All- 101 1^ 



velocities will changet Specifically, if the depth is decreased, 

 the free surface deflection is increased and all out-of-phase 

 quantities are increased. 



The above results appear to invalidate the solution of 

 the problem as obtained by Ichiye [l6] » Ichlye neglected the 

 contribution of the non- steady term in the integrated continuity 

 equation. However, with the values of the parameters used in 

 Section ^5 the magnitude of this term in the interior of the 

 ocean is as much as ten times that of the remaining non-steady 

 terms which were retained in Ichiye 's analysis. 



V/e have computed the mass transport through the Gulf 

 Stream for the one-layer steady problem. With the given wind 

 distribution our result is 26,6 x 10 metric tons per second. 

 This value is about three-fourths of Munk's value [5"! and about 

 one-third of the observed value, Munk used an empirical east- 

 west v/ind distributioru 



The two-layer steady problem is solved in Section 5 

 where it is shown that the mass transport streamline pattern is 

 the same as in the one-layer problem. This is to be expected 

 since, for the steady case, the same assumptions are made regard- 

 ing negligible velocities below the thermocline. Thus, the 

 height of the thermocline is shown to be proportional to the 

 free surface deflection. Since the free surface height is deter- 

 mined largely by the thickness of the top layer, the thermocline 



* In [TdJ the term corresponding to W in the present paper 

 was assumed to be identically zero, i.e, , the wind had a 

 zero mean value, 



** The factor of proportionality is the reciprocal of the 

 density difference. 



