It can also be shown that if two surge heights are known, one to the left 

 and one to the right of the peak surge, then the peak surge height is 



Hp = (Srjn + 30.67 Hr + 19.01 Hl)/U9.68 (3) 



where Srp is the total distance measured along the coastline between the 

 points where Hpj and H^ were reckoned. This can also be extended to find- 

 ing the position of the peak surge on the coastline by either of the 

 following relations: 



Sp = 30.67 (Hp-Hj^) 

 S^ = 19.01 (Hp- H^) 



(M 



While developing surge-height profiles based on actual data, it was noted 

 that the curves exhibited a tendency to flatten out as the distance along 

 the coastline reached a position far to the left and right of the peak 

 surge. However, it was found that the relationship remained essentially 

 linear if these distances were limited to: 



Sr £ 2U.U Hp (5) 



Sl 1 15.0 Hp (6) 



Surge heights lying beyond this range, or at the outer periphery of the 

 hurricane are included implicitly in the water levels for nonhurricanes 

 which will be covered later. 



k. Computed Surge Heights 



Beta Hurricane siorge heights used in connection with this study are 

 based on those determined by Marines and Woodward (1968) for the entire 

 Texas Coast . These surge heights were computed based on previously 

 developed theory that was extended by Freeman, Baer, and Jung (1957) to 

 take into account the bathystrophic effect or longshore component of flow 

 caused by the Coriolis force. Calibration of the niomerical analogs of 

 the basic differential equations of fluid motion, appropriate to the 

 problem was carried out by adjustment of the seabed friction factor for 

 each basin investigated. Verification of reasonable calibration was 

 achieved by making comparisons of the computed surge heights to those 

 that actually occurred for various hurricanes of record. After adequate 

 calibration, the equations were used for predicting the surge heights 

 that would be expected from hypothetical hurricanes (i.e., of the Beta 

 type) by variation of the parameters, radius of maximiim winds (R), and 

 forward speed Vp. The results of this investigation are indicated on 

 Figiire 2. The radius of maximxmi winds is the distance from the eye of 

 the hurricane to the place where surface wind velocities are maximum; 

 this parameter reflects the areal extent of the storm. There is a 

 general tendency for R to exhibit a partial relationship to the CPI 



