. Compendium of meteorology. Meteorology. tion (increasing cyclonic vorticity in the central upper parts of the cold drop) similar to the vertical circula- tion outlined here. Quite different points of view have been expressed by Rossby [54] in his paper on the meridional movement of sinking cold domes. It seems obvious that the problem of the extreme meandering of the west-wind belt resulting in the formation of cold upper lows must be subjected to further investigations before the nature of the process can be regarded as completely clarified. The meandering of the belt of upper westerlies an
. Compendium of meteorology. Meteorology. tion (increasing cyclonic vorticity in the central upper parts of the cold drop) similar to the vertical circula- tion outlined here. Quite different points of view have been expressed by Rossby [54] in his paper on the meridional movement of sinking cold domes. It seems obvious that the problem of the extreme meandering of the west-wind belt resulting in the formation of cold upper lows must be subjected to further investigations before the nature of the process can be regarded as completely clarified. The meandering of the belt of upper westerlies and the deformation of the upper polar front also result iia an increase of the amplitude of the warm upper ridges. In extreme cases a warm ridge can be completely sepa-. FiG. 15.—Vertical north-south cross section through cen of high-level cyclone of Fig. 14. Heavy line indicates tro] ter yji iii^ii-icvci uvtujiic yjL ±i^. \:a\ \ iiiic liiuiutn^co iiiupO- pause, solid thin lines isentropes (degrees absolute) and dashed lines isotherms (degrees centigrade). Fig. 16.—Vertical west-east cross section through center of high-level cyclone of Fig. 14. Legend as in Fig. 15. rated from its warm source region in the south. The meandering then results in the formation of closed warm upper anticyclones and the belt of strong wester- lies can be re-established south of it. These types of warm upper anticyclones consist mostl}^ of cold polar air masses in the lower layers and therefore appear, in a superficial analysis, as cold polar anticyclones. The true nature of these anticyclones has been elucidated through a number of sjmoptic investigations. The struc- ture of such a warm upper anticyclone has been sub- jected to a detailed analysis by Berggren, Bolin, and Rossby [4]. The case they studied has been used as a model for the upper anticyclone over northern Europe shown in Fig. 4. The pronounced anticyclonic vorticity in these warm upper highs can partly be explained as a r
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