Preliminary Observations on the Hawai`I Earthquakes of October 15, 2006
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EERI Special Earthquake Report — December 2006 Learning from Earthquakes Preliminary Observations on the Hawai`i Earthquakes of October 15, 2006 This report was compiled by EERI Introduction the built infrastructure in the vicinity member Gary Chock of Martin & of the earthquake epicenters sur- Chock, Inc., Honolulu, Hawai`i. He Beginning at 7:07 a.m. local time on vived with little or no apparent dam- drew on his own observations as October 5, 2006, two earthquakes age. The low rates of injury and eco- well as information from and materi- with magnitudes of Mw6.7 and nomic loss are attributed in part to als prepared by a number of other Mw6.0 struck in close succession the relatively rural area in which the professionals: Ian Robertson, Peter just off the northwest coast of the earthquakes struck, and the focal big island of Hawai`i (see Figure ). Nicholson, and Horst Brandes, the depth (39 km) of the Mw6.7 Kiholo University of Hawai`i at Manoa; Shaking reached Intensity VIII on Bay earthquake. It was also fortun- Edward Medley, the Geo-Engineer- the Modified Mercalli Scale (MMI), ate that the earthquakes struck just ing Earthquake Reconnaissance as reported by residents. after sunrise on a Sunday morning. Association; Paul Okubo, the Ha- No deaths were attributed to ground There were numerous rockfalls and waiian Volcano Observatory; Barry shaking, and only minor injuries landslides in road cuts, embank- Hirshorn, the Pacific Tsunami Warn- were reported. Damage caused by ments and natural slopes on Hawai`i ing Center; Jiro Sumada, the County these earthquakes was estimated at Island, and road transportation was of Hawai‘i Department of Public more than $20 million as of mid- disrupted in some places. There Works; Ernest Lau, State of Hawaii November, without including dam- was damage to dams and irrigation Department of Accounting and Gen- age to private residences. Most of ditches in the Waimea area. Two eral Services; Afaq Sarwar, Sarwar Structural Engineering; John Dal Figure 1. Epicenter of the October 15 Kiholo Bay earth- Pino, Albert Chen, David Gonzalez, quake and the locations of island of Hawai`i towns William Grogan, Brenda Guyader, (USGS). Lisbeth Blaisdell, and Wayne Low, Degenkolb Engineers; and William Holmes, Rutherford & Chekene and EERI Learning from Earthquakes Program Committee chair. A number of organizations were al- so involved in the post-earthquake reconnaissance: ATC-20 building safety engineers from the Structural Engineers Association of Hawai`i; the Hawai`i State Earthquake Advi- sory Committee of State Civil De- fense, and the U.S. Geological Sur- vey’s National Strong Motion Pro- gram. Several reports, with many additional figures and photos, are available in their entirety on the EERI web site at http://www.eeri. org/lfe/usa_hawaii.html. The publication of this report is funded by EERI’s Learning from Earthquakes Program, under National Science Foundation Grant # CMS-0131895. EERI Special Earthquake Report — December 2006 kua fault zone on the southern Kona coast was the site of an earthquake of about magnitude 6.9 on August 2, 95, which damaged scores of homes on the Kona coast and trig- gered numerous damaging land- slides (see Figure 2). The Mw6.7 Kiholo Bay earthquake struck at 7.07 a.m. local time with an epicenter location of 9.878°N, 55.935°W, and a focal depth of ap- proximately 39 km (24 miles). It was followed by the Mw 6.0 Hawi earth- quake at 7.4 a.m. local time with an epicenter location of 20.29 N, 55.983 W, and a focal depth of approximately 9 km (2 miles). Strong ground motions lasted for approximately 20 seconds during the Kiloho Bay earthquake, and 5 seconds during the Hawi earth- quake. While the two events were only seven minutes apart, the differ- ence in depths and aftershock epi- centers suggests that the M6.0 may not be an aftershock of the M6.7, and that they were events from dif- Figure 2. Hawaii historical earthquakes and the inferred rupture zones of the ferent seismic sources. larger events (figure: Klein, F., USGS). Historically, the largest earthquakes in Hawai`i have occurred beneath dams had earth fill disturbance and churches and historic buildings with the flanks of the Kilauea, Mauna cracks along their crests, while at thick bearing walls constructed of Loa, and Hualalai volcanoes. The least two others showed clear evi- unreinforced lava rocks sustained flanks of these volcanoes adjust to dence of incipient slope failure on the most dramatic and potentially the intrusions of magma into their their embankments. A system of irri- life-threatening damage. adjacent rift zones by storing com- gation ditches feeding some of the pressive stresses and occasionally Over ,800 individual residences— reservoirs was interrupted due to releasing it in crustal earthquakes. less than 5% of the single family debris blockage. One of the two ma- The active fault surfaces for these home inventory—were damaged to jor commercial ports on the island, large earthquakes are associated varying degrees. Many of the most Kawaihae Harbor, sustained major with a near-horizontal basal décolle- severely damaged homes were con- damage from liquefaction and later- ment separating the ancient oceanic structed on post and pier foundation al spreading. This facility is located crust from the emplaced volcanic systems resting on small unanchored less than 24 km (5 miles) from both pile, lying approximately 0 km be- concrete foundation blocks. Several earthquake epicenters. neath the earth`s surface. (A dé- residences also had damage to lava collement is a tectonic surface that Most modern engineered buildings rock retaining walls—typically con- acts as a plane of detachment be- performed well, with some excep- sisting of individual, rough lava rocks tween two masses.) Examples of tions. Healthcare and school facili- stacked dry, or with minimal mortar. such crustal or décollement earth- ties had little structural damage, but quakes are the 975 M7.2 Kalapana considerable damage to their non- Seismotectonics earthquake beneath Kilauea`s south structural systems, principally T-bar flank, and the 1868 M7.9 earth- lighting and ceiling systems and Earthquakes on the island of Ha- quake beneath the Kau district on fire sprinkler systems. As a result, wai`i are not rare. The ground shak- Mauna Loa`s southeast flank, the they were not fully operational in the ing hazard in Hawai`i County ranks largest earthquake in recorded weeks following the earthquakes. among the highest in the United Hawaiian history. Close to the epicenters, older States. For example, the Kealake- 2 EERI Special Earthquake Report — December 2006 peak ground accelerations, and magnitudes suggested that Hawaii may not follow the typical models utilized in California and the main- land United States. The USGS found that accelerations in Hawaii are substantially higher than aver- age for a given intensity. Hawaiian earthquakes have to register at least a unit in magnitude greater than those in California to produce the same maximum intensity. Seismographic recordings of the October 5 earthquake showed a predominance of high frequency vibration (high accelerations with very short cycles) as compared to the types of earthquake motions in California earthquakes. Due to the atypically low amount of damage thus far observed (relative to U.S. mainland experience for a similar sized event) for the Kiholo Bay and Hawi earthquakes, it may be appropriate to further study whether Figure 3 certain seismic source regions of Hawaiian earthquakes produce ground motion with atypical fre- quency content and whether the fractured volcanic crust might lead to unique characteristics of fre- The Kiholo Bay earthquake probably Intensity VIII was reported close to quency-banded ground motion reflected the long-term accumulation the Hawi epicenter, and personal attenuation. and release of lithospheric flexural communications with residents of the stresses. The long-term stresses are North Kohala area indicate that its Three minutes after the initiation of generated in the crust and mantle effects in their area were as severe rupture at the first event’s hypocen- by the weight of the volcanic rock as, or even worse than, those of the ter, the Pacific Tsunami Warning that composes the islands. Deeper Kiholo Bay event. The shallower Center issued a Local Tsunami In- mantle earthquakes at approximate- Hawi hypocenter would plausibly in- formation Bulletin (LTIB) for the ly 30-40 km depth result from flexur- crease the severity of the local ef- state of Hawai`i. The LTIB stated al fracture of the underlying litho- fects of the smaller magnitude event. that a large earthquake had oc- sphere in long-term geologic re- Soil development on Hawai`i Island curred, but that there was no dan- sponse to the load of the island is most apparent at the older north- ger of a destructive tsunami. The mass. Past examples of such “man- ern end of the island (Kohala) and scientists were able to determine tle” earthquakes include the 973 along the wetter northeastern side rapidly that the rupture mechanism M6.2 Honomu (on the northeast (Hamakua). had a very small vertical displace- coast of Hawai`i island), the 938 ment component. The System for In USGS Bulletin 2006, Wyss and M7 Maui, and the 87 M7 Lanai Processing Local Earthquakes in Koyanagi (992) made a compilation earthquakes. Real Time (SPLERT) triggered this of 56 moderate to large Hawaiian response by paging duty scientists The effects of the earthquakes were earthquakes that occurred between with an accurate location 26 sec- felt on all islands in the state of 823 and 989, mostly of magni- onds after the origin time of the Hawai`i. Figure 3 shows the USGS tudes 5.4 to 6.6.