| OCR Text |
Show o r G = K n + l T + h n Xdi( KrKi+ 1) i= l n Xdi( KrKi+ 1) i= l ( 2.5) where d{ is the height to the it n layer, K{ is hydraulic conductivity of the Kth layer and n+ 1 is the number of layers. Layer n+ 1 n W dn+ l Kn+ 1 Kn K2 d2 d n ' K l d. T L^ yz^//////////^^^ stated as: Figure 2.1 Stratified Aquifer System The continuity equation for steady state flow in a stratified aquifer may then be V2G + Q( 5( x - x*), ( y - y*)) - R = 0 ( 2.6) This is linear in the dependent variable G, and the principle of linear superposition is applicable. Halek and Svec ( 1979) also provide an approximate linearization of the partial differential equation for transient groundwater flow, using the Girinski potential. This is stated as: V2G + Q( 5( x - x*), ( y - y*)) - R( x, y) = - 1 3G a 3t ( 2.7) where n a = VlVX^ i- Ki+ l) i= l ( 2.8) ' n+ 1 where & n+ i is the active porosity of the n+ lth layer and hs is a pre- assigned ( expected) value for h. 13 |
