oceans alone, 3,9 ergs sec would be supplied to each square centimeter 

 of ocean surface. The total area of ocean involved is 361x10 km , (S, 15). 

 When discussing Taylor's method of computing tidal dissipation, Jeffries 

 shows that practically all of this energy is lost in the form of heat in 

 shallow seaSo Thus, very little of it could be converted into turbulent 

 motion in deep ocean. 



The sun produces motion in the sea by a variety of processeSo Direct 

 heating of the water produces mechanical effects as does heating of the atmos- 

 phere with its concomitant winds. 



The energy supplied by the winds was obtained from the product of 

 the stress t exerted by wind on the surface of water and the associated 

 water velocity. Stresses were calculated from the equation 



-6 2 



X = 3.2xlO^W'^ , 



where W is the wind velocity, and W and x are in c.g.s. units. %. marine 



atlas (Uob. Navy 1955) was used to estimate average winds for each month in 



-2 



the North Atlantic. An average wind stress of 1;1 dynes cm was obtained. 



The surface velocity imparted to the water was then assumed to be 3 per cent 

 of the wind velocity (Hughes, 1957) and the shear stress-velocity products 



for each month were obtained. The average rate of energy input to the water 



-2 -1 

 during a year was found to be 32 ergs cm sec . Knauss (1956) used a 



-2 -1 

 value of 15 ergs cm sec which he obtained from averaged surface currents. 



Most of this energy is probably converted to motion in the layer of water 



above the thermocline. 



An approximate value for the kinetic energy obtained from the sun 



can be obtained by not questioning details of the process. Although the 



yearly average incidence of radiation on the North Atlantic is approximately 



-1 -2 

 .004 cal sec cm (S, 103), only a small fraction of that energy can be 



