By M.K. Yau, R R Rogers

ISBN-10: 0750632151

ISBN-13: 9780750632157

Covers crucial components of cloud and precipitation physics and has been commonly rewritten with over 60 new illustrations and lots of new and recent references. Many present issues are coated corresponding to mesoscale meteorology, radar cloud stories and numerical cloud modelling, and issues from the second one version, equivalent to serious storms, precipitation strategies and massive scale elements of cloud physics, were revised. difficulties are incorporated as examples and to complement the text.

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Sample text

Continued expansion of the air sample of Fig. 2 beyond point P, the isentropic condensation point. The dashed line is the pseudoadiabat through P. This diagram indicates the graphical determination of some of the important theoretical temperatures that characterize an air sample. Water Vapor 23 Some additional special temperatures that may be defined by referring to this illustration are: (a) Adiabatic wet-bulb temperature Tsw , obtained by following the pseudoadiabat from P down to the original pressure.

If strong heating at the surface continues, this heat will be convected upwards, raising the potential temperature of the air throughout the layer. This process is indicated schematically in Fig. 2. The heavy line indicates the initial temperature profile, with To the surface temperature. Heating raises this temperature causing a superadiabatic lapse rate temporarily and convection then tends to establish a dry adiabatic lapse rate with surface temperature T 1 • Additional heating raises the temperature and increases the thickness of the mixing layer.

9w]. 2w]. 27) may often be neglected. Ways of reaching saturation A sample of moist air may undergo several processes that lead to saturation. Some of these processes are of theoretical importance, and introduce certain new temperatures that reflect the moisture content of the air. (a) Dew point temperature Td , defined as the temperature to which moist air must be cooled, with p and w held constant, for it to reach saturation with respect to water. ) Clearly the saturation mixing ratio at the dew point equals the mixing ratio of the moist air: w = ws(p, Td ) .

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A Short Course in Cloud Physics by M.K. Yau, R R Rogers

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