the location of Matagorda Bay where the highest high water marks were 

 observed for this hurricane. The agreement is good over the entire 

 simulation period at Galveston. The effect of the reversing inflow 

 angle in the simulation is clearly pronounced as the computed water 

 level suddenly drops at approimately 2200 GMT 9 September. This 

 result is somewhat out of phase with that indicated by the 

 observations . 



Figures 30-32 show instantaneous fields of the barotropic and 

 baroclinic height anomalies and surface currents at 1200 GMT 10 

 September. Contours of the barotropic height (Fig. 30) clearly 

 demonstrate the inverted barometric effect around the storm center. 

 Upwelling along the hurricane path, a feature first investigated by 

 Leipper (1967) in the wake of hurricane Hilda in the Gulf of Mexico 

 in 1964, is noticeable in the baroclinic height field shown in Fig. 

 31. It should be remembered that the negative contours of the 

 baroclinic height anomalies correspond to upwelling of the interface. 

 Geisler (1970), ±n his linear analytic model, found that the 

 baroclinic response to a moving hurricane consisted of both upwelling 

 and inertio-gravity waves in the lee of the storm. Figures 31,32 

 strikingly portray this wake oscillation. Chang and Anthes (1978) 

 carried out numerical experiments to investigate the character of 

 this wake produced by various types of atmospheric forcing. They 

 found that the wavelength is longer for a faster moving storm and, 

 for the same forward speed of the storm, is shorter at higher 

 lattitude. In addition, within the limit of 50 h and 1200 km time 

 and space scales employed, the /J-effect (variation of f) did not 



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