Japan Geoscience Union Meeting 2018

Presentation information

[EE] Oral

S (Solid Earth Sciences) » S-MP Mineralogy & Petrology

[S-MP35] Antarctica and surrounds in Supercontinent Evolution

Tue. May 22, 2018 10:45 AM - 12:15 PM 302 (3F International Conference Hall, Makuhari Messe)

convener:Tomokazu Hokada(National Institute of Polar Research), Yasuhito Osanai(Division of Evolution of Earth Environments, Faculty of Social and Cultural Studies, Kyushu University), Geoffrey Hugo Grantham (共同), Madhusoodhan Satish-Kumar(Department of Geology, Faculty of Science, Niigata University), Chairperson:Hokada Tomokazu(National Institute of Polar Research), Grantham Geoffrey(University of Johannesburg)

11:15 AM - 11:30 AM

[SMP35-08] Protolith characteristics and tectonic implications for high-grade metamorphic rocks in the Highland and Wanni Complexes, Sri Lanka.

*Ippei Kitano1, Yasuhito Osanai1, Nobuhiko Nakano1, Tatsuro Adachi1 (1.Division of Earth Sciences, Faculty of Social and Cultural Studies, Kyushu University)

Keywords:protolith characteristics, tectonic implication, Highland Complex, Wanni Complex, Sri Lanka, Gondwana supercontinent

Sri Lanka has been considered to locate inside the collision zone during amalgamation of Gondwana supercontinent (e.g. Meert, 2003). Therefore, Sri Lanka plays an important role to elucidate the process of amalgamation of the Gondwana supercontinent. On the basis of rock type, metamorphic grade and Nd model ages, the metamorphic rocks in Sri Lanka are subdivided into three major crustal units (e.g. Cooray, 1994), which are Wanni Complex (WC), Highland Complex (HC) and Vijayan Complex (VC). This study conducted whole rock chemistry and LA-ICP-MS zircon U–Pb ages from 45 metamorphic rocks in the Highland and Wanni Complexes, and discuss their origin and tectonic models.
The bulk chemical analyses indicated sedimentary affinities for 17 samples and igneous affinities for 28 samples as protolith types. The metasedimentary rocks are characterized by relatively sandy, felsic compositions from the HC and relatively muddy, mafic compositions from the WC. The metaigneous rocks from both complexes are mainly characterized by the volcanic arc affinities. The zircon dating results provided dominant detrital zircon ages of ca. 3500–1500 Ma and igneous protolith ages of ca. 2000–1800 Ma in the east and dominate detrital zircon ages of ca. 1100–700 Ma and igneous protolith ages of ca. 1100–800 Ma in the west. The systematic differences of inherited zircon ages suggest eastern and western areas correspond to the HC and WC, respectively. Additionally, metamorphic ages of ca. 650–500 Ma are widely recognized from the HC and WC. The geochemical and geochronological characteristics of these complexes gave their tectonic implications for the protolith formation as the continental arc at the margin of old continental crust. The provenances of detrital zircons in the HC may be a mixture of detritus from local arc igneous rocks (2000–1800 Ma) and Paleoproterozoic to Archean craton, while those in the WC may consist of the detritus come from mainly arc igneous basements (1100–800 Ma), minor metamorphic rocks (1000–800 Ma) and old craton (2500–1500 Ma). However, before the assembly of these complexes precursors, that of the HC might have had a passive tectonic setting after its arc magmatism at ca. 2000–1800 Ma, and subsequently started to approach that of the Wanni Complex during subduction-related arc magmatism at ca. 1100 Ma, maybe as a part of continent. Moreover, the protolith characteristics, P-T evolutions and oldest ages of metamorphic zircons/monazites (ca. 650–620 Ma) are similar among southern India (Trivandrum Block, Achankovil Shear Zone and Southern Madurai Block), the HC and WC and Lützow-Holm Complex (Skallen Group, Ongul Group and Okuiwa Group). It suggests possibly that the protoliths (continent) of the Trivandrum Block, HC and a part of Skallen Group had collided together with continental arcs of Achankovil Shear Zone and Southern Madurai Block, WC, Ongul and Okuiwa Groups (except Cape Hinode) precursors at ca. 650–620 Ma.