. Compendium of meteorology. Meteorology. Fig. 11.—Schematic profiles (normal to the slope) of the wind speed w and temperature &'. (After Prandtl [62].) I have checked the correctness of these theoretical results by a detailed comparison with actually meas- ured average values of ^' and w and have found a splendid agreement, except for the disturbing gradient influences in the upper layers. Furthermore, it is note- worthy that the resulting values of the austausch due to impulse transport (virtual friction) and of that due to transport of the heat content (virtual heat conduc- tion) are o
. Compendium of meteorology. Meteorology. Fig. 11.—Schematic profiles (normal to the slope) of the wind speed w and temperature &'. (After Prandtl [62].) I have checked the correctness of these theoretical results by a detailed comparison with actually meas- ured average values of ^' and w and have found a splendid agreement, except for the disturbing gradient influences in the upper layers. Furthermore, it is note- worthy that the resulting values of the austausch due to impulse transport (virtual friction) and of that due to transport of the heat content (virtual heat conduc- tion) are of a plausible magnitude. Figure 12 presents the theoretical distribution of the potential temperature during upslope and downslope winds, respectively, for which no observations are available. The characteristics of the stratification become very apparent. 200. -I Fig. 12.—Theoretical distribution of the potential tempera- ture Over a mountain slope during (a) upslope wind and (6) downslope wind. {After F. Defant [11].) The theory can be extended to include the oscillatory nature of the slope wind by simply multiplying, as a first approximation, the solutions (10) of the stationary case by the factor cos Oi. Because of the fourth root in the expression for I, variations in the values of ;' and K [17, pp. 441-444] are of little influence on the solution. The average air transport by the slope winds can be roughly computed from the calculated and the observed average profiles of the slope wind. We can then estimate how long it would take until the rising heated slope air has replaced the air masses over the valley bottom. The interest of this question becomes apparent if we consider that this process of warming the air in the valley center has an effect on the pressure gradient and thus on the generation of the mountain and valley winds. Calculations show that a slab of air 1 m thick, 1500 m long (the width of the valley), and 1750 m. Please note that these images are ex
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