of the seabed have been made. In order to define the shape of the rupture 

 zone and the uplift distribution of each deformation in the synthesized rec- 

 ord, it was assumed that the rupture zone and uplift of the 1964 event were 

 appropriate to use as a model for all proposed deformations. A record of 

 tectonic deformations of the seabed was synthesized by specifying that each 

 deformation in the record would have not only the same location but also the 

 same rupture zone shape and uplift distribution (but different magnitude of 

 uplift) as that caused by the 1964 Alaskan earthquake. 



Numerical Model 



16. The linear nondispersive shallow-water equations used to model the 

 propagation of tsunamis are 



at R 36 d v ; 



&■ = - — £_ in _ fu - Kv (2) 



3t R sine 34) d 



3n _ 1 < 9 |_(d+n) u sine] 3l_(d+n)v] [ n) 



3t R sine ( 36 3<t> J 



where 



u,v = vertically averaged velocity components in the 6 and $ 

 directions 



t = time 



g = acceleration because of gravity 



R = radius of the Earth 



n = displacement of the water surface from the still-water level 



9 = latitude measured from at the North Pole 



f = Coriolis parameter 



k = linear friction coefficient 



d = still-water depth 



(j> = longitude measured east from Greenwich 



17. Kowalik and Murty (1984) used these equations to study the tsunami 

 propagation resulting from a predicted major earthquake in the Shumagin 

 seismic gap area of the Aleutian Island chain. These or similar linear 



10 



