By J.-P. Bardet, C. E. Synolakis, H. L. Davies (auth.), Jean-Pierre Bardet, Fumihiko Imamura, Costas E. Synolakis, Emile A. Okal, Hugh L. Davies (eds.)
In the wake of the disastrous tsunami which struck Papua New Guinea in 1998, this quantity offers 20 cutting-edge contributions on landslide tsunamis, together with earthquake features and floor motions, modeling of landslides in geotechnical engineering, box surveys on land and at sea, simulations of earlier, current, and power destiny tsunamis, and theoretical experiences of tsunami iteration by way of landslides.
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Extra info for Landslide Tsunamis: Recent Findings and Research Directions
Sample text
The minimum number of observed events at these stations was 3. 1832 Nobuo Hurukawa et al. Pure appl. , Figure 2 The fifty-nine stations used in this study for relocation of the 1998 Papua New Guinea earthquake sequence. The asterisk at the center of the left-hand map represents the epicenter of the main shock. 5 140 E 14 1 E 142 E 143 ]' 0 ~ 50 frlOO Cl o 50100 144 E Depth(km) 4 5~ 7 "00 Oepth(km) -200 -100 0 100 Oi tancc(km) 200 o 10 2030 ol Figure 3 Hypocenter distribution of the 1998 Papua New Guinea earthquake sequence during the period from July 17 through August 31,1998.
L991) to relocate these events, including an assessment of their 95%-confidence ellipses through a Monte Carlo method injecting Gaussian noise (with standard deviation O"G) into the data set. Note that, while the two events considered are legitimate contenders for the generation of the tsunami in terms of their timing, their size clearly rules out explaining the amplitude of the observed run up as due to any model of those earthquakes as standard dislocations in an elastic medium. , 1999). It is then legitimate to assume that the 09:02 event took place at the location of the observed slump, inside the amphitheater.
Geological Survey (USGS), which includes three stations at the northeastern edge of Irian Jaya and one station in northern Papua New Guinea, from which the epicentral distances are less than 2 degrees. Secondly, in addition to the above permanent-station data, we used data from temporary aftershock observations near the epicentral area around the Sissano Lagoon carried out by TSUJI el al. (1998) . Using three-component seismometers, they carried out observations from August 2 to October 2, 1998 at three sites.