A Short Course in Cloud Physics - download pdf or read online

February 2, 2018 | Weather | By admin | 0 Comments

By M.K. Yau, R R Rogers

ISBN-10: 0750632151

ISBN-13: 9780750632157

Covers crucial elements of cloud and precipitation physics and has been widely rewritten with over 60 new illustrations and plenty of new and recent references. Many present issues are lined equivalent to mesoscale meteorology, radar cloud stories and numerical cloud modelling, and themes from the second one variation, resembling serious storms, precipitation tactics and big scale facets of cloud physics, were revised. difficulties are incorporated as examples and to complement the text.

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Additional resources for A Short Course in Cloud Physics

Example text

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. L FIG. 2. Illustration of convective condensation level. 48 A Short Course in Cloud Physics Eventually the surface temperature reaches T2 and the total heat added by convection is proportional to the hatched area ABC. Meanwhile the mixing ratio has become approximately constant up to the altitude of point C and equal to the average in the layer.

Hence the net buoyant force (upward) is Vg(e' - e). Therefore, the buoyant force per unit mass is FB g( e' ; e) g( T;, T'). 9) If this is the only force acting on a parcel, its equation of motion is ddt2z = F 2 B =g (T -T' T') . 10) As expected, this force is positive when the parcel is warmer than ambient air, negative when the parcel is cooler than ambient. 9) may be generalized by merely replacing the temperatures with virtual temperatures. Stability criteria for dry air One of the uses of the dry adiabatic lapse rate is in assessing the stability of atmospheric layers with respect to the vertical displacement of a parcel.

At height ~z above the initial position of the parcel, the ambient temperature is T - y~z. The excess temperature of parcel over ambient air is therefore ~z(y - f). 9), is accelerated upwards. Consequently the air is unstable whenever y - r > O. Conversely the parcel is subjected to a restoring force (downward) whenever y - I' < O. For the special case y = I', the displaced parcel experiences zero buoyancy force. The stability criteria for dry air may thus be summarized yr UNSTABLE These criteria may alternatively be expressed in terms of potential temperature.

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


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