Figure l88 shows that Port Wells and its tributary fjords are a 

 relatively deep and intricate system of connecting basins whose os- 

 cillating characteristics are apt to be complex. No attempt has been 

 made to determine this oscillating regime. It may be noted from Figure 

 188 (inset) that Whittier lies on the northwest side of the hinge line 

 of zero vertical earth movement running through Prince William Sound. 



The delta upon which Whittier rests and also the southern part of 

 the delta at the head of Passage Canal are formed of unconsolidated 

 deposits. These consist of outwash and stream gravels composed pre- 

 dominantly of subangular to subrounded gravel in a matrix of coarse sand 

 (Kachadoorian, I965). Figure I89 is a prequake map of Whittier and its 

 immediate vicinity; its rather limited area on the fan delta is illus- 

 trated by the aerial view of the town and port facilities prior to the 

 earthquake (Figure 190). 



The extensive damage suffered by Whittier was caused by (l) seismic 

 shock, (2) submarine landslides, (3) waves, (U) fracturing and compaction 

 of fill and unconsolidated sediments, (5) fire, and (6) a 5.3-foot sub- 

 sidence of the landmasses. The port was rendered totally inoperative, 

 and for a time was without rail communication (Eckel, I967). 



The destructive waves that lashed Whittier were undoubtedly gene- 

 rated by submarine landslides. Figure I9I shows the areas affected by 

 slides and some pre- and postquake profiles indicating the amount of 

 landmasses involved in the slides (Kachadoorian, I965). 



An inferred marigram for Whittier has been constructed in Figure 192, 

 but data are extremely limited. Not many people witnessed the waves. 

 Some of those who watched the water (cf. Bryant, 196^+; Kachadoorian, 1965; 

 Chance, I968) have reported that, approximately one minute after the 

 earthquake started, the water in Passage Canal in the vicinity of the 

 town rose rapidly to about 30 feet above tide level for that time, which 

 was about 1 foot above MLLW. The water was glassy and did not contain 

 any debris. 



The water immediately receded, and the "glassy h\imp" apparently did 

 not encroach on the shore as a wave above normal maximum tide level. The 

 first damaging wave struck Whittier at 1 to 1.5 minutes after the glassy 

 hiimp occurred. This wave was muddy and contained much debris which 

 radiated from a boil halfway across Passage Canal. The crest of the 

 wave was 3^ feet above water level when it reached the Alaska Railroad 

 depot (see Figures 191 and 193). It struck the depot 8 to 10 feet above 

 ground level . 



About 1/2 to 1 minute after the first damaging wave (second rise of 

 water) another damaging wave rolled in on Whittier. Its crest reached 

 about 30 feet above tide level at the Alaska Railroad Depot (Bryant, I96U) 



No waves other than the two that struck during the earthquake have 

 been reported. The high waves which reached Cordova and Valdez late in 



296 



