All- 101 35 



T^ and, in addition, the stress of the ocean bottom on the 

 2x 



lower layer, is so complex that an analytic solution is out of 

 the question. V/e therefore assume that the effects of these 

 shear stresses on the velocity in the lov/er layer are negligible 

 when compared to the velocity resulting from the variation of 

 the thermocline. 



If the two problems v;ere now solved and the results 

 compared with available observational data, it might be possible 

 to determine whether or not sensible deep-water motion exists. 

 As we shall see in Sec, 5? however, Problem 2 cannot be solved 

 by the methods used in the present paper, and numerical methods 

 of solution may have to be employed* 



*+• Solution to Pro,ble_m_l« The solution to Problem 1 

 will be carried out by means of a boundary layer technique. For 

 the convenience of the reader who is not familiar with this 

 technique and who wishes to follov; the details of the present 

 section, a discussion of boundary layer analysis is presented 

 in Appendix 5» 



The solution of differential equations by boundary layer 

 analysis can be carried out most conveniently if the equations 

 are first put into non-dimensional form. Let the rectangular 

 ocean have dimensions 



0<x<r-j_, 0<y<s (Fig. 1). 



Choose as a reference length the north- south dimension, 

 s, and define dimenslonless coordinates x', y' by 



