of Kachadoorian and Plafker (196t)j who considered the runup to he only 

 15.7 feet above MLLW. 



The latter authors report that the house which survived the tsunami, 

 although flooded, was securely tied down to a concrete foundation. Its 

 location in Figure 129 is unknown. The cost of replacing the homes and 

 aiixiliary buildings has been estimated at $707,000. 



Kaguyak, a small fishing village at the head of Kaguyak Bay (Figures, 

 1 and UO), although undamaged by the earthquake, was completely destroyed 

 by the tsunami. The first wave came approximately 20 minutes after the 

 quake and the largest (probably the third) struck at about 9:00 p.m. 

 The houses of the village were carried across the spit on which they 

 stood and were diimped into or washed up the far shore of the intermedi- 

 ate lagoon. The maximum runup was about 32 feet above postquake MLLW 

 according to Berg, et al (l96i+), but is given as 25 feet above MLLW by 

 Kachadoorian and Plafker (1967). The high runup was probably due to a 

 resonance effect of Kaguyak Bay on the seismic sea waves. Three of the 

 37 inhabitants of the village drowned. Loss of property has been esti- 

 mated at $321,000. The survivors have moved to Akhiok and Old Harbor. 



Total losses of property and income in communities on Kodiak Island 

 and neighboring islands have been estimated at $^5,509,300 (Kachadoorian 

 and Plafker, 1967). The distribution of this amount is detailed in Table 

 E-h of Appendix E. 



5. Seismic Sea Waves in Cook Inlet 



On the Continental Shelf opposite the entrance to Cook Inlet, 

 a vast negative wave, extending from beyond the Barren Islands into the 

 Inlet, woiild have been created almost instantly with the subsidence of 

 the land at the mouth of the Inlet. The ensuing wave system that would 

 advance from the hinge line of zero vertical earth movement could be 

 expected to be similar in general to the waves that reached Kodiak, but 

 different in detail according to the special oscillating characteristics 

 of the Continental Shelf in this region. We envision an Interplay of 

 the gravity waves of separation (Figure ^2) with parallel free oscilla- 

 tions of the shelf, advancing on a front parallel to the hinge line 

 (Figures 33 and 130). The first crest would have to travel a distance 

 of about 70 nautical miles at a mean speed for a mean depth of UOO feet, 

 according to Equation {h) , of approximately 115 feet per second, and 

 thus should have reached the neighborhood of Perl Island (Figure 130) 

 about one hour after the earthquake, or at about 6:hO p.m. The second 

 wave would probably have followed at about 8:i+0 p.m. 



Perl Island was actually struck by a 28-foot wave at 8:i+0 p.m. 

 (Waller, 1966). This was followed by a second wave of 30 feet at 11:U0 

 p.m. and a third wave, also about 30 feet high, at 2:30 a.m. on March 28. 

 The time interval between these waves is three hours. In the absence of 

 a detailed calculation of the oscillating characteristics of the open- 

 ended basin system illustrated in Figure 36b, we feel unqualified to 

 elaborate further on this phenomenon. 



198 



