![]() Hamphill's, Austin, pp 1–70įrancis P (1985) The origin of the 1883 Krakatau tsunamis. Geol Soc Am Bull 192:1038–1054įolk RL (1968) Petrology of sedimentary rocks. Bull Volcanol 54:156–167įisher RV (1990) Transport and deposition of a pyroclastic surge across an area of high relief: the eruption of Mount St. Nature 310:679–681įierstein J, Nathanson M (1992) Another look at the calculation of fallout tephra volumes. ![]() ![]() Bull Volcanol 54:554–572ĭruitt TH, Sparks RSJ (1984) On the formation of calderas during ignimbrite formation. ![]() Sci Tsunami Hazards 9:73–82ĭruitt TH (1992) Emplacement of the lateral blast deposit ENE of Mount St. J Archaeol Sci 17:509–512ĭawson AG, Foster I, Shi S, Smith DE, Long D (1991) The identification of tsunami deposits in coastal sediment sequences. Bull Volcanol 53:357–380ĭawson AG, Smith DE, Long D (1990) Evidence for a tsunami from a mesolithic site in Inverness, Scotland. J Geophys Res 93:15314–15328Ĭas R, Wright JV (1991) Subaqueous pyroclastic flows and ignimbrites: an assessment. J Volcanol Geotherm Res 19:167–173Ĭarey SN, Sigurdsson H, Sparks RSJ (1988) The fluid dynamic behavior of particle-laden plumes. Indones Instit Sci United Nation Univ, pp 54–75Ĭamus G, Vincent P (1983) Discussion of a new hypothesis for the Krakatau volcanic eruption in 1883. In: Bird E, Soegiarto A, Soegiarto K (eds) Proceedings of Workshop on coastal resources management of Krakatau and the Sunda Strait region, Indonesia. Bull Volcanol 52:532–544īirowo S, Uktolseja H (1983) Oceanographic features of Sunda Strait. Bull Volcanol 41 (1):10–31īaxter PJ (1990) Medical effects of volcanic eruptions I. The buoyant distal edge of these ash-and steam-laden clouds lifted off into the atmosphere, leading to cooling, condensation, and mud rain.īarberi F, Innocenti F, Liser L, Munno R, Pescatore T, Santacroce R (1978) The Campanian ignimbrite: a major prehistoric eruption in the Neapolitan area. It is proposed that the generation of steam at the flow/seawater interface may have led to a reduction in the sedimentation of particles and consequently a delay in the time before the flows ceased lateral motion and became buoyantly convective. activity may be the result of enhanced runout over the sea. The great mobility of the Krakatau flows from the 10 a.m. At the distal edge of this area the flows were relatively dilute and turbulent, yet carried enough material to deposit several tens of centimeters of tephra. Historical accounts from ships in the Sunda Straits constrain the area affected by the flows to a minimum of 4x10 3 km 2. The flows retained temperatures high enough to burn victims on the SW coast of Sumatra. Energetic flows spread out away from the volcano at speeds in excess of 100 km/h and traveled up to 80 km from source. The deposits are correlated to a major pyroclastic flow phase that occurred on the morning of 27 August at approximately 10 a.m. Crystal fractionation is consistent with the distal facies being derived from the upper part of gravitationally segregated pyroclastic flows in which the relative amount of crystal enrichment and abundance of dense lithic clasts diminished upwards. The distal deposits exhibit a decrease in sorting coefficient, median grain size, and thickness with increasing distance from Krakatau. Granulometric and lithologic characteristics of the deposits indicate that they represent the complement of proximal subaerial and submarine pyroclastic flow deposits laid down on and close to the Krakatau islands. Massive and poorly stratified units formed predominantly from pyroclastic flows and surges that traveled over the sea for distances up to 80 km. Pyroclastic deposits from the 1883 eruption of Krakatau are described from areas northeast of the volcano on the islands of Sebesi, Sebuku, and Lagoendi, and the southeast coast of Sumatra.
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