日本地球惑星科学連合2015年大会

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セッション記号 S (固体地球科学) » S-MP 岩石学・鉱物学

[S-MP09] Supercontinents and Crustal Evolution

2015年5月27日(水) 11:00 〜 12:57 201A (2F)

コンビーナ:*Madhusoodhan Satish-Kumar(Department of Geology, Faculty of Science, Niigata University)、Yasuhito Osanai(Division of Evolution of Earth Environments, Faculty of Social and Cultural Studies, Kyushu University)、Geoffrey H. Grantham(Council for Geoscience, P/Bag X112, Pretoria, SOUTH AFRICA)、Sajeev Krishnan(Centre for Earth Sciences, Indian Institute of Science, Bangalore 560 012, INDIA)、Tomokazu Hokada(National Institute of Polar Research)、座長:河上 哲生(京都大学大学院理学研究科)、外田 智千(国立極地研究所)

12:45 〜 12:48

[SMP09-P04] 南インド・チットラドゥルガ片岩帯に分布する後期太古代表成岩層序の再解釈

*三島 郁1Madhusoodhan Satish-Kumar2外田 智千3豊島 剛志2堀江 憲路3上野 雄一郎1 (1.東京工業大学、2.新潟大学、3.国立極地研究所)

キーワード:後期太古代, 南インド, 変成岩, 年代学, ジルコン, 超大陸

In order to understand late Archean tectonic and climatic systems prior to the great oxidation event, we studied volcano-sedimentary sequence of the Dharwar Supergroup, distributed in the Chitradurga Schist Belt, Western Dharwar craton. The Chitradurga schist belt consists of >3.0 Ga greenstones (Sargur Group) and overlying 2.9-2.6 Ga volcano-sedimentary sequence (Dharwar Supergroup), which are surrounded by 3.2~3.0 Ga TTG (tonalitic-trondhjemitic-granodioritic) gneiss (Chadwick et al., 2000; Jayananda et al., 2006). The Supergroup is classified into two major groups (lower Bababudan Group and upper Chitradurga Group). Preliminary studies on metamorphic conditions and geochronology of the Chitradurga Schist Belt have shown that this subdivision has to be reconsidered (Hokada et al., 2013). Therefore, we carried out a detailed lithostratigraphy, geochronology, metamorphism and tectonic evolution of the Chitradurga Schist Belt. Furthermore, it is important to compare the geological record with the other cratons for discussing any global events occurring in the late Archean. Our new field mapping and detrital zircon U-Pb dating allows us to reconstruct detailed lithostratigraphy of the Dharwar Supergroup. The lower unit consists of basal conglomerate, stromatolitic carbonate, silici-clastics with diamictite (Talya conglomerate), chert/BIFs and pillowed basalt in assending order, indicating that rift margin environment predominated at this time. The upper unit unconformably overlies the pillow lava, and consists of conglomerate/sandstone with ~ 2536 Ma detrital zircons, mafic lava, BIFs and silici-clastic sequence with mafic volcanics. The provenance analysis by detrital zircons allow us to divide the Dharwar Supergroup into the lower and upper groups. Especially, the maxima in the age distribution in the upper group (Hiriyur Formation) shows a peak at around 2.55 Ga, suggesting the source from the Eastern Dharwar Craton. Three metamorphic zones are identified in the Ingaldhal basalts. The metamorphic grade increases from lower greenschist facies to sub amphibolite facies. The boundaries between three metamorphic zones are subparallel to the bedding of interbedded BIF and tectonic contact between the lower group and upper group. On the other hand, the Hiriyur metabasalts are characterized by extensive carbonatization, whereas most samples from the lower group do not contain carbonate minerals. These differences in metamorphic grade and carbonatization of the greenstone indicate that the two groups of the Dhawrar Supergroup might preserve key information about amalgamation and/or breakup of the Dharwar protocontinent in the late Arcehan.