. Compendium of meteorology. Meteorology. UJ Q O H 160 200 240 280 320 360 TEMPERATURE (°K) 400 Fig. 4,—Comparison of measured upper-atmosphere temp- eratures (Helgoland blast), V-2 rocket results, and tentative standards (taken from [5] Cox: Amer. J. Phys., 16: 473 (1948), by permission of the publishens). Rough rocket data appearing on Cox's published figure have been replaced by an average curve of temperatures calcuhited from Naval Research Laboratory rocket flights. The lower values are more in keeping with Cox's results and those obtained from rockets. Ozone Heating in the Upper
. Compendium of meteorology. Meteorology. UJ Q O H 160 200 240 280 320 360 TEMPERATURE (°K) 400 Fig. 4,—Comparison of measured upper-atmosphere temp- eratures (Helgoland blast), V-2 rocket results, and tentative standards (taken from [5] Cox: Amer. J. Phys., 16: 473 (1948), by permission of the publishens). Rough rocket data appearing on Cox's published figure have been replaced by an average curve of temperatures calcuhited from Naval Research Laboratory rocket flights. The lower values are more in keeping with Cox's results and those obtained from rockets. Ozone Heating in the Upper Atmosphere The high-temperatiu'e region deduced from sound- propagation experiments coincides with the upper por- tion of the ozonosphere, which lies between 15 and 55 km. The total amount of ozone in the atmosphere is at most a few millimeters at standard conditions. Never- theless ozone absorption in the ultraviolet is strong, and the ozone content appears to be sufficient to account for observed atmospheric heating immediately above the stratosphere. Gowan [7] and Penndorf [15] have made extensive calculations to show how much heating can be expected from atmospheric ozone. Gowan assumes the ozono- sphere to be essentially nonconvective and in radiative. 500 200 300 400 TEMPERATURE(°K) Fig. 5.—Atmospheric temperatures based on calculations of ultraviolet al)sorption in the ozonosphere (taken from [7] Gowan:Ptoc. roy. Soc, (A) 190: 223 (1947), by permission of The Royal Society). equilibrium. The ^-alidity of these assumptions, how- ever, is open to question. Water vapor, ozone, and carbon dioxide are taken to be the principal gases in- volved, and the calculations are made for a number of different himiidities. The assumed solar temperature is 6000K. Ozone content is taken from experiments of Gotz, Meetham, and Dobson and applies to the atmos- phere above Switzerland. A temperature-distribution cur\'e is obtained by dividing the ozonosphere into nine layers and calcul
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