Lakes: Chemistry, Geology, Physics by Robert A. Ragotzkie (auth.), Abraham Lerman (eds.)

By Robert A. Ragotzkie (auth.), Abraham Lerman (eds.)

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8) and (11). It is important to remember that this does not resolve the wall layers: the "surface" velocity calculated in this manner is actually velocity some distance below the surface, and the "bottom" velocity refers to the flow just outside the bottom wall layer. It is emphasized here that the classical zero-velocity (no-slip) bottom boundary condition, coupled with a constant eddy viscosity, gives quite unrealistic results. Transport equations The uncertainties affecting Reynolds stresses provide powerful incentive for avoiding the necessity of quantifying them.

The calculated transport is zero where h = Sib, which is the average depth of the section. The elevation gradient dVdx is the same as would be produced by the wind in a basin of constant depth, equal to the average depth. Along the locus of the average depth the wind stress and pressure gradient are in exact balance and no downwind or upwind flow is produced. In shallower water the wind-stress is greater than the total gravity force gh d ~ I dx due to the surface slope, and the water accelerates downwind.

Curiously, very little attention has been paid in the oceanographic literature so far to the forced solution of Eqs. (17), in contrast to seiches on which there is an overwhelming wealth of information. The only forced solution of Eqs. (17) which has often been quoted is the static setup of a constant depth basin, briefly mentioned above, in which the lake surface is an inclined plane: Fx Fy + gh y, ~ = gh x U = 0 , V = 0 . (18) This solution does not satisfy Eq. (17) for nonuniform depth. For a realistic depth distribution a more complex time-independent elevation distribution ~(x, y) may be found.

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