where Ta is the air temperature, Ts is the ocean model generated surface temperature, qa is the specific humidity, qs is the saturation humidity, cp is the specific heat of air, Lw is the latent heat of evaporation, and CH and CL are the stability dependent sensible andlatent heat transfer coefficients. The soalr insolaion is not only a a function of season and latitude, but also is strongly dependent on latitudinally specified cloud cover. The long wave radiation Ql is a function of Ta, Ts and latitudinally specified cloud cover. These values are calculated in the manner described by Oberhuber [1990]. The interior heat fluxes, Qk, is calculated by exponentially decaying function with a constant decaying coefficient in the global ocean.
Wright [1988] prepared data on a 2 degree by 2 degree, which is sufficiently fine for forcing an OGCM. The climatology covers the years 1950-79. From this data Oberhuber [1988] derived all fluxes required for forcing the ocean model such as heat, buoyancy, fresh water, and turbulent kinetic energy. The flux of momentium is taken from the surface wind stress from ECMWF analysis on a 2.5 degree by 2.5 degree grid. Since ECMWF data are useless for forcing an ocean model at low latitudes (too weak winds) this data set has been blended withthe monthly mean surface wind stress from Herman and Rosenstein as pseudo wind stress.
3. Numerical result
The first experiment with this isopycnal global ocean general circulation model represents an attempt to describe the climatological seasonal cycle of the Pacific, the Indian and the Atlantic Oceans in terms of extream summer and winter conditions after forcing the model by atmospheric flux of climatology. Figure 2 shows that the layer kinetic energy for the first four years (48 months from the initial rest state) and the last two years (from month 1560 to month 1584). It is noted that the mixed layer kinetic energy decrease rapidly in the begining of integration because the kinetic energy associated with the imposed initial temperature-salinity structure did not baluce with the no motion condition (the water rest in the begining.) After adjustment period the ocean approaches a cyclo-stationary state from the surface layer to the eighth layer, except for the deep ocean (from the 9th layer to the 13th layer) where temperature and salinity have not become stationary so that the layer enery exhibits interannual variation.
3a. Seasonal variation of temperature
Figures 3 and 4 shows the observed and calculated temperature anomalies at
