Atmosphere-Ocean Dynamics - download pdf or read online

By Adrian E. Gill

During this paintings, Dr. Gill appears to be like on the examine of oceanic and atmospheric circulations. He explains how atmospheric and oceanic circulations are eventually pushed via solar power, and covers the learn of saw distributions of actual amounts, together with temperature.

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Intuitively, one might expect the nonuniform heating of the atmosphere to cause rising motion in the tropics and descending motion at higher latitudes. 3). A similar circulation might be expected to occur in the ocean, so that the excess heat received in the tropics would be transported poleward in both atmosphere and ocean. The circulation (in the meridional plane) that actually occurs is known quantitatively (but with limited accuracy) for the atmosphere from observations and is shown in Fig.

1811. balances for this and other special regions are given by Bunker (1976). From such a map, heat fluxes across different sections can be computed by integrating southward from the northern extremity of the map. The poleward flux at 24"N is about 1 PW (1 petawatt = watts) and this compares well with calculations from oceanographic data across this section by Bryden and Hall (1980). Integrals over the ocean basins yield some surprises (Hastenrath, 1980; Stommel, 1980), e g , the heat flux in the Atlantic appears to be northward at all latitudes.

The inverse law holds only sufficiently close to the ground where the shear is strong because other effects become important when the shear gets weak. 5) is large enough to produce convection, turbulence due to convection will become more important than turbulence due to shear at somv level. 4 Dependence on Air-Sea Velocity, Temperature, and Humidity Differences fa) fbl Fig. 4. An example of how the wind speed (in m s-'1 varies with height (in m). The height scale is (a) linear and (b) logarithmic.

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