Generation mechanism of tsunamis from the 1883 Krakatau Eruption

Nomanbhoy, Nazli; Satake, Kenji

doi:10.1029/94gl03219

Cited by 100 publications

(72 citation statements)

References 6 publications

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“…The modeling of the tsunami sources of the volcanic eruption is extremely difficult task and three hypotheses: caldera collapse, submarine explosion and pyrolastic flow are actively considered for the Krakatau event (Francis, 1985). Recently Nomanbhoy and Satake (1995) concluded that the submarine explosion model as the source of the largest tsunami is favored. The global behavior of the tsunami waves during the 1883 Krakatau event should be determined by the integral characteristics (period, amplitude) on the waves going out the Sunda Strait only, not by the details of tsunami generation.…”

Section: Hydrodynamic Long Wave Modelingmentioning

confidence: 99%

“…The large difference in the computed and observed periods needs to be explained. According to the calculations by Nomanbhoy and Satake (1995), the characteristics period of the first two tsunami waves near the Krakatau Island, in the Sunda Strait is about 1 h (but the wave form is far from simplest sine), and, therefore, this low-frequency spectral component should be in the tsunami spectrum on any distance from the source, including the Port Blair. The computed tide-gauge record has the wide spectrum, and this low-frequency component is weak.…”

Section: Hydrodynamic Long Wave Modelingmentioning

confidence: 99%

“…He simulated also the tsunami wave propagation in the adjacent part of the Indian Ocean and the comparison with the observed data leads to the estimated depth in the equivalent tsunami source in 700 m. The Krakatau tsunami was also numerically simulated by Kawamata et al (1992) for the region of outside the Sunda Strait by assuming the caldera formation, which makes the surrounding water rush into the cavity. Nomanbhoy and Satake (1995) investigated the mechanism of the tsunami generation at the Krakatau volcanic eruption. Based on the numerical simulation of the near field (Java and Sumatra) they concluded that the submarine explosion model as the source of the largest tsunami is favored.…”

Section: Introductionmentioning

confidence: 99%

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Simulation of the trans-oceanic tsunami propagation due to the 1883 Krakatau volcanic eruption

Choi

Pelinovsky

Kim

et al. 2003

Nat. Hazards Earth Syst. Sci.

118

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Abstract. The 1883 Krakatau volcanic eruption has generated a destructive tsunami higher than 40 m on the Indonesian coast where more than 36 000 lives were lost. Sea level oscillations related with this event have been reported on significant distances from the source in the Indian, Atlantic and Pacific Oceans. Evidence of many manifestations of the Krakatau tsunami was a subject of the intense discussion, and it was suggested that some of them are not related with the direct propagation of the tsunami waves from the Krakatau volcanic eruption. Present paper analyzes the hydrodynamic part of the Krakatau event in details. The worldwide propagation of the tsunami waves generated by the Krakatau volcanic eruption is studied numerically using two conventional models: ray tracing method and two-dimensional linear shallow-water model. The results of the numerical simulations are compared with available data of the tsunami registration.

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Section: Hydrodynamic Long Wave Modelingmentioning

confidence: 99%

Section: Hydrodynamic Long Wave Modelingmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

See 1 more Smart Citation

Simulation of the trans-oceanic tsunami propagation due to the 1883 Krakatau volcanic eruption

Choi

Pelinovsky

Kim

et al. 2003

Nat. Hazards Earth Syst. Sci.

118

View full text Add to dashboard Cite

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“…The eruption began on 20 May 1883 and volcanic activity continued for a few months until the final cataclysmic explosive events on August 26 and 27. Tsunamis were generated by emplacement of pyroclastic flow deposits, caldera collapse of the northern part of Krakatau Island and a huge submarine explosion (Nomanbhoy and Satake, 1995). The main catastrophic tsunami occurred on 27 August 1883 and caused the death of more than 36,000 people, as 295 villages and towns were destroyed or damaged in Java and Sumatra along the Sunda Strait (Simkin and Fiske, 1983).…”

Section: Introductionmentioning

confidence: 99%

Geoarchaeological tsunami deposits at Palaikastro (Crete) and the Late Minoan IA eruption of Santorini

Bruins

MacGillivray

Synolakis

et al. 2008

Journal of Archaeological Science

168

134

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The explosive eruption at Santorini in the Aegean Sea during the second millennium BCE was the largest Holocene volcanic upheaval in the Eastern Mediterranean region. The eruption was disastrous for the Minoan settlements at Santorini, but the effect on human society in the neighbouring islands and regions is still clouded in uncertainty. Tsunami generation was suggested, but comparatively little evidence was found. The lack of firm tsunami traces is particularly puzzling in Crete with its coastal settlements of the Late Minoan IA period, during which the Santorini eruption occurred. Here, we report the discovery of extensive geoarchaeological tsunami deposits at Palaikastro in north-eastern Crete. These deposits are characterized by a mixture of geological materials, including volcanic Santorini ash, and archaeological settlement debris. Various tsunami signatures were identified: (1) erosional contact with the underlying strata, (2) volcanic ash intraclasts in the lower part of the deposit, (3) reworked building stone material in the lower part of the deposit, (4) individual marine shells, (5) marine micro-fauna, (6) imbrication of rounded beach pebbles, settlement debris, ceramic sherds and even bones, (7) multi-modal chaotic composition. Late Minoan human settlement activities at Palaikastro provided architectural and stratigraphic frameworks in space and time that recorded and preserved tsunami evidence as geoarchaeological deposits. Such stratigraphic resolution and preservation may not occur in the natural landscape. Volcanic ash transported by wind from Santorini south-east to Crete preceded the tsunami. Geological, archaeological and radiocarbon dating criteria all converge, indicating that the tsunami deposits are coeval with the Minoan Santorini eruption. Field evidence suggests that tsunami waves at Palaikastro were at least 9 m high. Inverse tsunami modeling was attempted, based on these newly discovered tsunamigenic deposits. The initial wave in the generation region at Santorini that best fits the stratigraphic data is a wave with þ35 to À15 m initial amplitude and a crest length of about 15 km.

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“…The eruptive processes, and the source and time propagation of the tsunamis have been widely debated on the basis of observations, analysis of nearfield (<20 km from Krakatau volcano) pyroclastic deposits, tide and pressure gauge records, and numerical modelling (Verbeek 1886;Stehn 1929;Williams 1941;Ewing and Press 1955;Latter 1981;Self and Rampino 1981;Yokoyama 1981Yokoyama , 1987Camus and Vincent 1983;Francis 1985;Self 1992;Nomanbhoy and Satake 1995;Carey et al 1996;Mandeville et al 1996a, b;Choi et al 2003;Pelinovsky et al 2005;Maeno and Imamura 2011). This paper does not attempt to re-analyse the 1883 eruption and question the source of the tsunamis.…”

Section: Introductionmentioning

confidence: 99%