By Michael V.Kurgansky

This e-book offers with the most ideas of large-scale atmospheric dynamics at the foundation of adiabatic movement constants. it may be regarded as an advent to the speculation of quasi two-dimensional fluid movement concentrating totally on approximately horizontal fluid parcel displacements in a stably stratified compressible fluid. a radical mathematical therapy of the governing equations is coupled with a transparent interpretation of the phenomena studied and observed through examples of actual meteorological info research. subject matters comprise an entire set of compressible fluid dynamic equations besides a survey on fluid dynamical conservation legislation utilized in meteorology and atmospheric physics; the derivation of two-dimensional atmospheric versions; large-scale flows; isentropic research of large-scale atmospheric procedures; and the foundations of kinetic strength sinks and their relation to the strength stability within the surroundings.

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**Example text**

It means that when к =f(m), к* =f (m+1). For instance, if к=5/3, к*=7/5 and if к=7/5, к*=9/7, and so on. We conclude that the three-dimensional quasi-static dynamics of an m-atomic gaseous atmosphere is reduced to the two-dimensional dynamics of an m+1atomic gaseous atmosphere. Suppose additionally that the gas molecular weight µ and the gas constant R are the constants of the transformation in question: R=R*. In this case, the specific heat capacity at constant pressure transforms according to the rule: c=Rк/(к−1)→cp*=R*к*/(к*−1)=R(2к−1)/(к—1).

Damp the westerlies. Secondly, the variations of atmospheric angular momentum are caused by the surface friction torque. Let us introduce a tensor of frictional stresses Tik (i, k=1, 2, 3) such that Fi=∂Tik/∂xk, by definition. KURGANSKY (4) where the unit vector n is orthogonal to the Earth’s surface and is oriented downward, beneath the ground. It is assumed that frictional stresses vanish at the top of the atmosphere. The second integral in the right-hand side of Equation (4) can be approximately taken at z=0 and is used in the form −∫∫Tλdσ, where Tλ is the zonal component of frictional stresses on the Earth’s surface.

We need only one of the three resulting equations. , it does not enter the spherical metrics (1′) explicitly and the gravitational potential does not depend on longitude, either. Consequently We arrived at the equation for the axial component of the angular momentum vector. Representing the atmosphere by a thin fluid film of a thickness much less than the Earth’s radius a and introducing a zonal LARGE-SCALE ATMOSPHERIC DYNAMICS 41 component of velocity uλ=asinυλ, we obtain the equation for the axial component of the angular momentum in Eulerian variables We integrate the resulting equation over the entire atmospheric volume (3) where dτ=a2sinυdυdλdz and z=r−a.