Gyre (32.5 N, 57.5 W) in May and June would be a 

 suitable location. Here the sea currents average 

 .45 k (23 cm sec ) with no consistent direction in a 

 5° square centered at the above position. A large 

 portion of the currents in the region may be due to 

 wind driven oscillations, due to the steady winds 

 and shallow thermocline, as we shall see. The 

 inertial frequency at this latitude is 22.33 hours. 

 This should be separable from diurnal tidal oscil- 

 lations, with a frequency of 24.8 hours. There 

 exists a very shallow thermocline beginning near 

 the surface of .06°C meter . The thermal struc- 

 ture of the area is homogeneous for a radius of 500 

 km around the site. (U.S. Naval Oceano. Off. Pub. 

 700). Surface winds for May and June aremostly 

 from S to SW, with a mean velocity of 12 knots 

 with 16% of winds being 16-21 knots (Navaer 

 50-1C-528). 



These shallow mixed layers and moderate 

 winds should produce very strong intertial oscil- 

 lations. Significant changes should also occur to 

 the thermocline during this period due to the 

 seasional warming of the sea at this position, 

 large wind stresses and shallow initial mixed 

 layers. 



The mooring itself should have current meters 

 and thermistors spaced as closely as possible 

 through the mixed layer and through the ther- 

 mocline to record variations of the currents with 

 depth in the mixed layer. The wind recorder 

 should be mounted as high above the sea surface 

 as possible, to free the wind measurements from 

 near boundary processes as much as possible. 



To determine more accurately the sea currents 

 in the area, standard sections should be taken 

 around the mooring when it is set and when it is 

 retrieved to determine by dynamic methods the 

 steady sea currents in the area. 



CONCLUSIONS 



I have, with reasonable success, modeled the 

 wind driven inertial oscillations in the deep 

 oceans, and demonstrated the importance of a 

 two dimensional model on the solution for surface 

 transport. This integration of thermocline mod- 

 els into the current models is very necessary 

 because of the large effects of vertical structure 

 on the total result. It is unfortunate that data in 

 the two dimensions is not available, but the 

 experiment I have proposed should yield data 

 usable to test this type of model. Even with the 



data now available, more work can be done to 

 obtain a better fit. Unfortunately, time constraints 

 have forced me to stop work on testing the model 

 at this point. The dissipation coefficients I found 

 may well be much too high, for the modeled 

 motions tend to die out much faster than the data 

 as seen in Figure 4.11. More experience with 

 statistical methods and demodulation of the data 

 set to derive inertial motions would also be help- 

 ful. Hopefully this paper will stimulate more 

 interest in the mixed layer and its atmospheric 

 interactions. 



Acknowledgements 



The author wishes to thank his research super- 

 visor, CAPT R. C. KOLLMEYER, USCG for 

 invaluable assistance in the fine points of this 

 project. This paper forms the report on the 

 author's undergraduate Independent Studies 

 courses. This research was supported by the 

 Department of Physical and Ocean Sciences, 

 U.S. Coast Guard Academy. 



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