All-101 61 



1 are used here, and if v;e put b = .005, then (12«a) is correct 

 to 0(10 ), The streamlines and the thermocline, H2 are shown 

 in Figs, 7 and 8, 



In Fig. 8 it can be seen from the contour lines of the 

 thermocline that there is not much deviation of the thermocline 

 from its equilibrium position. In particular, if the initial 

 depth be 500 meters, the thermocline does not fall more than 35 

 meters below its average depth in the southern half of the ocean. 



In checking our results with observation, we find that 

 quantitatively this result is in poor acreoment with field evi- 

 dence. The definition of the thermocline in the real ocean is 

 vague, however, and hence the two parameters 9 (corresponding 

 to the average thickness of the top layer) and b (the density 

 difference) are not clear Ij?- determined. In fact, they may vary 

 over a wide range giving rise to a very considerable variation 

 in the deflection of the thermocline. 



In Fig. 9j the vertical cross section of the ocean at 

 y' = 0,25 is shov/n for four combinations of and b. If we 

 consider the curve with Q == Oo0^92 (Di - Dg = 200 m, ) and 

 b = 0,0025, our result is in good qualitative agreement with 

 measurements of the thermocline off Chesapeake Bay [10], Quan- 

 titatively, the values are out by a factor of (approximately) 

 three. 



Our solution shows a tendency for the thermocline to 

 approach the surface in the northern part of the ocean (Fig, 8)0 

 As a matter of fact, if and b be chosen small enough, the 



