For two fictitious "stations" at 42.5°S and 47.5°S, respect- 

 ively, the following vertical distribution of 



'0 r ^0 



I = 



-D 



\L 



( O- - O". )dz 



dz 



'B 



A — T = 



A<r t . A z Z( Aa " t • A z ) 



TAz 



0.64 

 0.40 



0.33 

 0.34 



0.33 

 0.375 

 0.300 

 0.225 



0.137 

 0.100 



0.025 



x 10^ 





 0.64 

 1.04 

 1.37 

 1.71 

 2.04 



2.415 



2.715 

 2.940 



3.077 

 3.177 

 3.202 



x 10^" 



0.32 



0.84 



1.205 



1.54 



1.875 



2.228 



2.565 

 2.828 



3.085 



x 10 



8 



3.127 15.64 

 3.189 15.95 



With r x = 3.25 dyne/cm 2 , and a = 1.9< 

 .8 



sina 



x 10 





 0.64 

 2.32 



4.73 

 7.81 



11.56 

 17.13 

 23.55 

 30.63 

 38.33 

 53.97 

 69.92 



5.65 x 10 7 = 



0.64 



1.68 



2.410 



3.08 



3.75 



5.57 



6.42 

 7.08 

 7.70 



8 



53 x 10 u , 



therefore D = 2500 m for the zonal component. This compares fairly 

 well with the depth of the layer of no motion as shown in figure 2. 

 Similar computations for higher latitudes (55°S) lead to values 

 which are a little too large, whereas the depth D computed for the 



30 



