SECT. 2] 



LARGE-SCALE INTERACTIONS 



131 



ones, as does our increased knowledge of rainfall dynamics. Since it is now 

 knoMii that, even in the tropics, all significant rainfall occurs in major 

 synoptic-scale storms, it is likely that the "coast effect" on precipitation has 

 been considerably overrated in the past. 



100° 120° 140° 160° 180° 160° 140° 120° 100° 80° 60° 40° 20° 0° 20° 40° 60° 80° 100° 



100° 120° 140° 160° 180° 160° 140° 120° 100° 80° 60° 40° 20° 0° 20° 40° 60° 80° 100° 



Mean Annual Precipitation (mm) 



Fig. 14. Mean annual distribution of precipitation over the oceans in mm per year. (After 

 Drozdov, 1953.) 



c. The climatology of mean annual energy transactions 



Upon global ^ integration to obtain precipitation as a function of latitude, 

 multiplication by L, and subtraction from Qe, we arrive at the term L{E — P) 

 in (25). Its latitudinal dependence as used by Budyko is shown by the solid 

 curve in Fig. 13. Qvo is entered from Table VI (dotted curve) and Qva is com- 

 puted as residual from (25) and entered as the dot-dashed curve. We are now 

 prepared to place a quantitative foundation under the discussion of the whole 



1 Actually all computations entering. Fig. 13 were done for the whole earth and not just 

 the ocean areas to which our presentation has been restricted. This means, for example, 

 that evaporation and precipitation figures for land areas had also to be included and the 

 term Q^^o ^ Table VI corrected for the ratio of ocean to whole earth's area in each latitude 

 belt before inclusion in the graph. 



