those provided by NWS, the problem of specifying the proper deforma- 

 tion is not completely resolved. 



The observed high winds which remain along the coast after the 

 storm has proceeded inland are attained by setting R^ to be the 

 distance the storm center is from that coastal area of persistent 

 high winds. This procedure was also followed in modeling the winds 

 from Hurricane Camille. However, R^ in the pressure expression 

 was not allowed to increase in this manner. 



The hydrographs at selected grid points along the coast are 

 presented in Figure 42 illustrating the improved agreement with 

 respect to the observed water levels in using a deformed wind 

 forcing function rather than a symmetric one. The observed water 

 levels, corrected for the astronomical tide, are indicated by 

 squares. The computed water levels have been raised for comparison 

 purposes to correspond to the local sea level at the start of the 

 computations (1800 G.m.t., 9 September). The solid line represents 

 the computed surge employing the deformed wind and the dashline 

 shows the results with a symmetric wind. The surge computations 

 were formed using identical boundary conditions. 



The symmetric (a) and deformed (b) winds for Hurricane Camille at 

 0000 G.m.t. 18 August 1969 (approximately 4 hours before the storm 

 crossed the coast), 0400 G.m.t. and 0800 G.m.t. on the same date 

 are shown in Figures 43 through 45. The rotation and reduction of 

 the wind stress for this storm are different from that of Hurricane 

 Carla because of the differences in the coastal configuration. 

 Figure 46 (a,b) shows the wind vectors for the symmetric and deformed 

 representation of Hurricane Camille at the time the storm proceeded 

 inland. The pressure fields at the above times are presented in 

 Figure 47(a,b,c). The wind fields associated with Hurricane Gracie 

 were not deformed because the documentation was not amenable to the 

 deformation procedure. Also, R^ was not increased in the manner 

 specified above after the storm crossed the coast. The symmetric 

 winds at 1200 G.m.t., 29 September 1959, 1600 G.m.t. (the time the 

 storm proceeded inland), and 2000 G.m.t. on the same date are shown 

 in Figure 48. Figure 49 presents the pressure fields at the above 

 times. 



81 



