Q T Ji,JM,n+l) = , (75) 



i = 1,3 • • • IM . 



Thus, total reflection is assured at the boundary. The flu.x, Qs*» 

 along the coastline is calculated from equation (55) with D taken 

 as the two point average of the local fluid depths along the coast. 

 The local depths ranged from 1.0 to 2.3 meters, depending on the sea- 

 ward bottom slope and surrounding elevations. The water elevations 

 along the coast are computed from the continuity relation as given 

 by equation (57) with the following substitution: 



F(i,JM+l) Q T *(i,JM+l,n-l) = -F(i,JM-l) Q (i,JM-l,n-l) , (76) 



i = 2,4 • • • IM-2 . 



This is an artifact consistent with total reflection. 



Foi' the simulation of the Hurricane Camille storm surge, the 

 normal routine of the surge program was interrupted at those grid 

 points representing the protruding Mississippi Delta. Along this 

 part of the coast (the solid heavy line in Figures 28 and 29), the 

 normal flux was set to zero and the tangential flux was determined 

 from either equation (55) or equation (56) with the Coriolis term 

 vanishing. The continuity relation is altered depending on the 

 orientation of the boundary to be consistent with total reflection. 



The open deep sea boundary condition is : 



H(i,l,n+1) = H D (i,l,n+l) , (77) 



D 



i = 2,4 • •• IM-1 , 



and 



H(i,2,n+1) = [H(i-l,l,n+l) + H(i+l,l,n+l) 



+ H(i-l,3,n+l) + H(i+l,3,n+l)]/4 , (78) 



i = 3,5 • • ■ im-2 . 



Specifying the seaward boundary in this sawtooth form obviates the 

 calculations of Qg* and Q-p* along the boundary since they are not 

 required for computations at interior points. 



The lateral open boundary condition requires the normal gradient 

 of the S*-directed transport to vanish, 



72 



