Editing Kikai Caldera (section)

===Kikai-Tozurahara eruption===
Kikai-Tozurahara (K-Tz) [[tephra]] is a widespread rhyolitic tephra layer of [[Late Pleistocene]] age, attributed to a large [[Volcanic explosivity index|VEI]]-7 eruption from the Kikai caldera.<ref name=":0">{{Cite journal |last1=洋 |first1=町田 |last2=房夫 |first2=新井 |date=1983 |title=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) |url=https://www.jstage.jst.go.jp/article/kazanc/28/2/28_KJ00003453684/_article/-char/ja/ |journal=火山.第２集 |volume=28 |issue=2 |pages=206 |doi=10.18940/kazanc.28.2_206_2}}</ref> This layer is confirmed to have a wide distribution, extending from south [[Kyushu]] to eastern [[Honshu]] and reaching the [[Pacific Ocean]],<ref name=":1">{{Cite journal |last=Machida |first=Hiroshi |date=1999 |title=The stratigraphy, chronology and distribution of distal marker-tephras in and around Japan |url=https://linkinghub.elsevier.com/retrieve/pii/S0921818199000089 |journal=Global and Planetary Change |language=en |volume=21 |issue=1–3 |pages=71–94 |doi=10.1016/S0921-8181(99)00008-9|bibcode=1999GPC....21...71M |url-access=subscription }}</ref> and possibly including the [[Shandong Peninsula]].<ref>{{Cite journal |last1=Eden |first1=Dennis N. |last2=Froggatt |first2=Paul C. |last3=Zheng |first3=Honghan |last4=Machida |first4=Hiroshi |date=1996-01-01 |title=Volcanic glass found in Late Quaternary Chinese loess: A pointer for future studies? |url=https://dx.doi.org/10.1016/1040-6182%2895%2900074-7 |journal=Quaternary International |language=en |volume=34-36 |pages=107–111 |doi=10.1016/1040-6182(95)00074-7 |bibcode=1996QuInt..34..107E |issn=1040-6182|url-access=subscription }}</ref> The proximal equivalents of K-Tz are the Nagase [[pyroclastic flow]] and the Nishinoomote [[pyroclastic surge]]s.<ref name=":0" /><ref>{{Cite journal |last=信治 |first=長岡 |date=1988 |title=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 |url=https://www.jstage.jst.go.jp/article/jgeography1889/97/3/97_3_156/_article/-char/ja/ |journal=地學雜誌 |volume=97 |issue=3 |pages=156–169 |doi=10.5026/jgeography.97.3_156|doi-access=free }}</ref> The combined bulk volume of both distal and proximal deposits is estimated to exceed {{Convert|150|km3|mi3|abbr=on}}.<ref name=":1" />

In [[Marine isotope stages|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.<ref name=":1" /> More reliable age constraints were imposed by the high-resolution chronology derived from the Lake Suigetsu sediment sequence, which yielded an age of {{Val|94500|4800|fmt=commas}} years before present for this eruption.<ref>{{Cite journal |last1=Albert |first1=Paul G. |last2=Smith |first2=Victoria C. |last3=Suzuki |first3=Takehiko |last4=McLean |first4=Danielle |last5=Tomlinson |first5=Emma L. |last6=Miyabuchi |first6=Yasuo |last7=Kitaba |first7=Ikuko |last8=Mark |first8=Darren F. |last9=Moriwaki |first9=Hiroshi |last10=Nakagawa |first10=Takeshi |date=2019 |title=Geochemical characterisation of the Late Quaternary widespread Japanese tephrostratigraphic markers and correlations to the Lake Suigetsu sedimentary archive (SG06 core) |url=https://linkinghub.elsevier.com/retrieve/pii/S1871101418300967 |journal=Quaternary Geochronology |language=en |volume=52 |pages=103–131 |doi=10.1016/j.quageo.2019.01.005|bibcode=2019QuGeo..52..103A |hdl=2262/93449 |s2cid=134899116 |hdl-access=free }}</ref>