QoPoCo f

v po5'0

MHT0 = lp0c0

It only remains to find an expression for u^ and a relation between ST,^ and ST0. The following equality is used to estimate u^(CuUf, (5.2.15)

arising from the continuity condition for momentum fluxes at the ocean-atmosphere interface. Here C„ is the resistance coefficient of the sea surface; p is the air density. As for the relationship between 8TW and ST0, the condition <57w = 5T0 is apparently valid in the absence, and STW = (TE — T^ in the presence, of ice in the polar latitudes. This condition, together with (5.2.5) and (5.2.7)—(5.2.15), forms a closed set to determine the climatic characteristics of the atmosphere (T0, ST0, Te, Tp, u, MHTa) and the ocean (STW, ukH, MHT0, Q0, h). For example, for the present-day period, when the Antarctic is covered with ice and the Arctic is almost isolated from the World Ocean, the theory yields the following estimates: T0 = 17 °C, 5T0 = 36 °C, TE = 27 °C, TP = -9 °C, u = 10 m/s, MHTa = 244 W/m2, STW = 27 °C, u= 1.4 cm/s, kH = 1.7 cm2/s, MHT0 = 84 W2/m, Q0 = 126 W/m2, h = 300 m. In general, these are in good agreement with the empirical data.

We turn now to a discussion of general ideas on the construction of deterministic models. We start with the simplest ones in the hierarchy of the model position assigned for the low-parametric models, that is, the models describing the climatic system by means of a small number of parameters.

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