A turbulence closure model for atmospheric boundary layers is examined, under the assumption that the turbulent flow is steady in its ensemble average and the advection and diffusion terms in the turbulent Reynolds stress and heat flux equations are neglected. The constants which are introduced in order to obtain a closure system are determined referring the experimental results obtained in the wind tunnel. The validity of the closure model thus obtained is checked referring the observational results obtained in the constant-flux layer. In order to apply our model to the planetary boundary layer, simple forms for the eddy transport coefficients of momentum and heat are formulated.In this case the parametarization of the scale-length l=l(z) (z: heihgt) which is introduced in estimating the dissipation rate of turbulent kinetic energy with height is discussed in order to satisfy the observational result.
The stability of medium scale disturbances is discussed in connection with the Rossby and Richardson numbers. In case where the Richardson number is of the order of magnitude unity, we may find the unstable disturbances whose wave lengths are about 1,000km-2,000km in middle latitudes.Numerical experiments are also performed in order to simulate the rapid cyclogenesis of medium scale disturbances, which is frequently observed in the lower atmosphere near the southern part of the jet stream over Japan throughout all seasons except summer.
The standing waves responding to forcing by the Hemispheric topography are investigated by means of a quasi-geostrophic, steady state, 34-level model, with Rayleigh friction,
The northward transport of sensible heat in the baroclinic atmosphere is examined in relation with the non-adiabatic heating such as the heat supply into the atmosphere from in case of adiabatic motion, is improved considerably.
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