subject since 1948, this formula has been applied for computing 

 the wind stress in table 1 of this report, and it is also being 

 used for a numerical analysis of wind driven circulation in the 

 North Atlantic Ocean. 



X . Conclusions, and some remarks on the model of the wind driven 

 ocean circulation 



a) The differential equation (11) for the horizontal mass 

 transport of the wind driven oceanic circulation seems to promise 

 a more realistic approach to a quantitative analysis of the hori- 

 zontal mass transport in the upper layers of the sea. It comes 

 a little closer to Ekman's original formulation of the problem, 

 since the "topographic curl effect" was shown to be of significant 

 importance throughout all of his papers. 



By writing equation (9) in terms of the vertically integrated 

 mass transport, M, with the components, U and V, it follows that 



"■"."-ffc-^g-tPiM-i, 



_ v 



(33) 



where dp/dx and dp/dy again represent average values of the hori- 

 zontal pressure gradients in the whole layer between z = -D and 



z = 0. With Ap I = g A(pD) 



l-D 



£ + gA(p£ )|£ 



-D l-D 



and 



IE 



ay 



-D 



£ 



-D 



= gp 



+ gD xt ' + gP *T- 



"4 ^ 



= gp" g * gD g + gp- <£- 



(34) 



oy 



j 



42 



