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Show 292 and its spring habit of russet, soft grays, and emerald, together with a sky inimitable and as varied as the seasons, are as fertile in promise aa sufficient in contrasts. The caftan has a general westerly direction, and is some eight miles in length. About midway, a chain of lofty granitic escarpments borders the north side of the stream, along which they extend nearly a mile in truly Gothic grandeur. The lower mass occupies an angle in the canon, and viewed from below it may be imagined to bear striking resemblance to a cathedral- pile. The upper cliffs form a sort of amphitheater extending several hundred yards along the stream, and whose pierced and pinnacled heights rise 500 or 600 feet above the water in a sheer precipice, the face of which is vertically ribbed by the tendency of the rock to assume a columnar structure; however, in places it is solid, clustering in monumental groups in the steep declivities, or towering like castellated ruins in some promontory overlooking the gorge. Toward the upper end of the cliffs, a huge bowlder- like mass of dark-green stone protrudes like an enormous excrescence from their base, and which continues along the north side of the stream about one- fourth of a mile. It then loses its distinctive character, and thence appears like trap of various shades of dark brown and green, which may be traced two or three miles up the cation. This gigantic dike is traversed at various angles by fractures, which have been filled with various mineral substances, as black trap, quartz, & c. This portion of the caiion is frequently bordered by immense inclines, descending from heights of a thousand feet or more, and composed of the angular debris resulting from the atmospheric degradation of igneous ledges seated high up in the mountain- sides. These talus- slopes are sometimes quite destitute of vegetation, though generally sparsely grassed over and covered with pines, spruce, and cedar. The latter, with a sparser representation of the pinon at this elevation ( 8,000 feet), generally prevails in northern declivities, the pine and spruce occupying the opposite and more exposed slopes. Even here the dwarf- oak is met with; but the prevalence of the quaking- asp, which forms thickets beside the stream and high up in the adjacent mountains, plainly indicates the altitude, as also does the occurrence of dense tracts of spruce. Just before reaching Macelroy Creek, by which an old trail gains the Moreno Valley, a ledge of red feldspathic granite outcrops in the north side of the caiion, and a short distance above detached masses of gray syenitic rock were observed. A few hundred yards above Macelroy Creek, and perhaps a mile and a quarter from the upper entrance of the cafion, in a high ridge, round which the stream makes a sharp curve, a reddish contorto- laminated gneiss occurs, and which also appears in the little valley of Macelroy Creek. This rock continues thence nearly to the Moreno Valley, apparently constituting an immense thickness, perhaps interbedded with micaceous schists, and succeeded on the west by a very hard red quartzose rock. These deposits appear to constitute the high hills along the east border of the Moreno Valley ( at least in the neighborhood of the entrance of the Cimarron Caiion), and may possibly also be found in Little Baldy. Similar rocks are said to occur in the summit of Great Baldy, although none such were observed in the saddle over which the Blackhorse trail passes. The Moreno Valley extends in a north- south direction nearly eighteen miles, with an average width of two miles. It properly does not belong to the system of shallow park- basins which were excavated out of the Cretaceous and Tertiary formations, and to whichUte Valley belongs? but it rather pertains to the possibly older lake- basins, environed by the |