Wikipedia

Akahoya eruption

The Akahoya eruption or Kikai-Akahoya eruption was the strongest known volcanic eruption of the Kikai Caldera in Kyūshū, Japan. It ejected 332–457 km3 (80–110 cu mi) of volcanic material, giving it a Volcanic Explosivity Index of 7.

Akahoya eruption
VolcanoKikai Caldera
Date6,860 to 7,440 years calibrated before present[1]
TypeUltra-Plinian
LocationKyūshū, Japan
30°47′20″N 130°18′29″E / 30.789°N 130.308°E / 30.789; 130.308
Volume332–457 km3 (80–110 cu mi)[2]
VEI7[3]
ImpactOne of only six confirmed eruptions of its size in the Holocene; dramatically changed vegetation in Southern Kyūshū and impacted on the Jōmon culture
Affected areas of the eruption

Context

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The Kikai Caldera had erupted about 94,000 years before in the smaller Nagase eruption and that was preceded about 140,000 years ago by the Koabiyama eruption.[4][5][6]: 100 

Eruption sequence

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There is evidence of volcanic activity at the Kikai Caldera in what is termed the K–Km tephra layers between 16–9 cal ka BP.[7]: 336  The Takeshima debris avalanche followed by the Nagahama lava (NgL) and Heikejo ash (K–Hj) events preceded the eruption.[7]: 336  The eruption proper then started with a Plinian eruption of VEI-6 (K–KyP), which ejected the Koya (Funakura) pumice fall. The sequence from then on lasted at least 28 hours.[8]: 235  In the latter half of this Plinian eruption, the plume collapsed and an intra-plinian flow, Funakura pyroclastic flow (K–Fn), occurred.[7]: 336  The total volume of K-KyP and K-Fn is estimated to be 40 km3 (9.6 cu mi).[8]: 212  This was quickly followed by the ultimate caldera forming Akahoya Phreatoplinian eruption of VEI-7. This eruption was caused by the contact between magma and seawater, forming a huge plume. The Koya (Takeshima) Pyroclastic Flow occurred as a large-scale pyroclastic flow depositing ignimbrite (K–Ky), and the Kikai-Akahoya Volcanic Ash (K–Ah) as a widespread tephra covered Honshū, Okinawa, and the Southern Korean Peninsula.[7]: 336  As a result of this eruption, a double caldera with a diameter of 20 km × 17 km (12 mi × 11 mi) was formed at Kikai Volcano.[6]: 99 [9]

After the Funakura Pyroclastic Flow, a large earthquake (Ah1) occurred near the Kikai Caldera before the Koya Pyroclastic Flow occurred. Soil liquefaction occurred on Yakushima and Tanegashima due to the large shaking.[10]: 299 [7]: 336  Furthermore, a second large earthquake (Ah2) occurred while the Kikai-Akahoya Volcanic Ash was falling, and soil liquefaction occurred on the Satsuma Peninsula and Ōsumi Peninsula.[10]: 299  [7]: 336 

A megatsunami occurred either at the very end of the eruption or shortly thereafter. Tsunami deposits were formed over a wide area along the coast of Western Japan, certainly up to 300 km (190 mi) away where some Kikai-Akahoya tephra was deposited after the tsunami which was not the case closer to the eruption.[7]: 335  The cause of the tsunami is not well understood, but one possibility given the timings would be collapse of the caldera rim.[7]: 335 

Deposits

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The total bulk volume of the eruption is now estimated at 133–183 km3 (32–44 cu mi) DRE, about double previous estimates, noting that the headline volume estimates at 332–457 km3 (80–110 cu mi) relate to lighter deposits such as pumice fall,[8]: 235  than typical for lava that is used in DRE calculations.[2] The eruption was partially submarine and a fuller understanding of its character required the realisation that part of the pyroclastic density current had been transformed into a subaqueous density current that contributed to a total seafloor deposit volume of 71 km3 (17 cu mi).[2] The caldera bottom itself is at a depth between 300–500 m (980–1,640 ft) under the sea,[6]: 99  and most of the land deposits that are easier to study commence from about 40 km (25 mi) from the caldera.[7]: 337  The depth of some of the eruption is important as seafloor-hugging density currents are not described in shallow underwater settings.[2] Ignimbrite deposits on land exist with a volume of 5 km3 (1.2 cu mi) and the widespread tephra which is now known to cover an area of 4,500 km2 (1,700 sq mi) have a volume of 249–374 km3 (60–90 cu mi).[2] The main climactic ignimbrite is largely dry so not all the main eruption happened from vents that remained underwater or were underwater.[8]: 234  Previous studies of mainly land based tephra deposits had led to uncorrected volume estimates of 150 km3 (36 cu mi)[6]: 105  later increased to 170 km3 (41 cu mi)[11] These were later analysed to give dense rock equivalents so the Koya (Takeshima) Pyroclastic Flow (K–Ky) with its estimated total volume in three phrases of 30–45 km3 (7.2–10.8 cu mi) was assigned a DRE volume of 15–25 km3 (3.6–6.0 cu mi). The Kikai-Akahoya Volcanic Ash (K–Ah) with a volume of 100 km3 (24 cu mi) gave a DRE volume of 50 km3 (12 cu mi).[8]: 224  Until the presence of a subaqueous density current was understood a VRE of 7.2 had been estimated,[1] with a total DRE volume of 70–80 km3 (17–19 cu mi)[8]: 234  Sea level would have been lower than present at the time of the eruption but would have reached present levels within a thousand years.[8]: 215  The magma chamber that feed the majority of the eruption is estimated to be 3–7 km (1.9–4.3 mi) below the surface.[8]: 234 

Retrospective dating

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Archaeologically it has been dated around 7,300 cal. BP during the earliest stage of the Jōmon period,[12] but it had also been uncorrected radiocarbon dated to as recently as 6,500 BP.[13] The current accepted dating adjustment from multiple other sources is about 7,200 to 7,300 years ago.[14][15][1]

Aftermath

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This eruption has been linked to the end of the initial Jōmon culture in southern Kyūshū although impact, although marked, was not as great as some commentary had suggested with Nishinozono sub-type pottery tradition, that had started prior maintained throughout and after the eruption sequence in Kyūshū.[16] It took nearly 1000 years to recover.[17] Jōmon who lived further away survived such as on northern Kyūshū, Honshū and Hokkaidō but likely had to revert for a period to maritime food sources mainly.[16]

The fate of the initial Jōmon culture on south Kyūshū does not quite parallel the demise of the Minoan civilization, which may have ended as a consequence of another massive volcanic eruption.

These events give more credence to cultural traditions that maintain stories of established cultures vanishing quickly and completely. However while the demises happened in (Holocene) human history, in two very different parts of the world, the time scales of both were more gradual than some work suggests, allowing alternative suggestions as to all the mechanisms involved.[18] The associated issues have resulted in deeper study into the effects of volcanic activity on both human cultural development and social perception of volcanic risk.[19]

References

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  1. ^ a b c Smith, Victoria C.; Staff, Richard A.; Blockley, Simon P.E.; Ramsey, Christopher Bronk; Nakagawa, Takeshi; Mark, Darren F.; Takemura, Keiji; Danhara, Toru (2013). "Identification and correlation of visible tephras in the Lake Suigetsu SG06 sedimentary archive, Japan: chronostratigraphic markers for synchronising of east Asian/west Pacific palaeoclimatic records across the last 150 ka". Quaternary Science Reviews. 67: 121–137. Bibcode:2013QSRv...67..121S. doi:10.1016/j.quascirev.2013.01.026. ISSN 0277-3791.
  2. ^ a b c d e Satoshi Shimizu; Reina Nakaoka; Nobukazu Seama; Keiko Suzuki-Kamata; Katsuya Kaneko; Koji Kiyosugi; Hikaru Iwamaru; Mamoru Sano; Tetsuo Matsuno; Hiroko Sugioka; Yoshiyuki Tatsumi (2024). "Submarine pyroclastic deposits from 7.3 ka caldera-forming Kikai-Akahoya eruption". Journal of Volcanology and Geothermal Research. 448 (108017). Bibcode:2024JVGR..44808017S. doi:10.1016/j.jvolgeores.2024.108017.
  3. ^ "Kikai: Eruptive History". Global Volcanism Program. Smithsonian Institution. Retrieved 2024-02-26.
  4. ^ Machida, Hiroshi (1999). "The stratigraphy, chronology and distribution of distal marker-tephras in and around Japan". Global and Planetary Change. 21 (1–3): 71–94. Bibcode:1999GPC....21...71M. doi:10.1016/S0921-8181(99)00008-9.
  5. ^ "噴火史 - Iwojima". gbank.gsj.jp. Retrieved 2023-05-25.
  6. ^ a b c d Ngaoka, Shinji (1988). "The late quaternary tephra layers from the caldera volcanoes in and around Kagoshima bay, southern Kyushu, Japan". Geographical Reports of Tokyo Metropolitan University. 23: 49–122. Retrieved 26 February 2024.
  7. ^ a b c d e f g h i Kobayashi, Tetsuo (2022). "Overall View of the Akahoya Tsunami After the 7.3 cal ka BP Kikai Caldera-Forming Eruption". Bulletin of the Volcanological Society of Japan (火山) (in Japanese). 67 (3): 335–350. doi:10.18940/kazan.67.3_335.
  8. ^ a b c d e f g h Maeno, F.; Taniguchi, H. (2007). "Spatiotemporal evolution of a marine caldera-forming eruption, generating a low-aspect ratio pyroclastic flow, 7.3 ka, Kikai caldera, Japan: Implication from near-vent eruptive deposits" (PDF). Journal of Volcanology and Geothermal Research. 167 (1–4): 212–238. Bibcode:2007JVGR..167..212M. doi:10.1016/j.jvolgeores.2007.05.003. ISSN 0377-0273. Retrieved 26 February 2024.
  9. ^ "Large-volume Eruption Database Version 1.0.10" (in Japanese). Geological Survey of Japan. 2024.
  10. ^ a b Naruo, Hideto; Kobayashi, Tetsuo (2002). "Two Large-scale Earthquakes Triggered by a 6.5ka BP Eruption from Kikai Caldera, Southern Kyushu, Japan". The Quaternary Research (Daiyonki-Kenkyu) (in Japanese). 41 (4): 287–299. doi:10.4116/jaqua.41.287.
  11. ^ 町田洋; 新井房夫 (2003). 新編火山灰アトラス - 日本列島とその周辺 (in Japanese). University of Tokyo Press. ISBN 978-4-13-060745-2.
  12. ^ Kuwahata, Mitsuhiro (2002). "Age and cultural influence of the Kikai-Akahoya eruption as seen from archaeological material in south Kyūshū, Japan". Quaternary Research. 41 (4): 317–330. doi:10.4116/jaqua.41.317. ISSN 0418-2642.
  13. ^ Maeno, Fukashi; Taniguchi, Hiromitsu (2005). "Eruptive history of Satsuma Iwo-jima Island, Kikai caldera, after a 6.5 ka caldera-forming eruption". Bulletin of the Volcanological Society of Japan. 50 (2): 71–85. ISSN 0453-4360.
  14. ^ Okuno, Mitsuru (2019-04-15). "Chronological study on widespread tephra and volcanic stratigraphy of the past 100,000 years". The Journal of the Geological Society of Japan. 125 (1): 41–53. doi:10.5575/geosoc.2018.0069. ISSN 1349-9963.
  15. ^ Tsuji, Tomohiro; Ikeda, Michiharu; Furusawa, Akira; Nakamura, Chisato; Ichikawa, Kiyoshi; Yanagida, Makoto; Nishizaka, Naoki; Ohnishi, Kozo; Ohno, Yuki (2018). "High resolution record of Quaternary explosive volcanism recorded in fluvio-lacustrine sediments of the Uwa basin, southwest Japan". Quaternary International. 471: 278–297. Bibcode:2018QuInt.471..278T. doi:10.1016/j.quaint.2017.10.016. ISSN 1040-6182.
  16. ^ a b Junzo, Uchiyama (2021). "After a Super Volcanic Eruption: a new project on social-ecological impacts of the Kikai-Akahoya disaster, 7,300 years ago". Retrieved 2022-09-18.
  17. ^ "巨大カルデラ噴火のメカニズムとリスクを発表" [Announcement of the mechanism and risks of a massive caldera eruptions] (Press release). Kobe University. 22 October 2014. Archived from the original on 30 March 2019. Retrieved 31 March 2019.
  18. ^ Tsonis, AA; Swanson, KL; Sugihara, G; Tsonis, PA (24 August 2010). "Climate change and the demise of Minoan civilization". Climate of the Past. 6 (4): 525–30. Bibcode:2010CliPa...6..525T. doi:10.5194/cp-6-525-2010.
  19. ^ Donovan, A; Eiser, JR; Sparks, RS (2014). "Scientists' views about lay perceptions of volcanic hazard and risk". Journal of Applied Volcanology. 3 (1): 1–14. Bibcode:2014JApV....3...15D. doi:10.1186/s13617-014-0015-5.
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