東亞地區中國長江流域的降雨與其南北兩側降雨相位相反是非常普通的現象，在從年際或年代際的變化都可見到，而本研究探討的重點是針對全球暖化變得較為明顯後1970年代後期西北太平洋及東亞地區降雨的變化。自1979年之後，在西北太平洋及東亞地區的降雨變化南北呈現〝正-負〞（dipole）變化趨勢：80°E至145°E、10°N 至25°N（包含華南地區、中南半島、菲律賓海、南海、孟加拉灣）降雨趨勢增加；100°E至120°E 、28°N至33°N（華中地區）降雨趨勢減少。

從中高對流層溫度顯示在20°N至30°N、90°E至120°E溫度有明顯降低的趨勢，而在低緯度地區溫度有增加的趨勢，不管是北邊溫度降低或南邊溫度增加，任一個因素單獨的變化都能夠造成南北溫度梯度減弱進而使得夏季季風環流減弱造成降雨呈現〝正-負〞的變化趨勢，且除了造成南北溫度梯度減弱外，也能夠引發局部Hadley cell的改變造成〝正-負〞的降雨變化。

青康藏高原冬、春季雪覆蓋面積的增加造成夏季太陽雪融後土壤濕度的增加，太陽加熱的能量被土壤水吸收作為蒸發使用，並未直接加熱地表，所以地表溫度在夏季的變化趨勢是降低的，而青康藏高原平均高度為4000公尺以上，在高層西風的吹拂下將青康藏高原地表的較冷的溫度傳至東亞地區20°N至30°N附近。青康藏高原冬、春季雪覆蓋面積的增加可能是20°N至30°N中高對流層溫度減低的原因。

低緯度地區中高對流層溫度的增加可來自降雨增加時潛熱釋放會加熱整個對流層所致。在低緯地區海表溫度的增加使得能量藉由可感熱與蒸發傳至大氣，而當大氣能量增加時會產生上升運動，造成水氣在10°N 至25°N附近的輻合增加，使得降雨增加。

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