dy \ D dy / r dy I D i ' 



dy V D dy / r dy 



By integration, it follows that 



U = dy^ = -^ + C * D » (40) 



where C is a constant, which becomes zero if U = for T^ = 0. 

 This result shows that the zonal mass transport, U, is proportional 

 to the zonal component of the wind stress, T . This is different 

 from Monk's general result where in a confined ocean of constant 

 depth it was found that the horizontal mass transport of permanent 

 ocean currents depends only on the rotational component of the wind 

 stress field over the ocean. Of course, in an ocean bounded by con- 

 tinents, the assumptions which led to (40) are in general not justi- 

 fied any longer. Even in the case where T may be assumed to be 

 zero, dD/dx is not necessarily zero, and V ^ 0, at least for some 

 distance along the boundaries. The whole system of horizontal mass 

 transport will be modified by the boundary conditions, but besides 

 a dependence of the mass transport on the curl of T , there will 

 also be a dependence on T . 



Equation (40), however, will hold approximately, in the central 

 parts of the oceans, far away from the boundaries. Probably, it 

 can best be applied to the Antarctic Circum Polar Current, Just where 

 W. Munk and E. Palmen (195D found discrepancies with the results 

 of Munk's theory. 



In the Antarctic Circum Polar Current between 65°S and 45°S, 

 according to table 1, T^ « 2.0 dyne/cm 2 , and r s 3.34 x 10" 6 sec" 1 

 (see page 30). Thus according to (40) 



U = 6 x 10 y gr cm sec , 



47 



