Tsunami Deposits from the 1993 Southwest Hokkaido Earthquake and the 1640 Hokkaido Komagatake Eruption, Northern Japan

Nishimura, Yuichi; Miyaji, N.

doi:10.1007/978-3-0348-7279-9_19

Cited by 36 publications

(44 citation statements)

References 9 publications

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“…In the proximal area, the first pumice fall is covered by the overlying welded Funakura ignimbrite. (2) Tsunamis inundated the area before or after pyroclastic flow but tsunami deposits or other traces of tsunami inundation were not left, because a steep slope or nearshore flat beaches allowed the tsunami to erode the original surface (Nishimura and Miyaji, 1995;Gelfenbaum and Jaffe, 2003). In addition, most coasts are .…”

Section: Interpretation Of Tsunami Traces In Each Coastalmentioning

confidence: 99%

Numerical simulation of tsunamis generated by caldera collapse during the 7.3 ka Kikai eruption, Kyushu, Japan

2006

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The relationship between tsunamis and scales of caldera collapse during a 7.3 ka eruption of the Kikai volcano were numerically investigated, and a hypothetical caldera collapse scale was established. Wave height, arrival time, and run-up height and distance were determined at some locations along the coastline around Kikai caldera, using non-linear long-wave equations and caldera collapse models using parameters showing the difference in geometry between pre-and post-collapse and the collapse duration. Whether tsunamis become large and inundations occur in coasts is estimated by the dimensionless collapse speed. Computed tsunamis were then compared with geological characteristics found in coasts. The lack of evidence of tsunami inundation at Nejime, 65 km from the caldera, suggests that any tsunamis were small; indicating that the upper limit of dimensionless caldera collapse speed was 0.01. On the other hand, on the coast of the Satsuma Peninsula, 50 km from the caldera, geological characteristics suggests that tsunamis did not inundate, or that even if tsunamis inundated the area, the traces of a tsunami have been eroded by a climactic pyroclastic flow or the tsunami itself and they have not been left. In numerical computations, when a dimensionless caldera collapse speed is more than 0.003, tsunami can inundate this area.

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Section: Interpretation Of Tsunami Traces In Each Coastalmentioning

confidence: 99%

Numerical simulation of tsunamis generated by caldera collapse during the 7.3 ka Kikai eruption, Kyushu, Japan

2006

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“…During the last 15 years, much effort has been devoted to documenting the various recent tsunami deposits (Nishimura and Miyaji, 1995;Sato et al, 1995;Shi et al, 1995;Dawson et al, 1996;Minoura et al, 1997;Bourgeois et al, 1999;Gelfenbaum and Jaffe, 2003;Nanayama and Shigeno, 2006;Higman and Bourgeois, 2008;Goto et al, 2011;Moore et al, 2011). The majority of these works focused on documentation of the 2004 Indian Ocean Tsunami (IOT) depositional effects along the coasts of Sumatra (Moore et al, 2006;Razzhigaeva et al, 2006;Richmond et al, 2006;Paris et al, 2007Paris et al, , 2009, Thailand (Hori et al, 2007;Kelletat et al, 2007;Choowong et al, 2008a, b;Matsumoto et al, 2008;Sawai et al, 2009;Fujino et al, 2010;Naruse et al, 2010), Sri Lanka (Morton et al, 2008), India (Bahlburg and Weiss, 2007;Srinivasalu et al, 2007) and Maldives (Kench et al, 2006).…”

Section: Introductionmentioning

confidence: 99%

26 December 2004 tsunami deposits left in areas of various tsunami run up in coastal zone of Thailand

Szczuciński

Rachlewicz

Chaimanee³

et al. 2012

Earth Planet Sp

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The tsunami deposits left by the 26 December 2004 tsunami in the coastal zone of Thailand were studied within two months of the event and before any significant postdepositional changes could occur. The sediment structure and texture (grain size), as well as its thickness and spatial distribution, were documented for the tsunami deposits in 12 shore-perpendicular transects from areas of various tsunami runup and wave heights. The tsunami deposits were as thick as 0.4 m and were located as far as 1.5 km inland. They were composed mostly of poorly sorted sand and often consisted of one to four normally graded, massive or laminated layers. The deposits generally became finer in the landward direction; however, landward thinning trend of the deposits is not clear, and the maximum accumulation often is not located close to the shoreline but rather is further inland. In comparable coastal environments with similar available sediment sources the tsunami size (represented as the tsunami runup height) is reflected in the resulting deposits. Larger tsunamis are associated with deposits that are thicker, have a maximum accumulation located farther inland, include a finer sediment fraction (likely from deeper offshore areas) and frequently are composed of normally graded layers.

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“…The tuff ring deposits adjacent to the base of the eroded slope are interbedded with layers, 10-20 cm thick, that are rich in clasts of yellow, altered rock, and pieces of plants eroded from the slope. Such layers are interpreted as backwash deposits of the tsunamis (Nishimura & Miyaji, 1995) and/or of water pyroclastic flows formed from water-rich base surges. Along the rest of the shoreline the action of the multiple tsunamis in many places formed new beaches up to 50 m wide (area A in Fig.…”

Section: Tsunamismentioning

confidence: 99%

Eruptive Process, Effects and Deposits of the 1996 and the Ancient Basaltic Phreatomagmatic Eruptions in Karymskoye Lake, Kamchatka, Russia

Belousov

Belousova

2001

Volcaniclastic Sedimentation in Lacustrine Settings

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On 2-3 January 1996 an explosive eruption discharging = l0 6 kgs -1 of basaltic magma occurred in Karymskoye lake at an initial water depth of ~ 50 m. Characteristics of the deposits together with analyses of a videotape of several explosions have allowed us to model the eruptive events. Initial vent-clearing phreatic explosions ejected blocks of country rocks (up to 3 m diameter) to distances of up to 1.3 km. Then followed 10-20 h of phreatomagmatic Surtseyan activity (100-200 outbursts of water-gas-pyroclastic mixtures to heights of up to 1 km, with initial velocities of 110 m s -1 |. The eruption slugs collapsed back into the lake and produced base surges (runout up to 1.3 km; average velocity 12.5 m s -1 ). The convective eruption plume rose to a height of 3 km and deposited a thin distal fall deposit. The eruption ended with the ejection of scoria-crust bombs (specific basaltic bombs with dense core and scoriaceous crust).Pyroclasts of the eruption are mostly poorly to moderately vesicular juvenile basaltic particles shaped by a combination of magmatic vesiculation and magma-water interaction. Ninety-five percent of the products (0.047 km 3 ) formed an underwater tuff ring composed of parallel layers of moderately to poorly sorted lapilli ash and ash lapilli (Md -3.9 to 0.6 phi; sorting 1.5-3.2 phi), each 10-60 cm thick. They were deposited by water-rich base surges that originated from Surtseyan type eruption bursts. The most widespread hazards of the eruption were tsunamis and lahars. At distances < 1.3 km from the crater, base surges and ballistic clasts were very destructive.Eruptive activity in the lake before 1996 included two eruptions at c. 4800 14 C yr BP. The first left deposits similar to those of the 1996 eruption and thus is interpreted as a Surtseyan eruption that occurred at the same water depth as in 1996. The second of the 4800 l4 C yr BP eruptions deposited extensive cross-laminated base-surge deposits and is interpreted to have occurred in very shallow water.

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Tsunami Deposits from the 1993 Southwest Hokkaido Earthquake and the 1640 Hokkaido Komagatake Eruption, Northern Japan

Cited by 36 publications

References 9 publications

Numerical simulation of tsunamis generated by caldera collapse during the 7.3 ka Kikai eruption, Kyushu, Japan

Numerical simulation of tsunamis generated by caldera collapse during the 7.3 ka Kikai eruption, Kyushu, Japan

26 December 2004 tsunami deposits left in areas of various tsunami run up in coastal zone of Thailand

Eruptive Process, Effects and Deposits of the 1996 and the Ancient Basaltic Phreatomagmatic Eruptions in Karymskoye Lake, Kamchatka, Russia

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