日本地球惑星科学連合2015年大会

講演情報

印刷

口頭発表

セッション記号 M (領域外・複数領域) » M-IS ジョイント

[M-IS35] この星は、なぜ地球なのか？ -水の役割-

2015年5月24日(日) 14:15 〜 16:00 201A (2F)

コンビーナ:*島 伸和(神戸大学大学院理学研究科惑星学専攻)、巽 好幸(海洋研究開発機構 地球内部ダイナミクス領域)、大槻 圭史(神戸大学大学院理学研究科)、中川 貴司(海洋研究開発機構数理科学・先端技術研究分野)、片山 郁夫(広島大学大学院理学研究科地球惑星システム学専攻)、藤江 剛(海洋研究開発機構)、中村 昭子(神戸大学大学院理学研究科地球惑星科学専攻)、座長:片山 郁夫(広島大学大学院理学研究科地球惑星システム学専攻)、島 伸和(神戸大学大学院理学研究科惑星学専攻)

15:45 〜 15:48

[MIS35-P01] 海底および島上MTデータに基づく東北日本弧背弧域における比抵抗モデル

ポスター講演3分口頭発表枠

*市原 寛1、多田 訓子1、馬場 聖至2、笠谷 貴史1、市來 雅啓3、海田 俊輝3、小川 康雄4 (1.海洋研究開発機構、2.東京大学地震研究所、3.東北大学噴火予知研究観測センター、4.東京工業大学火山流体研究センター)

キーワード：東北日本弧, 日本海, 背弧, マグネトテルリクス, 比抵抗構造, 地殻流体

Distribution of physical properties in the back-arc in NE Japan subduction zone have not been understood because the area is mostly located beneath the sea floor. In this study, we estimated electrical resistivity distribution in this area based on electromagnetic data obtained on the seafloor and islands in the eastern part of Japan Sea. The ocean bottom EM data were obtained with 6 ocean bottom electro-magnetometers (OBEMs) between April and August 2013 by MR13-02A and NT13-18 JAMSTEC scientific cruises. The island data were acquired in the 3 islands in the Japan Sea (Tobishima, Awashima and Sado islands) between April and October 2013. These recorded time-series data were converted to a frequency-domain impedance tensor based on the BIRRP program (Chave and Thomson, 2004). As results, high-quality MT responses and geomagnetic tippers in both the trench and back-arc areas. The phase tensor ellipses (Caldwell et al. 2004) indicates high Φmax (>65 degrees) and Φmin (>50 degrees) in the long periods (>8000 seconds) implying conductive zone in the deep area. The ellipses in the short period show strong contrast between western part (Yamato basin) and eastern part of study area, which indicate heterogeneity in crustal structure. Then we also inverted the MT impedances into resistivity distribution based on the 3-D inversion code (Tada et al., 2012) after the correction local topographic effect. The inversion result shows a significant conductor above the subducting Pacific plate. A surface conductor is also estimated beneath the Yamato Basin. These features are consistent to the phase tensors discussed above. The deep conductor may be related to dehydration in subducting Pacific Plate and convention in the mantle wedge. The surface conductor may reflect sediments rocks formed during back-arc opening in Miocene.