. Aerographer's Mate 3 & 2. United States. Navy; Meteorology; Oceanography. Chapter 11 —WATCH ROUTINES (CONTINUED) weight of the atmosphere depends upon the density. Cold air is denser than warm air. Therefore, cold air must exert more pressure at a given altitude. Assume that two columns of air are exerting the same pressure at the surface; the column containing the warmer air has to extend to a greater altitude to exert a pressure at the surface equal to that exerted by a column of colder and denser air. Since the height of the colder column is lass, it follows that the pressure must dec
. Aerographer's Mate 3 & 2. United States. Navy; Meteorology; Oceanography. Chapter 11 —WATCH ROUTINES (CONTINUED) weight of the atmosphere depends upon the density. Cold air is denser than warm air. Therefore, cold air must exert more pressure at a given altitude. Assume that two columns of air are exerting the same pressure at the surface; the column containing the warmer air has to extend to a greater altitude to exert a pressure at the surface equal to that exerted by a column of colder and denser air. Since the height of the colder column is lass, it follows that the pressure must decrease more rapidly with altitude in the colder air, and the vertical spacing of isobars is closer together. For this reason, a pressure system on the surface does not necessarily exist aloft. On the other hand, under the proper temperature conditions, a pres- sure system may intensify with height. High- and low-pressure systems are classi- fied as either cold core or warm core systems. COLD CORE HIGH. —A cold core high is one in which the temperatures on a horizontal level decrease toward the center. Because the temperature in the center of a cold core high is less than toward the out- side of the system, it follows that the vertical spacing of isobars in the center of this system is closer together than on the outside. Although the pressure at the center of these systems on the surface may be high, the pressure de- creases rapidly with height. (See fig. 11-16.) (For the purpose of illustration, figures 11-16 through 11-19 are exaggerated from the way that they appear in actual atmospheric condi- tions.) Examples of cold core highs are the North American High and the Siberian High. WARM CORE HIGH. —A warm core high is one in which the temperatures on a horizontal level increase toward the center. Because the temperatures in the center of a warm core high are higher than on the outside of the system it follows that the vertical spacing of isobars in the center is farther a
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