e a s though t h o u g h much of of the t h e Cockscomb Cockscomb and V e r m i l i o n Cliffs Cliffs hhave a v e bbeen e e n pprospected r o s p e c t e d and staked s t a k e d out. out. G e o l o g i c factors f a c t o r s that t h a t \vould would Geologic t o ffavor a v o r uranium u r a n i u m deposition d e p o s i t i o n in i n tthe he P a r i a area a r e a include i n c l u d e local local Faria seem to rrelief e l i e f in i n tthe h e Shinarump S h i n a r u m p of of about a b o u t 80 feet f e e t (0-80 ( 0 - 8 0 feet), f e e t ) , well w e l l developed developed and tthick h i c k channel c h a n n e l ddeposits, e p o s i t s , local l o c a l areas a r e a s of of non-deposition, n o n - d e p o s i t i o n , the the and p r e s e n c e of of bboth oth m u d s t o n e and and conglomerate c o n g l o m e r a t e in i n the t h e channel, c h a n n e l , the the presence mudstone p r e s e n c e of of carbonized c a r b o n i z e d and ppetrified e t r i f i e d wood, and a w e l l developed developed presence well e x t e n s i v e sandstone--illudstone s a n d s t o n e - m u d s t o n e sequence s e q u e n c e in i n the the M o n i t o r Butte B u t t e Member. Member. extensive N.onitor The m most o s t likely-looking l i k e l y - l o o k i n g area a r e a for f o r uranium u r a n i u m is i s in i n the t h e northwest northwest corner where c o r n e r of of the t h e map area area w h e r e the t h e Shinarump S h i n a r u m p appears a p p e a r s to t o intertongue i n t e r t o n g u e with with the M o n i t o r Butte. Butte. the Monitor H e r e the t h e "upper " u p p e r Shinaru.1lp" S h i n a r u m p " contains c o n t a i n s numerous numerous Here c a r b o n i z e d logs l o g s covered covered w i t h a light-yellow l i g h t - y e l l o w ppm'ider. owder. carbonized with T h i s powder is This powder is a l s o distributed d i s t r i b u t e d through t h r o u g h tthe h e conglomerate c o n g l o m e r a t e and sandstone s a n d s t o n e deposit d e p o s i t that that also 149149 contains c o n t a i n s the t h e logs. logs. material Much of of the the m a t e r i a l was tested t e s t e d for f o r radioactivity radioactivity bbut u t the t h e rresults esults w e r e negative. negative. were y e l l o w powder i s pprobably r o b a b l y jarosite, jarosite, The yellow powder is a hydrated h y d r a t e d potassium p o t a s s i u m iron i r o n sulfate s u l f a t e that t h a t is i s often o f t e n mistaken m i s t a k e n for f o r uranium. uranium. As conditions c o n d i t i o n s for f o r uuranium r a n i u m accumulation a c c u m u l a t i o n are a r e favorable f a v o r a b l e pperhaps e r h a p s more more m e t h o d i c a l prospecting p r o s p e c t i n g with with m o d e r n equipment e q u i p m e n t may succeed s u c c e e d iin n finding finding methodical modern e c o n o m i c deposits. deposits. economic ·Coal Coal Kaiparowits IIf f present p r e s e n t predictions p r e d i c t i o n s are a r e ttrue, r u e , the the K a i p a r o w i t s rregion e g i o n may soon become one of s o o n become of the t h e largest l a r g e s t coal-producing c o a l - p r o d u c i n g areas a r e a s in i n tthe h e western western U n i t e d States. States. United G e o l o g i c a l Survey S u r v e y and and tthe he U t a h State State The U. S. Geological Utah G e o l o g i c a l Survey S u r v e y are a r e currently currently m a p p i n g parts p a r t s of of the t h e Kaiparowits Kaiparowits Geological mapping r e g i o n in i n order o r d e r tto o rreclassify e c l a s s i f y federal f e d e r a l and s t a t e lands l a n d s that t h a t contain contain region and state c o a l resources. resources. coal g o v e r n m e n t as a s well w e l l as a s pprivate r i v a t e industry i n d u s t r y is i s mapping, mapping, The government m e a s u r i n g , testing, t e s t i n g , and estimating e s t i m a t i n g coal c o a l reserves. reserves. measuring, One oorr more more Dew new ccommunities o m m u n i t i e s will w i l l pprobably r o b a b l y be b e bbuilt u i l t iin n eastern e a s t e r n Kane County C o u n t y as a s the the r e s u l t of of tthe h e coal c o a l mining m i n i n g operations. operations. result The m a i n coal-bearing c o a l - b e a r i n g rocks rocks main a r e in i n the t h e Smoky Hollow H o l l o w and John John H e n r y Members of of the t h e Straight S t r a i g h t Cliffs Cliffs are Henry Formation, Formation. A l t h o u g h both b o t h these t h e s e members members are a r e expos e x p o s eedd in i n the the P a r i a area, area, Although Paria e c o n o m i c deposits d e p o s i t s a re r e not n o t known i n tthe h e area. area. economic kno,Vll in A ffew t h i n , impure i m p u r e coal coal e,,, thin, seams w e r e seen s e e n when e a s u r i n g the t h e Straight S t r a i g h t Cliffs Cliffs F o r m a t i o n bbut u t none none seams were whe n m measuring Formation w e r e of e c o n o m i c int i n teerest. rest. were of economic Some coal Paria c o a l is i s ppresent r e s e n t in i n tthe h e Dakota D a k o t a Formation F o r m a t i o n in i n tthe he P a r i a area area s m a l l abandone a b a n d o n e dd m i n e is i s llocated o c a t e d above above A d a i r v i l l e Canyon Canyon on on and one small mine Adairville tthe h e east e a s t side s i d e of of tthe h e Paria Paria R iver. River. T h i s coal c o a l seam seam iis s the t h e tthickest h i c k e s t of of This 150 tthree h r e e or o r four f o u r coal c o a l seams tthat h a t ooccur c c u r in i n a cyclic c y c l i c sequence s e q u e n c e in i n tthe h e lower lower ppart a r t of of the t h e Dakota Dakota F ormation. Formation. is i s aabout b o u t 3 feet f e e t tthick. hick. h i c k e s t seam of of fairly f a i r l y pure p u r e coal coal The tthickest These T h e s e beds b e d s apparently a p p a r e n t l y have h a v e little l i t t l e horizontal horizontal miles ppersistence e r s i s t e n c e because b e c a u s e equivalent e q u i v a l e n t strata s t r a t a a few m i l e s to t o the t h e north n o r t h contain contain o n l y coal c o a l streaks. streaks. only But tthe h e deposits d e p o s i t s of of A d a i r v i l l e Canyon Canyon could could But Adairville c o n c e i v a b l y bbe e m i n e d again a g a i n if i f coal c o a l was nneeded e e d e d locally. locally. conceivably mined B uilding Materials BuildirtgMaterials of the t h e rrocks o c k s in i n tthe h e Paria P a r i a area a r e a could c o u l d be b e used u s e d for f o r various various Many of bbuilding u i l d i n g materials. materials. a r l i e s t inhabitants i n h a b i t a n t s of of tthe h e area, a r e a , tthe h e Indians, Indians, The eearliest u s e d tthe h e chert c h e r t from from tthe h e Kaibab K a i b a b and and tthe h e ppetrified e t r i f i e d wood from from tthe h e Chinle Chinle used t o make arrow a r r o w heads. heads. to The rim r i m of of Sand Sand Gulch G u l c h is i s locally l o c a l l y ccovered o v e r e d with with ttheir h e i r scraps s c r a p s and rejects r e j e c t s •. of the t h e bbuildings u i l d i n g s at at P a r i a are a r e constructed c o n s t r u c t e d of of siltstone siltstone Paria . Most Most of and sandstone s a n d s t o n e from from tthe h e Glen G l e n Canyon Canyon Group and Moenkopi Moenkopi Formation. Formation. and The red r e d and orange o r a n g e slabs s l a b s of of sandstone s a n d s t o n e and and siltstone s i l t s t o n e are a r e quite quite d e c o r a t i v e but b u t similar s i m i l a r rocks r o c k s are a r e found f o u n d ccloser l o s e r to to m a r k e t areas. areas. decorative market The Utah Highway Department U t a h State S t a t e Highway D e p a r t m e n t uuses s e s sand s a n d and gravel g r a v e l from from well tthe h e Paria P a r i a River R i v e r as as w e l l as a s other o t h e r rrecent e c e n t deposits d e p o s i t s in i n road r o a d construction. construction. Some of of the t h e sand s a n d deposits d e p o s i t s and sand s a n d uunits n i t s in i n the t h e Entrada E n t r a d a Sandstone Sandstone would uundoubtedly markets would n d o u b t e d l y pprove r o v e useful u s e f u l if i f tthere h e r e were w e r e local local m a r k e t s because because s i m i l a r deposits d e p o s i t s were w e r e uused s e d extensively e x t e n s i v e l y in i n the t h e construction c o n s t r u c t i o n of of Glen Glen similar Canyon Dam. Canyon The outlook o u t l o o k for f o r tangible t a n g i b l e economic e c o n o m i c products p r o d u c t s in i n the t h e Paria P a r i a area area i s nnett o t very v e r y ppromising r o m i s i n g at a t ppresent; r e s e n t ; if i f a local l o c a l market m a r k e t suddenly s u d d e n l y developed developed is 151 151 o r new m e t h o d s for f o r rrecovering e c o v e r i n g trace t r a c e elements e l e m e n t s from from the t h e Chinle C h i n l e were were or methods d e v e l o p e d this t h i s ooutlook u t l o o k could c o u l d improve. improve. developed But oone But n e vvery e r y important i m p o r t a n t iintangible n t a n g i b l e resource r e s o u r c e of of the t h e Paria P a r i a area area d o e s exist e x i s t and h i s is i s tthe h e scenic s c e n i c and and semi-wilderness s e m i - w i l d e r n e s s aspect a s p e c t of of the the does and tthis country. country. L i k e many other o t h e r areas a r e a s iin n tthe he A m e r i c a n West, W e s t , the t h e scenic scenic Like American ppossibilities o s s i b i l i t i e s greatly g r e a t l y ooutweigh u t w e i g h any a n y slight slight m i n e r a l values. values. mineral With With t h e great g r e a t iinflux n f l u x of of ppeople e o p l e attracted a t t r a c t e d tto o tthe h e rregion e g i o n bby y Lake L a k e Powell, Powell, the scenic s c e n i c surrounding s u r r o u n d i n g territories t e r r i t o r i e s such s u c h as a s Paria P a r i a may increase i n c r e a s e in in i m p o r t a n c e as a s areas a r e a s ffor o r camping, c a m p i n g , jjeeping, e e p i n g , hiking, h i k i n g , and and sight-seeing. sight-seeing. importance B u r e a u of of Land i s currently c u r r e n t l y investigating i n v e s t i g a t i n g much of of the the The Bureau Land Management Management is c o u n t r y along a l o n g tthe h e Cockscomb Cockscomb for f o r recreation r e c r e a t i o n ppurposes. urposes. country P e r h a p s then then Perhaps tthe h e scenery s c e n e r y of of P a r i a can c a n bbe e ppreserved r e s e r v e d and and enjoyed e n j o y e d for f o r many Paria ggenerations. enerations. STRATIGRAPHIC SECTIONS A A stratigraphic s t r a t i g r a p h i c section s e c t i o n 'vas was measured m e a s u r e d and described d e s c r i b e d for f o r each each formation exposed at the surface. The location of sections formation exposed a t the s u r f a c e . l o c a t i o n of s e c t i o n s was determined d e t e r m i n e d in i n respect r e s p e c t to t o exposure e x p o s u r e and accessability~ a c c e s s a b i l i t y C Color o l o r terms terms and related r e l a t e d numbers n u m b e r s are a r e from from Goddard, G o d d a r d , (1948). (1948). and 1 . - Sand Sand Gulch G u l c h section, s e c t i o n , El/2 E l / 2 sec. s e c . 11, 1 1 , T. T . 42 S., S . , R. 2 W. 1.- Lower Lower Triassic: Triassic: Moenkopi Formation: Formation: Siltstone, mudstone, S i l t s t o n e , grayish-red, g r a y i s h - r e d , thin-bedded; t h i n - b e d d e d ; and and m u d s t o n e , pale pale reddish-brown r e d d i s h - b r o w n to t o dark d a r k reddish-brown, r e d d i s h - b r o w n , fissie; f i s s i L e ; unmeasured. unmeasured. Note.N o t e . - Moenkopi-Kaibab M o e n k o p i - K a i b a b contact c o n t a c t is i s poorly p o o r l y exposed e x p o s e d bbut u t apparently apparently e v e n throughout t h r o u g h o u t locality; l o c a l i t y ; the t h e yellow, y e l l o w , fisSQe f i s s t L e mudstone m u d s t o n e transtrans­ even i t i o n zone z o n e described d e s c r i b e d in i n text t e x t is i s about a b o u t 2 feet f e e t thick. thick. ition ThickM i d d l e Permian: Permian: ThickMiddle Kaibab Formation: ness Kaibab F o r m a t i o n : ness Alpha (ft) A l p h a Member (ft) 6. 6 . Limestone, L i m e s t o n e , grayish-orange g r a y i s h - o r a n g e (lOYR (10YR 7/4) 7 / 4 ) with with numerous n u m e r o u s intraclasts; i n t r a c l a s t s ; in i n beds b e d s 1 tto o 6 ft f t thick. thick. 5. 5. Chert SGme 3ho~ indistinct C h e r t i3 i s ~bs2nt. absent. Some beds b e d s show indistinct cross Entire c r o s s stratification. stratification. E n t i r e unit u n i t iis s resisresis­ tant t a n t tto o erosion e r o s i o n and it i t weathers w e a t h e r s into i n t o massive massive c l i f f ss and steps s t e p s ----------------------------30 30 cliff Limestone) L i m e s t o n e , yellmvish-gray y e l l o w i s h - g r a y (5Y 8/1), 8 / 1 ) , ''leathers weathers light l i g h t brown and and intercalated i n t e r c a l a t e d grayish-white grayish-white chert. Unit chert. U n i t is i s wavy bedded b e d d e d and forms f o r m s cliffs cliffs and and slopes s l o p e s -------------·--------------------30 • •—30 T o t a l Alpha A l p h a Member --------------,- -----60 60 Total Beta B e t a Member 4. Limestone, 4. L i m e s t o n e , same as a s 3 but b u t with w i t h more m o r e silt s i l t and and sand. Unit and slopeG-36 sand. U n i t forms f o r m s cliffs, c l i f f s , ledges, l e d g e s , and slopes-36 3. Limestone. 3. L i m e s t o n e , yyellmdsh-orange e l l o w i s h - o r a n g e (lOYR (10YR 7/6) 7/6) weathers grayish-orange; bedding massive w e a t h e r s g r a y i s h - o r a n g e ; b e d d i n g m a s s i v e with with Unit bbedded e d d e d and nnodular o d u l a r chert. chert. U n i t vvery e r y fossilfossil­ iferous, Few i f e r o u s , especially e s p e c i a l l y in i n cherty c h e r t y beds. beds. distinct d i s t i n c t bedding b e d d i n g planes p l a n e s form form notches n o t c h e s in i n otherother­ w i s e vert v e r t iic c aa l cliff----------·----------------48 cliff—— • 48 wise 2. Siltstone, 2. S i l t s t o n e , pale p a l e yellO\vish-gray, y e l l o w i s h - g r a y , llimy, i m y , thinthinbedded; b e d d e d ; forms f o r m s nnotch o t c h between b e t w e e n t\VO two resis r e s i s tant tant uunits n i t s ---------------.,..------------------------•——• • — —— 2 153 M i d d l e Permian P e r a i a n - Continued Continued Hiddle Kaibab K a i b a b Formation F o r m a t i o n - Continued Continued Beta B e t a Hember Member - Continued Continued 1. 1. O u a r t z i t e , ppale a l e yyellowish-orange e l l o w i s h - o r a n g e (lOYR (10YR 8/4) 8/4) Quartzite, i n hhorizonta o r i z o n t a beds b e d s 1 to t o 3 ft f t thick. thick. in A b u n d a n t chert c h e r t and and iron i r o n nodules. nodules. Quartz Abundant Quartz f i n e - t o medium-grained, m e d i u m - g r a i n e d , well-sorted w e l l - s o r t e d and wellfine-to and wellrounded. U n i t form form rresistant e s i s t a n t ledges l e d g e s in in rounded. Unit bbottom o t t o m of of Sand Sand Gulch G u l c h --------------------- 16 Total Bee ta 102 T o t a l of of exposed exposed B t a Hember Member ------- 102 Total T o t a l of of exposed e x p o s e d incomplete incomplete Kaibab Formation -162 Kaibab F o r m a t i o n --------------------162 N o t e . - These T h e s e are a r e oldest o l d e s t rrocks o c k s exposed e x p o s e d at a t the t h e surface s u r f a c e on the t h e map area. area. Note.a b o u t hhalf a l f of of tthe h e Kaibab Kaibab F o r m a t i o n is i s exposed. exposed. Only about Formation 2.Section 2 . - Road Creek C r e e k Section, S e c t i o n , El/2 E l / 2 sec. s e c . 35, 3 5 , T. 441 1 S., S . , R. 2 W. S e c t i o n is is offset miles o f f s e t twice t w i c e about a b o u t 1 1/2 1/2 m i l e s bbecause e c a u s e of of faulting. faulting. Upp~r Upper Tr:Ul.ssir:-: Triassic: Chinle C h i n l e Formation: Formation: S i l t s t o n e , reddish-brown, reddish-brown, m a s s i v e ; unmeasured unmeasured Siltstone, massive; Note.N o t e . - Shinarump S h i n a r u m p absent a b s e n t here; h e r e ; Noenkopi-Chinle M o e n k o p i - C h i n l e contact c o n t a c t broadly broadly undulating ~vith u n d u l a t i n g surface surface w i t h 2 ft f t or o r lless e s s of of relief. relief. Lower and Middle M i d d l e (?) ( ? ) Triassic: Triassic: Moenkopi Formation: Formation: Hoenkopi Upper Upper Red Member (Middle ( M i d d l e (?) ( ? ) Triassic): Triassic): 16. Sandstone, 16. S a n d s t o n e , dark d a r k reddish-brovm r e d d i s h - b r o w n (lOR (10R 3/4), 3/4), silty, micaceous, silty, m i c a c e o u s , ppoorly o o r l y sorted, s o r t e d , thinthinmassive; bbedded e d d e d to to m a s s i v e ; forms f o r m s knobby knobby c 1l ij ff ff -----.------------------.---------------- 18 15. 15. Siltstone, mudstone~ and sandstone, Siltstone, m u d s t o n e , and sandstone, grayish-red g r a y i s h - r e d (lOR (10R 44/2), / 2 ) , thin-to t h i n - t o mediummediumbedded, b e d d e d , similar s i m i l a r to t o other o t h e r red r e d units u n i t s of of Hoenkopi. M o e n k o p i . Flute F l u t e cas c a s tts s and and ripple r i p p l e marks marks present p r e s e n t on some beds; b e d s ; unit u n i t forns f o r m s steep steep s l o p ee ss ----------------------------------------:.-- 8811 Glop 99 T o t a l Upper Member ---------------99 Total Upper Red Hember Note.-miles NW N o t e . - Section S e c t i o n off--set o f f - s e t 1 1/2 1/2 m i l e s east e a s t to to N W 1/4 1/4 sec. s e c . 30, 3 0 , T. T , l}l 4 1 S., S., R. J. 1 H. W, 154· 154 Middle and M Middle M i d d l e Red Member Member (Lower (Lower and i d d l e (?) ( ? ) Triassic): Triassic): 11. Siltstone, moderate-brown 11. Siltstone, m o d e r a t e - b r o w n (5 YR 5/4), 5/4), sypsiferous, s y p s i f e r o u s , sandy, s a n d y , ppoorly o o r l y sorted, s o r t e d , numerous numerous intercalated gypsum and i n t e r c a l a t e d thin t h i n bbeds e d s of of gypsum and b l u i s h - g r e e n claystone. claystone. Gypsum content content bluish-green i n c r e a s e s uupwards p w a r d s in i n the t h e member. Interincreases Interbbedding e d d i n g of of rred e d and and white w h i t e bbeds e d s causes c a u s e s mottling mottling and banding. banding. Gypsum is m a i n cementing c e m e n t i n g agent. agent. and Gyps~~ is main U n i t and and forms f o r m s slopes, s l o p e s , bbadlands, a d l a n d s , and and ragged ragged Unit c l i f f s ----.------------------------------- 296 cliffs 10. S i l t s t o n e , claystone, c l a y s t o n e , and s a n d s t o n e , reddishreddish10. Siltstone, and sandstone, b r o w n , lithologies l i t h o l o g i e s interbedded, i n t e r b e d d e d , thin-to thin-to brown, fissile; marked f i s s i l e ; unit u n i t hhighly i g h l y rripple ipple m a r k e d .,..------- 30 30 9. Sandstone, 9. S a n d s t o n e , reddish-brown, r e d d i s h - b r o w n , rresistant, e s i s t a n t , finefine­ grained, micaceous; g r a i n e d , poorly p o o r l y sorted, sorted, m i c a c e o u s ; interbedded interbedded with w i t h several s e v e r a l tthin h i n shaly s h a l y siltstones s i l t s t o n e s and and mud s t o n e beds b e d s -------------------------------- 12 12 stone 8. Claystone and siltstone, dark reddish-brown 8, C l a y s t o n e and s i l t s t o n e , d a r k r e d d i s h - b r o w n (lOR (10R 3/4), 3 / 4 ) , fissile f i s s i l e and and thin t h i n bedded; b e d d e d ; similar similar tto o much of of Lower Lower Red Member Member --------------- 6_ 6 T o t a l l-1iddle M i d d l e Red Member Total 344 ------------.344 Note.T.. 4411 S., N o t e , - Section S e c t i o n oIf-set o f f - s e t 1 1/2 1/2 miles m i l e s north n o r t h to t o E 1/2 1/2 3eo:::. s e c 223, 3, T S,, R. 2 W. Virgin Member (Lower V i r g i n Limestone L i m e s t o n e Member (Lower Triassic) Triassic) 7. 7 . Limestone, L i m e s t o n e , yyellowish-orange e l l o w i s h - o r a n g e (lOYR (10YR 77/6), / 6 ) , siltsilt­ sstone, t o n e , light l i g h t olive o l i v e gray g r a y (5Y 6/1) 6 / 1 ) and sandy and sandy limestone, l i m e s t o n e , grayish-orange g r a y i s h - o r a n g e (lOYR (10YR 7/5) 7 / 5 ) iin n thin, thin, lenticular beds. Much of unit is wavy bedded lenticular beds. of u n i t i s bedded w i t h some cross c r o s s llaminations. aminations. Q u a r t z grains grains with Quartz v e r y fine, fine, m o d e r a t e l y sorted; s o r t e d ; ccaps aps m esas 12_ very moderately mesas--12 Total V irgin L i m e s t o n e Member Total Virgin Limestone Member -------- 12 Lower Red Member (Lower Triassic): Triassic): LOvler Hember (Lower 6. Sandstone, same as 6. Sandstone, a s 2, 2 , and and limy l i m y siltstone, s i l t s t o n e , pale pale reddish-brown (lOR 5/ L t ), sand fine r e d d i s h - b r o w n (10R 5 / 4 ) , s a n d f i n e grained, grained, a r k o s i c , ppoorly o o r l y sorted; s o r t e d ; complex sedimentary arkosic, complex sedimentary s t r u c t u r e s include i n c l u d e interference i n t e r f e r e n c e ripple r i p p l e marks, marks, structures s c o u r marks, m a r k s , small s m a l l load l o a d casts, c a s t s , and coo.plex complex scour c r o s s lLaminations. aminations. U n i t fforms o r m s steep, s t e e p , light light cross Unit c o l o r e d slope slope w i t h rresistant e s i s t a n t ledges l e d g e s ------- 18 18 colored with 5. S i l t s t o n e , same aas s 1 - \'7ith w i t h thin t h i n bbeds e d s of of 5. Siltstone, p l a t y , ppoorly o o r l y sorted, s o r t e d , fine-grained fine-grained platy, s a n d s ttone one — • — 24 sands -----0----0----------------------- iss Lower Lower Red Member (Lower (Lower Triassic): T r i a s s i c ) : - Continued Continued 4. 4. 3. 3. 2. 2. 1. 1. Sandstone, with S a n d s t o n e , s~~e same as as 2 w i t h a few few shaly s h a l y beds beds t h i n gypsum gypsum --------------.----------- 4 and thin S i l t s t o n e and mudstone m u d s t o n e same as a s 1 --------- 30 Siltstone Sandstone, S a n d s t o n e , ppale a l e reddish--brown r e d d i s h - b r o w n (lOR (10R 5/4), 5 / 4 ) , poorly poorly s o r t e d , micaceous, m i c a c e o u s , silty. silty. U n i t is i s thin t h i n bedded bedded sorted, Unit w i t h abundant a b u n d a n t ripple r i p p l e marks m a r k s and and ripple r i p p l e cross cross with l a m i n a t i o n s ; ledge l e d g e former f o r m e r ------------------11 laminations; Siltstone S i l t s t o n e and and silty s i l t y shale, s h a l e , grayish-red g r a y i s h - r e d (lOR (10R 4/2), 4/2), "Tith w i t h distinct d i s t i n c t pparting a r t i n g bedding b e d d i n g planes. planes. Very V e r y little l i t t l e sand, s a n d , but b u t pparts a r t s of of unit u n i t more m o r e resistant resistant than Ripple t h a n others. others. R i p p l e marks m a r k s very v e r y common; common; u n i t very v e r y micaceous; m i c a c e o u s ; forms f o r m s slopes s l o p e s and and unit rrounded o u n d e d ledges ledges 64 ---------------------------64 T o t a l Lower Lower Red Member Total 141 -------------141 T o t a l Moenkopi F o r m a t i o n ------------ 760 760 Total Hoenkopi Formation 3 . - Gingham Gingham Skirt S k i r t Butte B u t t e section, s e c t i o n , NW NW 1/4 1/4 sec. s e c . 19, 1 9 , T. T . 41 S., S . , R. 1 W. 3.Sec:tion S e c t i o n starts s t a r t s 3/4 3 / 4 mile m i l e w'est w e s t of of Gingham Gingham Skirt S k i r t Butte B u t t e and ends e n d s at at t h e top t o p of of ti:he h e "squaw "squaw skirts". skirts". tile Upper Triassic: Upper Triassic: Wingate W i n g a t e Sandstone S a n d s t o n e undescribed undescribed Unconformity Unconformity Chinle C h i n l e Formation: Formation: Owl Rock Hember: Member: ; 7. 7 . Hudstone M u d s t o n e and and sandy s a n d y siltstone, s i l t s t o n e , moderate m o d e r a t e reddishreddishbrmm brown (lOR (10R 5/6) 5 / 6 ) and and yellowish-gray y e l l o w i s h - g r a y (5Y 8/1), 8/1), non-bentonitic, Unit n o n - b e n t o n i t i c , horizontally h o r i z o n t a l l y bbedded. edded. Unit b o t h mottled m o t t l e d and and banded; b a n d e d ; red r e d mudstone m u d s t o n e weathers weathers both i n t o shiny s h i n y chips. chips. Much of of member member poorly poorly into Nuch e x p o s e d ; boundary b o u n d a r y with w i t h Petrified P e t r i f i e d Forest Forest exposed; Member arbitrary, a r b i t r a r y , plac'2d p l a c e d vlhere w h e r e bentonite bentonite Hember i s apparently a p p a r e n t l y ahse::J.t a b s e n t or o r minor; m i n o r ; approximate approximate is t h i c k n e s ss -----------------------------------100+ —• 100+ thicknes T o t a l Owl Rock Member approximately--:-lOO+ approximately—100+ Total P e t r i f i e d Forest F o r e s t 1'1cmber Member Petr.ified 6. 6 . Mmlstone M u d s t o n e in i n alternating a l t e r n a t i n g bands b a n d s of of pale p a l e red, red, pink, p i n k , and orange; o r a n g e ; bedding b e d d i n g obscure o b s c u r e but but a p p a r e n t l y tthin h i n bedd€..d b e d d e d to t o massive.' massive. apparently S a n d s t o n e rare; r a r e ; bbentonite e n t o n i t e increases increases Sandstone dowmmrds downwards ---— erodes e r o d e s to t o rounded r o u n d e d slopes s l o p e s _____ 167 167 156156 Upper Upper Triassic T r i a s s i c - Continued Continued Chinle C h i n l e Formation F o r m a t i o n - Continued Continued Petrified P e t r i f i e d Forest F o r e s t Hember Member - Continued Continued 5. 5. 4. 4. Chert, C h e r t , mottled m o t t l e d ppale-green a l e - g r e e n (56 7/2) 7 / 2 ) to to grayish-pink massive; g r a y i s h - p i n k (5R 8/2), 8/2), m a s s i v e ; forms forms ledge ledge 6 Hudstone, M u d s t o n e , vvaricolored, a r i c o l o r e d , vanded, v a n d e d , mottled, mottled, bbright r i g h t shades s h a d e s of of rred, e d , pink, p i n k , purple, p u r p l e , blue, blue, g r a y , orange o r a n g e and bro~m; b r o w n ; bentonitic, bentonitic, gray, b e d d i n g obscure; o b s c u r e ; hhorizontal o r i z o n t a l bands b a n d s 2 tto o 20 bedding f t tthick; h i c k ; sandstone s a n d s t o n e increases i n c r e a s e s towards t o w a r d s base. base. ft U n i t e r o d e s t o r o u n d e d s l o p e s Unit erodes to rounded slopes ------------- 309 Total T o t a l Petrified P e t r i f i e d Forest F o r e s t Hember Member -------- 482 Monitor Butte Monitor B u t t e Member: Member: 3 . Mudstone, M u d s t o n e , sandstone, s a n d s t o n e , and and conglomerate c o n g l o m e r a t e complexly complexly 3. i n t e r b e d d e d ; bbanded a n d e d and vvaricolored a r i c o l o r e d bblue l u e and interbedded; g r a y , bbright r i g h t colors c o l o r s of of Petrified Petrified F o r e s t Member gray, Forest lacking. B e d d i n g highly h i g h l y lenticular, l e n t i c u l a r , variable; variable; lacking. Bedding c h a n n e l cut c u t and and fill f i l l structures; s t r u c t u r e s ; cross c r o s s stratistrati­ channel f i c a t i o n common. U n i t forms f o r m s ledges l e d g e s and fication Unit s t e e p rroundeu o u n d e d slope3 s l o p e s --------_.------------ 1[.5 145 steep 2. 2. Sandstone; S a n d s t o n e ; yellowish-gray y e l l o w i s h - g r a y (5Y 7/2), 7 / 2 ) , thinthint o thick-bedded; t h i c k - b e d d e d ; fine-grained f i n e - g r a i n e d and and silty silty to with w i t h pebbles p e b b l e s and abundant a b u n d a n t interstitial interstitial clay. G e n e r a l l y where w h e r e Shinarump'is Shinarumpfis clay. Generally a b s e n t this t h i s unit u n i t is i s grayish-red g r a y i s h - r e d and more absent and more s i l t y ; color c o l o r and lithalogic l i t h a l o g i c variation v a r i a t i o n along along silty; strike Contains s t r i k e considerable. considerable. C o n t a i n s abundant abundant p e t r i f i e d wood locally. locally. U n i t fornls f o r m s rounded rounded petrified Unit cliffs c l i f f s and and steep s t e e p slopes s l o p e s ----------------.---' — 40 T o t a l Monitor M o n i t o r Butte B u t t e Member Member ----------- 185 185 Total Shinannnp S h i n a r u m p Hember: Member: 1. Sandstone 1, S a n d s t o n e and conglomerate, c o n g l o m e r a t e , very v e r y pale-orange pale-orange (10YR 8/3), 8 / 3 ) , grayish-yellow g r a y i s h - y e l l o w (5Y 88/4) / 4 ) and light (lOYR and light o l i v e - g r a y (5Y 5/2) 5 / 2 ) with w i t h some beds b e d s stained stained olive-gray d a r k e r colors. colors. C h e r t ppebbles e b b l e s up tto o 1I in. in, darker Chert iin n diameter. diameter. S a n d s t o n e v e r y f i n e t o c o arse; Sandstone very fine-to coarse; some bbeus e d s ,\Tell-sorted w e l l - s o r t e d others o t h e r s poorly p o o r l y sorted; sorted; t h i n bedded b e d d e d at a t base b a s e massive m a s s i v e at a t ttop. o p . l1e,nber Member thin ccoarsens o a r s e n s uith w i t h increasing i n c r e a s i n g conglomerate c o n g l o m e r a t e up~\Tards. upwards. U n i t h i g h l y c r o s s l a m i n a t e d w i t h l e n t i cular Unit highly cross laminated with lenticular b e d ; many l o c a l u n c o n f o r m i t i e s , c h a n n e ls bed; local unconf ormi t ie3, channeL; and diastems. d i a s t e r n s . l.cntels L e n t e l s of of blue--green b l u e - g r e e n claystone claystone n e a r base b a s e in i n channels c h a n n e l s cut c u t in i n Moenkopi Moenkopi Formation. Formation, near 157 Upper U p p e r TriassicT r i a s s i c - Continued Continued Chinle FormationC hinle F o r m a t i o n - Continued Continued Shinarump Member- Continued S h i n a r u m p MemberContinued Local L o c a l rrelief e l i e f of of bbasal a s a l contact c o n t a c t 30 tto o 80 feet. Unit feet. U n i t forms f o r m s vvertical e r t i c a l cliff c l i f f ---------;...80 -80 T o t a l Shinarump S h i n a r u m p Member --------------:....- 8800 Total T otal C hinle F o r m a t i o n ------------,.-.847 -847 Total Chinle Formation Cockscomb Section, w. Section 44.. - Cockscomb S e c t i o n , C. sec. s e c . 31, 3 1 , T. T . 441 1 S., S . , R. 1 W. Section measured m e a s u r e d aalong l o n g abandoned a b a n d o n e d rroad o a d used u s e d tto o construct c o n s t r u c t power power lines. lines. Triassic: T riassic: Kayenta K a y e n t a Formation: Formation: Sandstone, S a n d s t o n e , ccross r o s s laminated l a m i n a t e d in i n horizontal h o r i z o n t a l bbeds; e d s ; unmeasured. unmeasured. Moenave Moenave Formation: Formation: Springdale S p r i n g d a l e Sandstone S a n d s t o n e Member: Member: 6. Sandstone, 6. S a n d s t o n e , same as a s 5 bbut u t with w i t h thinner t h i n n e r bbeds e d s and and Unit more ssilt; i l t ; bbeds e d s hhighly i g h l y llenticular. enticular. U n i t forms forms l e d g y , bbroken r o k e n cliff c l i f f ----------------------- 83 83 ledgy, 5. 5. Sandstone, Sandstone, m moderate o d e r a t e rred e d (5R 5/5) 5 / 5 ) with with purplish Sandp u r p l i s h ccast a s t from from short s h o r t distance. distance. Sand­ stone s t o n e vvery e r y ppoorly o o r l y sorted; s o r t e d ; wide w i d e variety variety of grain g r a i n textures t e x t u r e s and colors; c o l o r s ; angular, angular, of bbroken r o k e n grains, g r a i n s , few few round r o u n d grains. grains. A c c e s s o r i e s iinclude n c l u d e feldspar, f e l d s p a r , bblack l a c k mica, mica, Accessories and h e r t grains. grains. Bed highly h i g h l y lenticular, lenticular, and cchert c r o s s llaminated a m i n a t e d both b o t h low and and hhigh i g h angles; angles; cross r u n c a t i o n s , ddiastems, i a s t e r n s , channels. channels. Unit many ttruncations, Unit fforms orms m a s s i v e , vertical v e r t i c a l cliff c l i f f ------------- 40 massive, Total T o t a l Springdale S p r i n g d a l e Sandstone S a n d s t o n e Member --— - 1123 23 Dinosaur D i n o s a u r Canyon Canyon Nember: Member: Sandstone, moderate-red 4. Sandstone, m o d e r a t e - r e d (5P\. (5?v 5/5), 5 / 5 ) , massive massive 4. interbedded with interbedded w i t h fissile f i s s i l e siltstone s i l t s t o n e and and mudstone. Fair m udstone. F a i r to t o ppoor o o r sorting s o r t i n g in i n sandsand­ stones; shales thin and discontinuous; stones; shales thin discontinuous; 1 to t o 88 it f t thick; t h i c k ; sandstones s a n d s t o n e s 2 to t o 12 12 ft f t thick, thick, some~.;rhat lenticular, with somewhat lenticular, w i t h thin t h i n streaks s t r e a k s of of intercalated mudstone. marks intercalated m u d s t o n e . Ripple Ripple m a r k s and ccurrent u r r e n t pparting a r t i n g llineation i n e a t i o n common on nilty silty and and sa.ndy s a n d y bbeds, e d s , Uni U n i t f oorDr,S m s elif c l i f ff ssand and s t e e p slopes s l o p e s -------------------.----------— • .—— steep 94 iSs TriassicT r i a s s i c - Continued Continued Moenave Fo:::mationF o r m a t i o n - Continued Continued Hoenave Dinosaur Canyon MemberMember- Continued D i n o s a u r Canyon Continued 3. 3. 2. 2. Sandstone, m a s s i v e , rresistant, e s i s t a n t , moderate moderate Sandstone, massive, rred e d (5R 5/5), 5 / 5 ) , ppoorly o o r l y sorted, s o r t e d , fine-grained. fine-grained. Contains C o n t a i n s few few bbeds e d s of of ddeep e e p rred e d fissile fissile muds m u d s tone t o n e ------------------------------------ 6 M u d s t o n e , moderate m o d e r a t e reddish-orange r e d d i s h - o r a n g e (10 R 6/6) 6/6) Mudstone, slightly m i c a c e o u s 1>lith w i t h several s e v e r a l 2 iin. n , thick thick slightly micaceous s a n d s t o n e lenses. lenses. S l o p e former f o r m e r ------------ 2 sandstone Slope Total D i n o s a u r Canyon 102 Total Dinosaur Canyon Member -------- 102 T o t a l Moenave o r m a t i o n -------------- 225 Total Moenave FFormation Wingate W i n g a t e Sandstone: Sandstone: 1. Sandstone, 1. S a n d s t o n e , massive, m a s s i v e , moderate m o d e r a t e reddishreddisho r a n g e (lOR (10R 6/6) 6 / 6 ) to t o light-brown light-brown ~"i', :/ orange 6 / 6 ) ; very v e r y fine-grained, f i n e - g r a i n e d , well-sorted, well-sorted, (5YR 6/6); well-rounded; w e l l - r o u n d e d ; no horizontal h o r i z o n t a l bbeds; e d s ; highhigha n g l e cross c r o s s stratification; s t r a t i f i c a t i o n ; no breaks breaks angle i n deposition d e p o s i t i o n vvisible. isible. T h i n chertc h e r t - and and mudmudin Thin ppebble e b b l e congomerate c o n g o m e r a t e at a t bbase. ase. U n i t highly highly Unit jjointed; o i n t e d ; forms f o r m s vertical v e r t i c a l ccliff l i f f __________ ..____ 42 42 T otal W i n g a t e Sandstone S a n d s t o n e --------------42 -42 Total Hingate 5.5.- S h u r t z Gorge Gorge section, section, N W 1/4 1/4 sec. s e c . 20, 2 0 , T. 41 S., S . , R. 1 W. Shurtz NW S e c t i o n measured m e a s u r e d iin n Shurtz S h u r t z Gorge G o r g e along a l o n g Paria P a r i a River. River. Section JJurassic u r a s s i c and and Triassic(?): Triassic(?): Navaj Nav a j 0o Sandstone: Sand s t o n e : Sandstone, 3. S a n d s t o n e , highly h i g h l y cross c r o s s stratified, s t r a t i f i e d , grayishgrayish3. orange pink (lOR 8/2), fine-grained) o r a n g e p i n k (10R 8 / 2 ) , f i n e - g r a i n e d , \.,el1wellsorted well-rounded; s o r t e d and w e l l - r o u n d e d ; cross c r o s s laminations laminations vvery e r y complex. c o m p l e x . Heasurement M e a s u r e m e n t iincomplete, n c o m p l e t e , section section highly Unit h i g h l y faulted f a u l t e d and jjointed. ointed. U n i t forms forms ragged and ppires, and rounded r a g g e d cliffs c l i f f s and i r e s , nipples, n i p p l e s , and rounded .____.759+ bbuu tt tes t e s .• lncomp I n c o m pIe l e tte e __._______________________ . 759+ ?2 . Sandstone, S a n d s t o n e , massive m a s s i v e hhorizontal o r i z o n t a l bbeds e d s with w i t h high high and and 10\1 low angle a n g l e cross-stratific.ation; c r o s s - s t r a t i f i c a t i o n ; vvery e r y pale pale orange o r a n g e (lOYR (10YR 8/2) 8/2) w weathers e a t h e r s grayish-orange grayish-orange (10Y~ Minor (10YR 7/4). 7/4). M i n o r siltstone s i l t s t o n e bbeds e d s present. present. Unit U n i t fine f i n e grc:iined, g r a i n e d , "lell w e l l sorted, s o r t e d , ggrains r a i n s rounded. rounded. Bedding B e d d i n g lless e s s distinct d i s t i n c t uup'.vards; p w a r d s ; fanns f o r m s sheer, sheer, • •• desert ____ .______ d e s e r t --varnished v a r n i s h e d cliffs c l i f f s ———. —._____________ — - 2272 72 ... Navaj 1031+ IInCOll.p1ete ncomplete N a v a j o0 Sands S a n d stone t o n e _____ ._______ 1031+ 159159 JJurassic u r a s s i c and and Triassic(?)T r i a s s i c ( ? ) - Continued Continued Kayenta FormationK ayenta F o r m a t i o n - Continued Continued t~. 10- ..>.-, Kayenta K a y e n t a Fonnation: Formation: 1. S a n d s t o n e , dark d a r k reddish-brown r e d d i s h - b r o w n (10R and 1. Sandstone, (lOR A/3) 4/3) and oorangish-pink r a n g i s h - p i n k (SYR (5YR 7/4) 7 / 4 ) iinterbedded nterbedded w i t h thin with thin d a r k rreddish·-brmm eddish-brown m u d s t o n e . Mudstone M u d s t o n e increases increases dark mudstone. ttowards o w a r d s ttop. op. S a n d s t o n e hhorizontally o r i z o n t a l l y bedded bedded Sandstone iin n m a s s i v e uunits n i t s 2 tto o 10 ft f t tthick; h i c k ; poorly poorly massive ssorted, o r t e d , silty, silty, w i t h abundant a b u n d a n t mud ppebble e b b l e concon­ with g l o m e r a t e s ; hhighly i g h l y cross-laminated. cross-laminated. glomerates; Manyg r a i n ttextures; e x t u r e s ; much hhorizontal o r i z o n t a l variation. variation. grain S i l t s t o n e and and m u d s t o n e vvery e r y ppoorly o o r l y sorted, sorted, Siltstone mudstone tthin h i n bbedded, e d d e d , micaceous. micaceous. F o r m a t i o n forms forms Formation l e d g e s and c l i f f s ---------------------------- 215 ledges and cliffs T otal K ayenta F o r m a t i o n ----------------- 215 Total Kayenta Formation 6.T. 42 S., 6 , ~ Catstairs C a t s t a i r s section, s e c t i o n , S 1/2 1/2 sec. s e c 225, 5 , T, S , , R. 2 W. Section measured Section m e a s u r e d along a l o n g highway. highway. Hiddle Upper Jurassic: M i d d l e and and Upper Jurassic: Cannel C a r m e l Formation: Formation: and siltstone; Red sandstone s a n d s t o n e and s i l t s t o n e ; uruneasured. unmeasured. Middle M i d d l e Jurassic: Jurassic: Navajo N a v a j o Sandstone: Sandstone: Thousand T h o u s a n d Pockets P o c k e t s Tongue: Tongue: Sandstone, (SY 8/1) 44.. S a n d s t o n e , yyellowish-gray e l l o w i s h - g r a y (5Y 8 / 1 ) weathers weathers (lOYR 7/4); mature ggrayish-orange r a y i s h - o r a n g e (10YR 7/4); m a t u r e quartz quartz sandstone, mediu.rn ggrained, well s a n d s t o n e , ffine i n e tto o medium rained, w e l l sorted sorted and o u n d e d ; tthree hree m a s s i v e ccross-laminated r e s s - l a m i n a t e d beds beds and rrounded; massive a r e separated s e p a r a t e d by h i n silt.stone s i l t s t o n e bbeds; e d s ; some are by tthin aassoci.ated s s o c i a t e d cchanneling h a n n e l i n g '.-lith w i t h rrelief e l i e f of ft. of 1 ft. U n i t fforms o r m s rrounded o u n d e d hhogback o g b a c k and e r t i c a l cliff-230 cliff-230 Unit and vvertical T otal T housand P o c k e t s Tongue Total Thousand Pockets Tongue 230 ----------230 a r m e l Formation: Formation: - C Carmel JJudd udd H o l l o w Tongue: Tongue: Hollow 3. S i l t s t o n e and u d s t o n e , same u t "'ith with 3. Siltstone and m mudstone, same aass 1 bbut more e d bbeds e d s -----------------------·-------20 —— • 20 more rred 22.. S a n d s t o n e , yyellowish-g~ay e l l o w i s h - g r a y (5Y / 1 ) , mature mature Sandstone, (SY 88/1)~ massive; ttexture, e x t u r e , cross--larainated, cross-laminated, m a s s i v e ; forms forms hogback _____.___ .______________ .________________ 29 hogback «.—, 29 I' , t.", 1. 1. M u d s t o n e , ffissile i s s i l e tto o m a s s i v e , llight-gray i g h t - g r a y eN7), (N7), Mudstone, massive, ssiltstone~ i l t s t o n e , fissile f i s s i l e tto o tthin-bedded, h i n - b e d d e d , grayish-red grayish-red (10R / 2 ) , and i n e ssandstone; a n d s t o n e ; vvarious a r i o u s colors colors (lOR 55/2), and ffine and l i t h o l o g i e s i n t e r b e d d e d and m o t t l e d to and lithologies interbcclded and mottled to form bbanded, ____________ ._ 50_ 50 form a n d e d , iirregular r r e g u l a r slope slope . 160 160 Middle M i d d l e JurassicJ u r a s s i c - Continued Continued Carmel C a r m e l FormationF o r m a t i o n - Continued Continued Judd J u d d Hollow H o l l o w TongueT o n g u e - Continued Continued T o t a l Judd J u d d Hollmv H o l l o w Tongue ----------------------- 99_ Total 99 7.7 . - Hest West Cove section, s e c t i o n , W 1/2 1/2 sec. s e c . 30 T. 42 s. S. R. 1 W. Cretaceous C r e t a c e o u s System: System: Dakota D a k o t a Formation: Formation: Complex sandstone, s a n d s t o n e , conglomerate, c o n g l o m e r a t e , coal c o a l and mudstone; mudstone; uunmeasured. nmeasured. Note.N o t e . - Dakota-Entrada D a k o t a - E n t r a d a contact c o n t a c t an obvious o b v i o u s unconformity u n c o n f o r m i t y with w i t h numerous numerous channels c h a n n e l s 5 to t o 10 feet f e e t deep. deep. Upper Jurassic: Upper Jurassic: E n t r a d a Sandstone: Sandstone: Entrada Escalante E s c a l a n t e Member: Member: 4. Sandstone, 4. S a n d s t o n e , yyellowish-gray e l l o w i s h - g r a y (SY (5Y 8/1) 8 / 1 ) with with pink p i n k mottling, m o t t l i n g , low-angle l o w - a n g l e cross c r o s s stratifications stratifications i n t e r r u p t e d by by several s e v e r a l ceds b e d s of of red r e d and green green interrupted m o t t l e d siltstone; s i l t s t o n e ; forms f o r m s cliff c l i f f or o r steep, steep, mottled t a l u s - c o v e r e d slope slope 84 talus-covered --------------------84 Total 8/1 T o t a l Escalante E s c a l a n t e Membey Member --.. • --------• 84 Unconfo-;'lnity Unconformity Cannonville C a n n o n v i l l e Hember: Member: 3. .... ') Sandstone, S a n d s t o n e , yellouish-gray y e l l o w i s h - g r a y (5Y 8/1), 8 / 1 ) , friable, friable, Hith medium-scale festoon cross w i t h m e d i u m - s c a l e f e s t o o n c r o s s laminations laminations some of of which w h i c h form form a hash h a s h pattern; p a t t e r n ; fine fine grain~d g r a i n e d with w i t h silt s i l t matrix, m a t r i x , grains g r a i n s sub-round; sub-round; c o n t a i n s few isolated i s o l a t e d red r e d grains. grains. Locally contains Locally present p r e s e n t are a r e red r e d and green g r e e n silt s i l t bbeds e d s 2 ft ft thick. Unit thick. U n i t forms f o r m s rrounded o u n d e d cliffs, c l i f f s , ledges, ledges, and buttes b u t t e s --------·-·------···------------·-----·--156 —— —— • — •—-—156 and S a n d s t o n e , same as a s 1, 1 , bbounded o u n d e d on top t o p and and Sandstone, b o t t o m by fine-graineu, f i n e - g r a i n e d , ppoorly o o r l y sorted, s o r t e d , pale pale bottom r e d d i s h - b r o w n (lOR (10R 5/4) 5 / 4 ) silty s i l t y sandstone; sandstone; reddish-brown f o r m s cliffs c l i f f s and and hoodos h o o d o s ------.-------------— ~ 42 forms Total T o t a l Cannonville C a n n o n v i l l e .Hember Member --------------198 198 Unconformity Unconformity Gunsight G u n s i g h t Butte B u t t e }1ember: Member: 1. Sandstone, 1. S a n d s t o n e , very v e r y pale p a l e orange o r a n g e (10YR 8/4), 8 / 4 ) , crosscrossl a m i n a t e d , fine--grained, f i n e - g r a i n e d , grains g r a i n s vIe11··sorted) well-sorted, lauinated. well·-ro1.lHded; w e l l - r o u n d e d ; contains c o n t a i n s scattered s c a t t e r e d amber and and 161 161 Upper Upper JurassicJ u r a s s i c - Continued Continued E n t r a d a SandstoneS a n d s t o n e - Continued Continued Entraca Gunsight G u n s i g h t Butte B u t t e HemberMember- Continued Continued brown quartz brown q u a r t z grains g r a i n s and concentric concentric iron Unit i r o n stains. stains. U n i t forms f o r m s sheer s h e e r cliff c l i f f -----:...46 -46 Total Butte T o t a l Gunsight Gunsight B u t t e Member ---------:....46 -46 Total T o t a l Entrada E n t r a d a Sandstone S a n d s t o n e ____________- 3328 28 Note.N o t e . - Section S e c t i o n off-set o f f - s e t tto o southeast s o u t h e a s t about a b o u t 1 mile. mile. Middle M i d d l e and and Upper Upper Jurassic: Jurassic: Carmel C a r m e l Formation: Formation: Winsor W i n s o r Member: Member: 14. and mudstone, 1 4 . Sandstone, S a n d s t o n e , siltstone, s i l t s t o n e , and mudstone, complexly c o m p l e x l y interbedded; i n t e r b e d d e d ; sandstone s a n d s t o n e very very pale p a l e orange o r a n g e (lOYR (10YR 8/2), 8 / 2 ) , fine f i n e grained grained with w i t h small s m a l l scale s c a l e cross-laminations; cross-laminations; local and coarse l o c a l flute f l u t e casts c a s t s and c o a r s e channelchanneldeposited Siltstone d e p o s i t e d sand s a n d grains. grains. S i l t s t o n e very very sandy, s a n d y , rresistant; e s i s t a n t ; mudstone m u d s t o n e bentonitic, bentonitic, vvari-colored a r i - c o l o r e d ff0TI11S o r m s "popcorn" " p o p c o r n " surface. surface. Some bbeds e d s iintensly n t e n s l y colored c o l o r e d purple, purple, b r o w n , red, r e d , and and orange. orange. U n i t forms forms brown, Unit bbanded, a n d e d , very v e r y irregular i r r e g u l a r badland b a d l a n d slopes slopes and l e d g e s 204 and ledges ------------------------------ 204 1 3 . Sandstone, S a n d s t o n e , vvery e r y ppale-orange, a l e - o r a n g e , silty, silty, 13. s e m i - r e s i s t a n t ; forms f o r m s kknobby n o b b y ledge ledge semi-resistant; or hogback _______________________________ 55 or hogback . 55 12. 1 2 . Hudstone, M u d s t o n e , bentonitic, b e n t o n i t i c , color c o l o r bbanded a n d e d in in s h a d e s of of rred e d and r o w n ; bedded b e d d e d gypsum; gypsum; shades and bbrown; few intercalated i n t e r c a l a t e d sandstone s a n d s t o n e and siltstone siltstone few bbeds, e d s , forms f o r m s bbadlands a d l a n d s -------------_.--------2...2. . .— —50 Total \-Jillsor Total W i n s o r Member Member __________________ 309 . .309 l.;'hite W h i t e sandstone s a n d s t o n e facies: facies: 11. 1 1 . Sandstone, S a n d s t o n e , same as a s 9 bbut u t with w i t h high h i g h angle angle crQss-strdtification 61 c r o s s - s t r a t i f i c a t i o n ----------------------—— 61 10. 1 0 . Siltstone, S i l t s t o n e , reddish-brcwn r e d d i s h - b r c w n (lOR (1QR 4/5), 4 / 5 ) , ~vavy wavy bbedde.d> e d d e d , sandy s a n d y --------.--.-----.---.-._--------. — 11 9 . Sandstone, S a n d s t o n e , vvery e r y friable, f r i a b l e , massive, m a s s i v e , Hith with 9. h o r i z o n t a l beds b e d s of of low-angle l o w - a n g l e crosscrosshorizontal stratification. S a n d s t o n e is i s highly highly stratification. Sandstone m a t u r e , yye.lJ.owish-gray e l l o w i s h - g r a y (5Y 9/1); 9 / 1 ) ; forms forms matu1."e~ rYOL!nded o u n d e d bb!u tt ttes e s and and hog h o g back b a c k .------------.----' -— 35 3S Total w'hite Total w h i t e sandstone s a n d s t o n e facies f a c i e s -.------...:. 97 162 Middle M i d d l e and Upper Upper JurassicJ u r a s s i c - Continued Continued Ca~el C a r m e l FonnationF o r m a t i o n - Continued Continued Paria P a r i a River.Hember R i v e r Member (Hiddle ( M i d d l e Jurassic) Jurassic) 8. C o n g l o m e r a t i c sandstone, s a n d s t o n e , very v e r y palepaleConglomeratic o r a n g e (IOYR (10YR 8/2) 8 / 2 ) interbedded i n t e r b e d d e d with with orange r e d d i s h - b r o w n (lOR (10R 4/4), 4 / 4 ) , claystone c l a y s t o n e and and reddish-brown ssiltstone. iltstone. S a n d s t o n e c o n t a i n s n u m e rous Sandstone contains numerous q u a r t z i t e p e b b l e s and t r a c e s of b l a c quartzite pebbles and traces of blackk m i c a ; siltstone s i l t s t o n e very v e r y fine f i n e grained. grained, mica; and p o o r l y s o r t e d ; f o r m s b a nded and poorly sorted; forms banded slope ____________________________________ 36 7. S a n d s t o n e , mottled, m o t t l e d , very v e r y ppale a l e orange orange Sandstone, 5 / 4 ) , texture t e x t u r e similar s i m i l a r to t o 4; 4; (5YR 5/4), b e d d i n g complex, c o m p l e x , includes i n c l u d e s flame flame bedding s t r u c t u r e s , load l o a d casts, c a s t s , ripple r i p p l e marks; marks; structures, unit u n i t forms f o r m s rounded r o u n d e d cliffs c l i f f s _________________ — 15 15 Limy sandstone, s a n d s t o n e , yellowish-gray, y e l l o w i s h - g r a y , interinter­ b e d d e d with w i t h reddish-orange r e d d i s h - o r a n g e bentonitic bentonitic bedded claystone. S a n d s t o n e several s e v e r a l inches inches claystone. Sandstone t o 2 ft f t thick, t h i c k , very v e r y fine f i n e grained, g r a i n e d , well well to s o r t e d and rounded; r o u n d e d ; top t o p of of uunit n i t is is sorted m a s s i v e clay c l a y bed b e d with w i t h abundant a b u n d a n t chert chert massive conglomerate. U n i t forms f o r m s 1mV' low hills h i l l s and and conglomerate. Unit lledges e d g e s ------------------------------------17 17 S a n d s t o n e and siltstone, s i l t s t o n e , interbedded; interbedded; Sandstone sandstone s a n d s t o n e is i s yyellowish-gray, e l l o w i s h - g r a y , fine fine grained, g r a i n e d , poor p o o r to t o well w e l l cemented; c e m e n t e d ; beds beds 2 in. i n . to t o I1 ft. f t . thick, t h i c k , locally l o c a l l y contorted; contorted; s i l t - s t o n e is i s poorly p o o r l y sorted, s o r t e d , dark dark silt-stone rreddish-brow~, e d d i s h - b r o w n , contorted c o n t o r t e d with w i t h flame flame s t r u c t u r e s ; abundant abundant m e d i u m - s i z e sand sand st:ructures; medium-size g r a i n s in i n silt silt m a t r i x ; forms f o r m s irregular irregular grains matrix; c l i f ff -------------------------.--------·----12 — 12 clif S a n d s t o n e , massive, m a s s i v e , reddish-brovffi r e d d i s h - b r o w n and and Sandstone, g r a y i s h - y e l l o w , mediu:n-grained, m e d i u m - g r a i n e d , wel1wellgrayish-yellow, sorted; and rounded; s o r t e d ; grains g r a i n s frosted f r o s t e d and rounded; b e d d i n g complex c o m p l e x and v a r i e d ; rain r a i n drop drop bedding and varied; p r i n t s , flmne f l a m e structures, s t r u c t u r e s , contorted contorted prints, bedding. U n i t contains c o n t a i n s interbedded interbedded bedding. Unit d a r k - r e d siltstone; s i l t s t o n e ; reistant, r e i s t a n t , forms forms dark-red hhogback o g b a c k and and dips d i p s llope o p e ------~.----------------54 • —-54 S a n d s t o n e , massive, m a s s i v e , interbedded i n t e r b e d d e d reddishreddishSandstone, brown and yellowish-gray; y e l l o w i s h - g r a y ; sorting s o r t i n g and and bYo\>lIl and g r a i n s i z e v a r i a b l e ; c e m e n t i n g v a r iable, grain size variable; cementing variable, bbedding e d d i n g parallel p a r a l l e l and even; e v e n ; interbedded interbedded b e n t o n i t i c mudstone; m u d s t o n e ; forms f o r m s ledgy, l e d g y , rubblerubblebentonitic covered .______ .___.__ ._________ ·_55 c o v e r e d slope s l o p e ________ •— — • •—55 slope 6. 5. 4. 3. 2. S i l t s t o n e , sandy, s a n d y , arkosic, a r k o s i c , bentonitic, bentonitic, Siltstone, dark d a r k reddish-bro\VD r e d d i s h - b r o w n (lOR (10R l+flf); 4 / 4 ) ; coarse c o a r s e silt silt f i n e sand s a n d bbecoming e c o m i n g finer f i n e r ufHV'ards; u p w a r d s ; some and fine 36 163 !·fiddle M i d d l e JurassicJ u r a s s i c - Continued Continued Carmel C a r m e l FormationF o r m a t i o n - Continued Continued Paria P a r i a River R i v e r HemberMember- Continued Continued 1. 1. fissile f i s s i l e bbedding e d d i n g near n e a r top. t o p . Lower Lower part p a r t of of unit u n i t massive, m a s s i v e , contorted; contorted; f o r m s knobby knobby cliff c l i f f --------------• forms .. ------- 28 Sandstone, S a n d s t o n e , yellowish-gray y e l l o w i s h - g r a y (5Y 8/1), 8/1), rreworked e w o r k e d Thousand T h o u s a n d Pockets P o c k e t s Tongue Tongue -----------.! 1 Total River T o t a l Paria Paria R i v e r Member ----....------ ·218 218 T o t a l Carmel C a r m e l Formation--------------624 Formation -624 Total 8.T.. 4411 S., 8 . - Mouth of of Cottonwood C o t t o n w o o d Canyon Canyon section, s e c t i o n , N 1/2 1/2 sec. s e c . 229, 9, T S., R. 1 H. W. Section S e c t i o n measured m e a s u r e d where w h e r e Paria P a r i a River R i v e r crosses c r o s s e s Dakota Dakota hhogback. ogback. Upper Upper Cretaceous: Cretaceous: Straight S t r a i g h t Cliffs C l i f f s Formation F o r m a t i o n undescribed undescribed Tropic T r o p i c Shale: Shale: 5. Siltstone 5. S i l t s t o n e and and mudstone, m u d s t o n e , medium dark-gray d a r k - g r a y (N4) and light olive-gray (SY 6/2) with and l i g h t o l i v e - g r a y (5Y 6 / 2 ) w i t h thin thin interbeds i n t e r b e d s of of dusky-yellow d u s k y - y e l l o w (5Y 7/4) 7 / 4 ) sandstone. sandstone. S a n d s t o n e increases i n c r e a s e s upwards; u p w a r d s ; numerous n u m e r o u s trails trails Sandstone and burrows b u r r o w s on sandstones; s a n d s t o n e s ; forms f o r m s steep steep and slope s l o p e ss --________________________________._______ 91 91 Claystone mudstone, 4. C l a y s t o n e and m u d s t o n e , dark-gray d a r k - g r a y (N4), (N4), 4. l a m i n a t e d (varved), ( v a r v e d ) , bbentonitic, e n t o n i t i c , becoming becoming laminated yellowish-gray y e l l o w i s h - g r a y about a b o u t halfway h a l f w a y up apparently apparently due to t o fine f i n e pyrite p y r i t e and an a n increase i n c r e a s e in in kkaolinite. aolinite. U n i t covered c o v e r e d by by "popcorn" "popcorn" Unit s u r f a c e ; forms f o r m s rounded r o u n d e d slopes s l o p e s -----------------214 514 surface; '. Total Tropic Shale _______________________ 6_05 Total Tropic Shale ~05 Note.M o t e . - Section S e c t i o n off-set o f f - s e t 1 1/3 1/3 miles m i l e s northeast. northeast. Dakota D a k o t a Formation; Formation; 3. Sandstone, 3. S a n d s t o n e , coal-streaked; c o a l - s t r e a k e d ; very v e r y fossiliferous, fossiliferous, oyster o y s t e r bed; b e d ; hhogback o g b a c k former f o r m e r ______ — . ._______________ 8 8 2. S a n d s t o n e , siltstone, s i l t s t o n e , and mudstone, m u d s t o n e , yellowishyellowish2. Sal1Clstone, o r a n g e (lOYR (10YR 7/6), 7 / 6 ) , complexly c o m p l e x l y beGded bedded w i t h many orange with u n c o n f o r m i t i e s ; small-scale s m a l l - s c a l e cross' c r o s s - laminations, laminations, unconformities; poor p o o r sorting s o r t i n g and rounding; r o u n d i n g ; many textures t e x t u r e s and and ttypes y p e s of of grains; g r a i n s ; much m atrix. Thin, matrix. Thin, d i s c o n t i n u o u s coal c o a l streaks s t r e a k s are a r e present; p r e s e n t ; along along discontinuous strike s t r i k e some sandstones s a n d s t o n e s are a r e bright b r i g h t red r e d apparently apparently t o burned b u r n e d coal; c o a l ; forms f o r m s jjagged a g g e d hogbacks h o g b a c k s -----100 100 due to 164 Upper e r CretaceousC r e t a c e o u s - Continued Continued Dakota D a k o t a FormationF o r m a t i o n - Continued Continued 1. 1. Sandstone, S a n d s t o n e , siltstone, s i l t s t o n e , mudstone m u d s t o n e and and conglomerate, conglomerate, grayish-orange g r a y i s h - o r a n g e (10YR 7/3), 7 / 3 ) , abundant a b u n d a n t crosscrossstratification, s t r a t i f i c a t i o n , moderate-sorting; m o d e r a t e - s o r t i n g ; massive m a s s i v e to to tthin-bedded, h i n - b e d d e d , lenticular l e n t i c u l a r bbeds; e d s ; channels c h a n n e l s up to to 3 feet f e e t of of relief; r e l i e f ; hogback h o g b a c k former f o r m e r --------------'-70 70 T o t a l Dakota D a k o t a Sandstone S a n d s t o n e -------------------178 -178 Total r i g h a m Plains P l a i n s Jeep J e e p Road section, section, 4.- B Brigham NW 1/4 1/4 sec. s e c . 15, 1 5 , T. 41 41 NIol S., S., R. 1 W. Upper e r Cretaceous: Cretaceous: Straight S t r a i g h t Cliffs C l i f f s Formation: Formation: D r i p Tank Member: Drip Tank Member: 7. Sandstone, 7. S a n d s t o n e , coarse-grained, c o a r s e - g r a i n e d , moderate moderate yyellowish-brown e l l o w i s h - b r o w n (lOR (10R 6/4), 6 / 4 ) , crosscrossstratified, with stratified, w i t h numerous n u m e r o u s lenses l e n s e s of of conglomerate c o n g l o m e r a t e with w i t h chert c h e r t pebbles p e b b l e s up to to 1/2 Some beds 1/2 in. i n . in i n diameter. diameter. b e d s contain contain abundant a b u n d a n t iron i r o n oxide o x i d e in i n bbands a n d s and nodules. nodules. Unit U n i t forms f o r m s resistant r e s i s t a n t cliff c l i f f and and hogback; hogback; measured m e a s u r e d and and estimated e s t i m a t e d thickness t h i c k n e s s ---------~380 -380 Total T o t a l Drip D r i p Tank Tank Member ---------------380 380 JJohn o h n Henry H e n r y Hember: Member: 6. Sandstone, 6. S a n d s t o n e , dark d a r k yyellowish-orange e l l o w i s h - o r a n g e (10 ( 1 0 YR 7/6) 7/6) alternating w i t h olive-gray olive-gray m u d s t o n e . MudMud­ alternating with mudstone. sstone t o n e contains c o n t a i n s numerous n u m e r o u s carbonaceous carbonaceous s t r e a k s bbut u t no minable m i n a b l e coal; c o a l ; sandstone s a n d s t o n e is is streaks t o 30 ft f t thick, t h i c k , fine-to f i n e - t o medil~-grained; medium-grained; 2 to l o w - a n g l e ccross-laminations; r o s s - l a m i n a t i o n s ; uppermost uppermost low-angle s a n d s t o n e s conglomeratic c o n g l o m e r a t i c with w i t h sedimentary sedimentary sandstones rrock o c k fragments f r a g m e n t s up tto o 1/4 1/4 in. i n . in i n diameter; diameter; fOTIns ------Slf6 f o r m s alternating a l t e r n a t i n g slopes s l o p e s and cliffs cliffs -• 546 5. Sandstone, 5. S a n d s t o n e , rresistant, e s i s t a n t , coarse--grained c o a r s e - g r a i n e d in in l e n t i c u l a r beds; b e d s ; uunit n i t extremely e x t r e m e l y cross cross lenticular laminated; l a m i n a t e d ; forms f o r m s cliff c l i f f ___________________ ——, -————24 ~~24 Total Nember ____________ T o t a l John J o h n Henry H e n r y Member — — 570 570 H o l l o w Hember: Member: Smokey Hollow Calico 4. C a l i c o sand s a n d bed; b e d ; sandstone, s a n d s t o n e , yellowish-orange yellowish-orange 4. (lOYR (10YR 7/6), 7 / 6 ) , coarse c o a r s e to t o slightly s l i g h t l y conglomeratic; conglomeratic; contains bluish-gray mudstone that c o n t a i n s b l u i s h - g r a y m u d s t o n e t h a t weathers weathers into ___________________ 20 i n t o chips; c h i p s ; cliff c l i f f former former — — 20 165 Upper Upper CretaceousC r e t a c e o u s - Continued Continued Straight S t r a i g h t Cliffs C l i f f s FormationF o r m a t i o n - Continued Continued Sr.lOkey Hember- Continued Smokey Hollmv H o l l o w MemberContinued 3. 3. Sandstone and m mudstone S a n d s t o n e and u d s t o n e ssequence, e q u e n c e , poorly poorly exposed. Sandstones exposed. S a n d s t o n e s 8 to t o 12 ft f t thick, thick, c r o s s - s t r a t i f i e d and c o n t a i n many cross-stratified and contain ttruncations. runcations. Sand coarser c o a r s e r than t h a n 1 oorr 2. 2, Sand M u d s t o n e i s c a r b o n a c e o u s and o l i v e g r a y; Mudstone is carbonaceous and olive-gray; s l o p e former f o r m e r ----------------------------: 197 slope 197 Total Hollm" T o t a l Smokey H o l l o w Member ---------- 2217 17 Tibbet T i b b e t Canyon Canyon Member Sandstone 2. 2, S a n d s t o n e same as a s 1 bbut u t with w i t h abundant abundant ttrough-type r o u g h - t y p e cross c r o s s stratification s t r a t i f i c a t i o n ---------- 58 Sandstone, 1, S a n d s t o n e , dusky d u s k y yyellow e l l o w (SY (5Y 77/4), / 4 ) , with with 1. thin mudstone. Sandstone t h i n interbedded interbedded m udstone. Sandstone i s fine-grained fine-grained w i t h a few few coarser coarser is with l e n s e s ; rripple ipple m a r k e d and ripple lenses; marked and ripple laminated. L o c a l small, s m a l l , 2 iin. n . channels channels laminated. Local Unit becomes m more ppresent. resent. U n i t becomes o r e massive massive and Numerous tracks and sandy s a n d y upwards. upwards. Numerous tracks aud ttrails Unit and r a i l s ppresent. resent. U n i t fonrrs forms cliff c l i f f -------------------------------------- 42 Total Tibbet T otal T i b b e t Canyon Canyon Member Member ---------100 —• 100 Total Cliffs FO~illation----1276 T o t a l Straight Straight C liffs F ormation 1276 REFERENCES CITED A v e r i t t , Paul, P a u l , Detterman, D e t t e r r a a n , J. J . S., S . , Harshbarger, H a r s h b a r g e r , J. J . lV-., W., R e p enning e n n i n g ,, C A., Averitt, Rep C.. A., and Wilson, W i l s o n , R. F., F . , 1955, 1 9 5 5 , Revisions R e v i s i o n s in i n correlation c o r r e l a t i o n and nomenclature n o m e n c l a t u r e of Triassic T r i a s s i c and Jurassic J u r a s s i c formations f o r m a t i o n s iin n southwestern southwestern U t a h and northern n o r t h e r n Arizona: Arizona: Am. Assoc. A s s o c . 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