number; N=l, NE=2, E=3, SE=4, S=5, 

 SW=6, W=7, NW=8. The term f.-.j in 

 equation (1) was represented by FA 

 (K) for the wind intervals UA through 

 UE. A wind stress was calculated for 

 each wind direction so that T (1) = 

 stress to the north, T(2) = stress to the 

 northeast and so on. The surface of the 

 coastal area was placed in a cartesian 

 coordinate system with positive T x 

 representing a stress toward the east 

 and positive T^- representing a stress 

 toward the north. Thus the wind stress 

 equation from any direction appears as 

 follows: 



T(K)=CA*FA(K)»UA + 

 CB«FB(K)»UB + 

 CC*FC(K) # UC + 

 CD # FD(K)*UD + 

 CD*FE(K)*UE 



The final T^ and T^, for a particular 

 month and coastal area was computed 

 as: 



T. = YU = T(l) + .707 T(2) 

 ' - .707 T(4) - T(5) - .707 T(6) 

 + .707 T (8) 



T x = XU = .707 T(2) + T(3) 

 + .707 T(4) - .707 T(6) 

 - T(7) - .707 T(8) 



Appendix A is a copy of the TAUCOM 

 program. 



Appendix B is a listing of TAUCOM 

 stress outputs. 



RESULTS 



Atlantic and Gulf of Mexico Coasts 



Figures 1 through 12 show average 

 monthly wind stress as calculated by 

 TAUCOM. The winter months Dec- 



ember, January, February , along the 

 east coast of the United States show a 

 generally southeast stress. The 



magnitude of the stress generally de- 

 creases southward along the coast to 

 the Charleston area. From Jacksonville 

 to the Corpus Christi area the maxi- 

 mum magnitude appears in late fall. 

 This difference is apparently due to the 

 position of the North Atlantic High 

 Pressure System. In December and 

 January this high generally extends 

 across the U.S. and mid-Atlantic area as 

 a fairly wide (10* ) belt. At the same 

 time the Icelandic Low Pressure System 

 lies generally over Eastern Greenland 

 producing a moderate pressure gradient 

 in the northeastern U.S. This would 

 account for the 1.30 dynes cm" 4 in 

 the Boston and Quonset Point area. In 

 the Charleston area the maximum is 

 0.88 dynes cm~* , due to the lesser 

 pressure gradient. 



The areas from Jacksonville to 

 Corpus Christi during January and 

 February are influenced by the weak 

 pressure gradient which occurs be- 

 tween the North Atlantic High Pres- 

 sure S ystem and the Inter - Tropical 

 Convergence Zone (ITCZ). This is 

 evident by the change in stress di- 

 rection and the lower stress magni- 

 tudes. In March, from Boston to the 

 Miami area the stress magnitudes begin 

 to decrease appreciably due to the 

 weakening pressure gradient between 

 the Icelandic low and the North 

 Atlantic high. The pressure gradient in 

 the Gulf coastal area is generally weak. 

 March also generally shows the first 

 indication of the development of the 

 thermal low pressure area of the Pacific 

 southwest and Mexico. April shows 

 the first significant change in stress 

 direction along the east coast. This 

 stress has shifted generally to the east- 



