By G T Csanady,NetLibrary, Inc.
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Extra resources for Air-sea interaction: laws and mechanisms
This can only be true The Transfer Laws of the Air-Sea Interface 44 of an irreversible process like heat flux if the flux vanishes, too. The Reynolds flux of heat therefore vanishes in an atmosphere of constant potential temperature. Texts in meteorology explain that a parcel of air moved adiabatically up or down in such an atmosphere changes its temperature owing to expansion or compression just so as to remain at the temperature of its environment. There is then no mechanism for producing temperature fluctuations, and there can be no Reynolds flux of heat.
Therefore, it also affects the temperature and humidity distributions, just as it influences the velocity distribution. In dimensional argument, the Obukhov length L conventionally represents interface buoyancy flux. 62) with φt , and φq functions to be determined by observation. A number of different empirical formulations for these functions have appeared in the literature. By general agreement they are the same for temperature and humidity, φt = φq . In the stable case, with buoyancy negative, Obukhov length positive, the simple consensus formula, φt (z/L) = 1 + βz/L, applies, the same as the correction for the velocity gradient, although with some variation in the value of the constant β.
Another point is that, as the language of meteorological forecasts teaches us, light winds are also variable, so that U + u may even vary between positive and negative values. The mean wind stress then falls between extremes of the product ρ|U + u |(U + u )C D , at √ u 2 it could be much higher. a higher value than ρU 2 C D . For U Even more puzzling than the high drag coefficients at low wind speeds, are some very low ones, found by Sheppard et al. (1972) and Portman (1960), over inland lakes in light winds.
Air-sea interaction: laws and mechanisms by G T Csanady,NetLibrary, Inc.