somewhat different in strength at each level. For example, upwelling may 

 he more intense at the surface than at 400 feet or vice versa. Forces 

 tending to modify anomalies of the same origin may also he of different 

 intensity. For example, originally negative anomalies at both levels will 

 be modified by heating in summer at different rates. Consequently, anom- 

 alies cannot be expected to be of the same magnitude at both levels even 

 if they are correlated; differences will usually exist, and coinciding 

 magnitudes will only be accidental. 



Owing to sparsity of data at individual ocean weather stations or 

 lack of data for certain months, analysis of individual anomaly ratios 

 is difficult. A workable distribution which covers at least all months 

 can be achieved only by combining the data for all 5 Atlantic stations. 

 These data are shown in the last columns of table 5' After grouping of 

 positive and negative anomalies, mean values at each level were computed 

 for individual months. The ratio of each pair of mean anomalies was 

 then computed for each month. The monthly ratio distribution was time 

 smoothed by the normal smoothing function. The smoothed ratios for 

 negative and positive anomalies are plotted against time in figure 8. 

 Although the annual range of ratio variations for positive anomalies 

 is somewhat larger than that for negative anomalies, both curves show 



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FIGURE 8 MEAN RATIOS OF MONTHLY MEAN TEMPERATURE ANOMALIES (400 FT/SURFACE) 



