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Denoting the upper and lower layers by subscripts "1" and "2", K. Hutter 30 respectively, the continuity and momentum equations reduce to ClWl v. Yl + Tz = 0, 1 d Vl dt + f ~II Yl + Pl V Pl ClW2 v. Y2 +at: 0, apl az - Pl g , ( 5. 1 ) 0, 1 d Y2 Cit+ f ~ II Y2 + P2 V P2 = 0, Clp2 az = - P2 g . Integrating the pressure equations yields (see ~ig. 2) in which the constants of inte~ration have been chosen such that Pl(z=q)=patm and Pl=P2 at z=-Hl+Q. 2) imply that Vp1 and Vp2 are functions of x and y only~ one may thus deduce from the horizontal momentum equations that Yl and Y2 are independent of z and must obey the equations layer '1' a) b) Shore line Figure 3 Two layer model with upper layer depth Hl and lower layer depth H2.
The mathematical model uses a vertical wall as boundary at the depth contour of H1. The dashed portion in b) is i~nored in the model calculations. 3) + g'v(r;;z-r;;,)+gvc;,=O, where g' = g (PZ- Pl )/pz is the reduced gravity constant for the two layer model. A second set of equations can be deduced by vertically integrating the continuity equations and using the kine~atic boundary conditions*) d/;;1 q(x,y,t), - 3t + 171;; 1 . vl - - wl 0, at z 3c;z + vc; 2 . v1 - wl 3t 0, at z =-H 1 +r;;z(x,y,t).
F·1em. Imp. t·lar. Obs. Kobe, 5, pp. 141-266. , 1959. Turbulence. McGraw Hill, New York. , 1972. Eddy thermal conductivity in the upper 12 m of the tropical Atlantic. J. Phys. , 2, pp. 303-304. , 1971. Die zeitliche Veranderlichkeit der Temperatur der ozeanische~. Deckschicht im Gebiet der grossen meteorbank. Meteor. Forsch. Ergebn. (A), i·lo. 9, S. 42- 51, Berlin-Stuttgart. , 1966. Ekman drift currents in the arctic oceans. , 13, pp. 607-620. , 1983. Theoretical Glaciology. Reidel Publishing Camp.
Alice in Wonderland Coloring Book by Carroll
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