Earth:Kikai Caldera

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Short description: Mostly-submerged caldera in the Ōsumi Islands of Kagoshima Prefecture, Japan
Not to be confused with the island Kikaijima nor the town on it Kikai, Kagoshima
Kikai Caldera
Kikai Caldera Relief Map, SRTM, English.jpg
Highest point
PeakMount Iō (Iōjima), Iōjima, Ōsumi Islands, Japan
Elevation704 m (2,310 ft)
Coordinates [ ⚑ ] : 30°47′N 130°19′E / 30.79°N 130.31°E / 30.79; 130.31 [1]
Dimensions
Length17 km (11 mi) NS
Width20 km (12 mi) EW
Naming
Native name鬼界カルデラ  (Japanese)
Geography
CountryJapan
StateKagoshima Prefecture
RegionŌsumi Islands
DistrictKagoshima District
SubdivisionsMount Yahazu, Mount Iō (Iōjima), Mount Inamura (Iōjima), Iōjima, Shin Iōjima, Takeshima, Mount Nakasone, Mount Asase, Mount Shitakisone, Iō Tai and Takeshima Tai
MunicipalityMishima
Geology
Age of rock6,300 to 95,000 years ago

Kikai Caldera (鬼界カルデラ, Kikai karudera) (alternatively Kikaiga-shima, Kikai Caldera Complex) is a massive, mostly submerged caldera up to 19 kilometres (12 mi) in diameter in the Ōsumi Islands of Kagoshima Prefecture, Japan.[2]

Geology

The Kikai Caldera Complex has twin ovoid caldera 20 km (12 mi) by 17 km (11 mi) in diameter.[2] Yahazu-dake (north west part of Satsuma Io-jima) and Takeshima, located on the caldera rim, are pre-caldera volcanoes.[2] The pre-caldera stage of volcanic activity involved rhyolite, basalt, and andesite phases.[2][3] The earliest definitive caldera formation has been dated back to at least 140,000 years ago, resulting from the eruption of Koabiyama pyroclastic flows.[2][4][3] The formation of caldera has been associated with at least three catastrophic ignimbrite eruptions.[2][4][3] Additionally, there are two older deposits (Koseda pyroclastic flows and Anbo tephra) of large caldera-forming eruptions in the vicinity, although their attribution to the Kikai caldera remains controversial.[5][6][7]

Kikai-Koabiyama eruption

The Kikai-Koabiyama (K-Kob) pyroclastic flows are rhyolitic and are distributed across most of Takeshima and the plateau-like area on the northwest side of the caldera rim of Satsuma Iwo-Jima. They consist of numerous thin flow units and fill the basins in the basement, exhibiting significant variation in thickness. In Takeshima, the pyroclastic flows are thick, ranging from 20–100 m (66–328 ft), whereas in Iwo Jima, they are relatively thin, measuring a few to 30 m (98 ft).[2][3]

The eruption of the K-Kob pyroclastic flows has been dated using K-Ar dating to be 140000±20000 years before present.[2] While no distal tephra from this eruption has been reported, a tephra layer with potential geochemical and age correlation has been discovered in Lake Suigetsu.[8]

Kikai-Tozurahara eruption

Kikai-Tozurahara (K-Tz) tephra is a widespread rhyolitic tephra layer of Late Pleistocene age, attributed to a large VEI-7 eruption from the Kikai caldera.[9] This layer is confirmed to have a wide distribution, extending from south Kyushu to eastern Honshu and reaching the Pacific Ocean,[10] and possibly including the Shandong Peninsula.[11] The proximal equivalents of K-Tz are the Nagase pyroclastic flow and the Nishinoomote pyroclastic surges.[9][12] The combined bulk volume of both distal and proximal deposits is estimated to exceed 150 km3 (36 cu mi).[10]

In marine isotope stratigraphy (MIS), K-Tz is located between MIS 5.2 and 5.3, providing a loosely constrained preliminary eruption age of approximately 95,000 years before present.[10] More reliable age constraints were imposed by the high-resolution chronology derived from the Lake Suigetsu sediment sequence, which yielded an age of 94500±4800 years before present for this eruption.[13]

Kikai-Akahoya eruption

Impact
Kikai-Kikai-Akahoya (K-Ah) tephra and pyroclastic flow impact from Kikai-Akahoya eruption
Main page: Earth:Akahoya eruption

The caldera was the source of the Kikai-Akahoya eruption, one of the largest eruptions during the Holocene (10,000 years ago to present) that produced the Kikai-Akahoya (K-Ah) tephra.[14] Between 7,200 and 7,300 years ago,[14][15][16] pyroclastic flows producing Koya ignimbrite from that eruption reached the coast of southern Kyūshū up to 100 km (62 mi) away, and ash fell as far as Hokkaidō. The eruption produced about 150 km³ of tephra,[17] giving it a Volcanic Explosivity Index of 7[18] and making it one of the most explosive in the last 10,000 years, ranking alongside the eruptions of Santorini, Paektu, Crater Lake, Kurile Lake, Samalas and Tambora.[19]

The eruption had a major impact on the Jōmon culture in southern Kyūshū although the impact was not as great as some commentary had suggested with Nishinozono sub-type pottery tradition, that had started prior to the eruption, maintained in Kyūshū.[20]

Eruptive history since Kikai-Akahoya eruption

Kikai is still an active volcano. Io-dake(Mount Iō), Inamura-dake (south coast of Satsuma-Io-jima), Tokara-Iwo-Jima (north east coast of Satsuma-Io-jima) and Shōwa Iōjima (Shin-Io-jima) are post-caldera volcanoes within it.[2] Minor eruptions occur frequently on Mount Iō, one of the post-caldera subaerial volcanic peaks on Iōjima. Iōjima is one of three volcanic islands, two of which lie on the caldera rim. On June 4, 2013, weak tremors were recorded. Shortly after, eruptions began and continued off-and-on for several hours.[21]

Mount Iō, a rhyolite lava dome, May, 2015, viewed from the east

Eruptions occurred:[2][22]

  • old Iwo-dake stage (stage OIo-I-II)
    • phreatomagmatic eruptions and pumice fallout (stage OIo-I), followed by rhyolitic lava with continuous tephra, resulting in a volcanic edifice (stage OIo-II)
    • 3250 BCE ± 75 years (uncalibrated) Old Iwo-dake
    • 2450 BCE ± 840 years (tephrochronology) Old Iwo-dake
  • Inamura-dake stage (stage In-I-IV)
    • basaltic lava flows and scoria-cone building (stage In-I-II), then phreatomagmatic eruptions (stage In-III), and then andesitic lava (stage In-IV)
    • 1830 BCE ± 75 years (uncalibrated) Inamura-dake[17]
      • In-I tephra
    • 1090 BCE ± 100 years (uncalibrated) Inamura-dake[17]
  • young Iwo-dake stage (stage YIo-I-IV)
    • continuing with a different magma source including rhyolitic lava and intermittent pumice
    • 280 BCE ± 75 years (uncalibrated) Iwo-dake[17]
    • 390 ± 100 years (uncalibrated) Iwo-dake[17]
    • 750 (tephrochronology) Iwo-dake[17]
    • 830 ± 40 years (uncalibrated) Iwo-dake[17]
      • K-Iw-P1 tephra
    • 1010 ± 40 years (uncalibrated) Iwo-dake[17]
      • K-Sk-u-3 tephra
    • 1030 ± 40 years (uncalibrated) Iwo-dake[17]
      • K-Sk-u-4 tephra
    • 1340 ± 30 years (uncalibrated) Iwo-dake[17]
      • K-Iw-P2 tephra
    • 1430 ± 75 years (uncalibrated) Iwo-dake[17]
    • 13 Feb 1914 Tokara-Iwo-Jima[17]
    • Sep-Nov 1934
      • Submarine eruption with pumice
    • 7 Dec 1934 -Mar 1935 2 km east of Tokara-Iwo-Jima[2]
      • New island Shōwa Iōjima (Shin-Io-jima) with lava finally stabilised 19 January 1935
    • 1997-2003 Iwo-dake[2]
      • Formation and enlargement of new pit crater inside the summit crater
    • Apr-Nov 1998 Iwo-dake[2]
      • Ash
    • May-Aug 1999 Iwo-dake[2]
      • Ash
    • Jan, Mar, Oct-Dec 2000 Iwo-dake[2]
      • Ash
    • Feb, Apr-Dec 2001 Iwo-dake[2]
      • Ash
    • May-Jul 2002 Iwo-dake[2]
      • Ash
    • Feb, Apr-Oct 2003 Iwo-dake[2]
      • Ash
    • May-Apr, Jun, Aug-Oct 2004 Iwo-dake[2]
      • Ash
    • 3-5 May, 3-5 Jun 2013 Iwo-dake[2]
      • Minor eruptions
    • 2 Nov 2019 Iwo-dake[2]
      • Minor eruption
    • 29 Apr 2020 Iwo-dake[2]
      • Minor eruption
    • 6 Oct 2020 Iwo-dake[2]
      • Minor eruption

See also

  • List of volcanoes in Japan

Further reading

References

  1. ↑ "Kikai | Volcano World | Oregon State University" (in en). 24 April 2011. http://volcano.oregonstate.edu/kikai. 
  2. ↑ 2.00 2.01 2.02 2.03 2.04 2.05 2.06 2.07 2.08 2.09 2.10 2.11 2.12 2.13 2.14 2.15 2.16 2.17 2.18 2.19 2.20 2.21 2.22 "噴火史 - Iwojima". https://gbank.gsj.jp/volcano/Act_Vol/satsumaioujima/vr/doc/012.html. 
  3. ↑ 3.0 3.1 3.2 3.3 小野, 晃司; 曽屋, 龍典; 細野, 武男 (1982) (in ja). 薩摩硫黄島地域の地質. 地質調査所. https://ci.nii.ac.jp/ncid/BA36838038. 
  4. ↑ 4.0 4.1 Nishino, Y., Takarada, S. and Geshi, N. (2019) Volcanic activities and eruption sequence of the large-scale eruption at Aira, Kikai, Ata, Kutcharo, Towada, Mashu and Ikeda Volcanoes. Open-File Report of the Geological Survey of Japan, AIST, no.680, p. 1-126.
  5. ↑ Ito, Hisatoshi; Uesawa, Shimpei; Nanayama, Futoshi; Nakagawa, Shojiro (2017-05-15). "Zircon U–Pb dating using LA-ICP-MS: Quaternary tephras in Yakushima Island, Japan" (in en). Journal of Volcanology and Geothermal Research 338: 92–100. doi:10.1016/j.jvolgeores.2017.02.003. https://linkinghub.elsevier.com/retrieve/pii/S0377027316303079. 
  6. ↑ Moriwaki, Hiroshi; Westgate, John A.; Sandhu, Amanjit S.; Preece, Shari J.; Arai, Fusao (2008-02-01). "New glass fission-track ages of Middle Pleistocene tephras on Yakushima Island, southern Japan" (in en). Quaternary International. Global Tephra Studies: John Westgate and Andrei Sarna-Wojcicki Commemorative Volume 178 (1): 128–137. doi:10.1016/j.quaint.2006.11.013. ISSN 1040-6182. https://www.sciencedirect.com/science/article/pii/S1040618206002874. 
  7. ↑ 久敏, 伊藤; 真平, 上澤 (2017). "鬼界カルデラにおける鬼界アカホヤ噴火以前の大噴火について". 日本地質学会学術大会講演要旨 2017: 023. doi:10.14863/geosocabst.2017.0_023. https://www.jstage.jst.go.jp/article/geosocabst/2017/0/2017_023/_article/-char/ja/. 
  8. ↑ Maruyama, Seiji; Takemura, Keiji; Hirata, Takafumi; Yamashita, Tohru; Danhara, Tohru (2019-08-11). "Major and trace element abundances in volcanic glass shards in visible tephras in SG93 and SG06 drillcore samples from Lake Suigetsu, central Japan, obtained using femtosecond LA–ICP–MS". Journal of Quaternary Science 35 (1-2): 66–80. doi:10.1002/jqs.3124. ISSN 0267-8179. http://dx.doi.org/10.1002/jqs.3124. 
  9. ↑ 9.0 9.1 洋, 町田; 房夫, 新井 (1983). "101. 鬼界カルデラ起源の新広域テフラと九州における更新世後期大火砕流の噴出年代(日本火山学会 1983 年度春季大会講演要旨)". 火山.第２集 28 (2): 206. doi:10.18940/kazanc.28.2_206_2. https://www.jstage.jst.go.jp/article/kazanc/28/2/28_KJ00003453684/_article/-char/ja/. 
  10. ↑ 10.0 10.1 10.2 Machida, Hiroshi (1999). "The stratigraphy, chronology and distribution of distal marker-tephras in and around Japan" (in en). Global and Planetary Change 21 (1-3): 71–94. doi:10.1016/S0921-8181(99)00008-9. https://linkinghub.elsevier.com/retrieve/pii/S0921818199000089. 
  11. ↑ Eden, Dennis N.; Froggatt, Paul C.; Zheng, Honghan; Machida, Hiroshi (1996-01-01). "Volcanic glass found in Late Quaternary Chinese loess: A pointer for future studies?" (in en). Quaternary International 34-36: 107–111. doi:10.1016/1040-6182(95)00074-7. ISSN 1040-6182. https://www.sciencedirect.com/science/article/pii/1040618295000747. 
  12. ↑ 信治, 長岡 (1988). "最終間氷期末に起きた鬼界カルデラの珪長質火砕流噴火と火砕サージの形成". 地學雜誌 97 (3): 156–169. doi:10.5026/jgeography.97.3_156. https://www.jstage.jst.go.jp/article/jgeography1889/97/3/97_3_156/_article/-char/ja/. 
  13. ↑ Albert, Paul G.; Smith, Victoria C.; Suzuki, Takehiko; McLean, Danielle; Tomlinson, Emma L.; Miyabuchi, Yasuo; Kitaba, Ikuko; Mark, Darren F. et al. (2019). "Geochemical characterisation of the Late Quaternary widespread Japanese tephrostratigraphic markers and correlations to the Lake Suigetsu sedimentary archive (SG06 core)" (in en). Quaternary Geochronology 52: 103–131. doi:10.1016/j.quageo.2019.01.005. https://linkinghub.elsevier.com/retrieve/pii/S1871101418300967. 
  14. ↑ 14.0 14.1 Tsuji, Tomohiro; Ikeda, Michiharu; Furusawa, Akira; Nakamura, Chisato; Ichikawa, Kiyoshi; Yanagida, Makoto; Nishizaka, Naoki; Ohnishi, Kozo et al. (2018). "High resolution record of Quaternary explosive volcanism recorded in fluvio-lacustrine sediments of the Uwa basin, southwest Japan". Quaternary International 471: 278–297. doi:10.1016/j.quaint.2017.10.016. ISSN 1040-6182. https://www.sciencedirect.com/science/article/pii/S1040618216316081. 
  15. ↑ 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. https://www.jstage.jst.go.jp/article/geosoc/125/1/125_2018.0069/_article/-char/en. 
  16. ↑ 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. doi:10.1016/j.quascirev.2013.01.026. ISSN 0277-3791. https://www.sciencedirect.com/science/article/pii/S0277379113000413. 
  17. ↑ 17.00 17.01 17.02 17.03 17.04 17.05 17.06 17.07 17.08 17.09 17.10 17.11 17.12 17.13 Kikai – Eruptive history, Global Volcanism Program. Smithsonian Institution.
  18. ↑ Johnston, Eric, "Latest volcano show: Shinmoe", The Japan Times, 1 March 2011, p. 3.
  19. ↑ "Large Volcano Explocivity Index". Countries of the World. http://www.allcountries.org/ranks/volcano_explocivity_index_ranks.html. 
  20. ↑ Junzo, Uchiyama (2021). "After a Super Volcanic Eruption: a new project on social-ecological impacts of the Kikai-Akahoya disaster, 7,300 years ago". https://www.sainsbury-institute.org/e-bulletin/april-2021/after-a-super-volcanic-eruption-a-new-project-on-social-ecological-impacts-of-the-kikai-akahoya-disaster-7300-years-ago/. 
  21. ↑ "Global Volcanism Program | Kikai" (in en). https://volcano.si.edu/volcano.cfm?vn=282060. 
  22. ↑ Maeno, Fukashi; Taniguchi, Hiromitsu (2005-05-20). "Eruptive History of Satsuma Iwo-jima Island, Kikai Caldera, after a 6.5 ka Caldera-forming Eruption". 火山 (Volcano) 50: 71–85. doi:10.18940/kazan.50.2_71. https://www.jstage.jst.go.jp/article/kazan/50/2/50_KJ00003562590/_article/-char/ja/. 

External links



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