Japan Geoscience Union Meeting 2016

Presentation information

International Session (Oral)

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

[S-MP14] Supercontinents and Crustal Evolution

Tue. May 24, 2016 1:45 PM - 3:15 PM A07 (APA HOTEL&RESORT TOKYO BAY MAKUHARI)

Convener:*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), Grantham Grantham(Geology Department, University of Johannesburg, South Africa.), Krishnan Sajeev(Centre for Earth Sciences, Indian Institute of Science), Tomokazu Hokada(National Institute of Polar Research), Chair:Madhusoodhan Satish-Kumar(Department of Geology, Faculty of Science, Niigata University), Krishnan Sajeev(Centre for Earth Sciences, Indian Institute of Science)

2:15 PM - 2:30 PM

[SMP14-03] The growth history of continents delineated by compilation of detrital zircon ages

*Hikaru Sawada1, Shigenori Maruyama2, Yukio Isozaki3, Shuhei Sakata3, Takafumi Hirata4 (1.Department of Earth and Planetary Sciences, Tokyo Institute of Technology, 2.Earth-Life Science Institute, Tokyo Institute of Technology, 3.Department of Earth Science and Astronomy, The University of Tokyo, 4.Division of Earth and Planetary Sciences, Kyoto University)

Keywords:continental growth, detrital zircon, U-Pb age, embryonic continent

The current understanding on the growth history of continents needs a major revision in view of granitoid recycling into the mantle. At present, Archean continental crusts occupy less than 20 % in area of the modern continents; on the other hand, various previous studies on geochemistry and thermal evolution suggest active production of the continental crust since the Hadean. Production of the continental crust and the growth of the continents in large-term should be differentiated. In order to reconstruct the secular change in continental growth from ca. 3 Ga (Meso-Archean) to the present, we conducted global compilation of detrital zircon U-Pb ages from sandstones of various depositional age in the world. Using this database, the growth patterns of continents, at the timing of ca. 2.9, 2.6, 2.3, 1,0 and 0.6 Ga, are estimated for each continent first, then overall picture was reconstructed, as follows. Before ca. 2.3 Ga (Archean and Paleoproterozoic), the production and recycling of the continental crust were likely relatively short-cycled, and the net continental growth was probably slow. The short cycle was likely driven by the numerous formation of small-sized embryonic continents, much smaller than modern ones, and by the more ubiquitous subduction. From ca. 2.3 Ga to 1.0 Ga, the average size of continent became larger, comparable to the modern ones. Especially after ca. 1.8 Ga formation of the continent Nuna, more efficient continental growth started by the accretion of island arcs to continental margins. Since ca. 1.0 Ga, the breakup of the supercontinent Rodinia, the total volume of the continental crust likely has decreased according to the more effective recycling of relatively young continental crust.