Atmospheric Circulation Systems: Their Structure and by E. Palmén and C.W. Newton (Eds.)

By E. Palmén and C.W. Newton (Eds.)

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Considering also that the winter-summer mean may not represent a true annual average, it is difficult to judge which of the curves in Fig. 6 better represents the real northward flux of energy in the atmosphere.

This is essentially after Mintz, but with consideration of the transport by the Hadley cell in winter. For the flux in summer, the 50 x10 25 40 ':'0 30 :: N SUMMER --------- 20 E o 10 E Cl FIG. 10 Total northward flux of angular momentum in winter and summer in the Northern Hemisphere. Units are 1025 gm ern- sec". Based upon geostrophic eddy fluxes computed by Mintz (1955) at latitudes 20° to 75°N, with flux by Hadley circulation added for winter. relatively weak Hadley cell of the Northern Hemisphere is neglected, and because of lack of data close to the Equator, the curve is not extended to the equatorial region of the Southern Hemisphere Hadley cell (cf.

1/ " I I FIG. 13 Profiles of the 200-mb mean zonal wind between the Equator and 300N in winter, compared to the profile corresponding to constant angular momentum. 5°N. ) o From Fig. 3 we can compute that at the 200-mb level, a time of about 15 days would be required for an air parcel to move from SON to 25°N in the mean circulation, or. about 30 days to move from the Equator to 30oN. The corresponding mean air trajectory is shown in Fig. 12. During the same times, the eastward displacement of the air would be 21,000 and 52,000 km, respectively.

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