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    东北印度洋区BAR9427岩心末次冰期以来的古季风活动记录

    丁旋 方念乔

    丁旋, 方念乔, 2006. 东北印度洋区BAR9427岩心末次冰期以来的古季风活动记录. 地球科学, 31(6): 765-772.
    引用本文: 丁旋, 方念乔, 2006. 东北印度洋区BAR9427岩心末次冰期以来的古季风活动记录. 地球科学, 31(6): 765-772.
    DING Xuan, FANG Nian-qiao, 2006. Records of Paleo-Monsoon of Core BAR9427 in Northeastern Indian Ocean during Last Glaciation. Earth Science, 31(6): 765-772.
    Citation: DING Xuan, FANG Nian-qiao, 2006. Records of Paleo-Monsoon of Core BAR9427 in Northeastern Indian Ocean during Last Glaciation. Earth Science, 31(6): 765-772.

    东北印度洋区BAR9427岩心末次冰期以来的古季风活动记录

    基金项目: 

    国家自然科学基金项目 40476022

    详细信息
      作者简介:

      丁旋(1964—), 女, 博士, 副教授, 主要从事古海洋学和微体古生物学研究. E-mail:dingx@cugb.edu.cn

    • 中图分类号: P532

    Records of Paleo-Monsoon of Core BAR9427 in Northeastern Indian Ocean during Last Glaciation

    • 摘要: 末次冰期旋回尤其是氧同位素3期气候明显不稳定, 南亚季风活动并不遵循冰期间冰期的规律.通过东北印度洋区位于安达曼海南部、苏门答腊岛西北端格雷特海峡的BAR9427岩心的古海洋学研究, 并与相邻孟加拉湾地区的MD77181和MD81349二支岩心进行对比分析, 认识到末次冰期氧同位素2期时, 研究区东北冬季风增强, 上升流活跃, 古生产力较高, 同时近岸地区蒸发作用强烈, 海水盐度升高.末次冰期大间冰阶氧同位素3期的早、晚期, 研究区西南夏季风活动强烈, 向东的西南季风流, 使得孟加拉湾中部盐度升高, 而北部由于季风降雨, 大量的淡水输入使得盐度大幅度下降, 且八月盐度远低于二月.西南夏季风变化遵循23ka的岁差周期, 在我国青藏高原、黄土与沙漠以及阿拉伯海等区都有表现.

       

    • 图  1  现代印度洋表层海水盐度分布(Cullen, 1981)

      a.西南季风时期(5—10月); b.东北季风时期(11—4月); ☆指示岩心位置图; 盐度等值线单位‰

      Fig.  1.  Surface salinity patterns in the northern Indian Ocean

      图  2  BAR9427岩心氧碳稳定同位素, 表层水温和盐度变化曲线

      Fig.  2.  Curves of oxygen, carbon isotope, the sea surface temperature and salinity of the core BAR9427

      图  3  BAR9427岩心浮游有孔虫重要属种丰度变化曲线

      Fig.  3.  Species relative abundances of important planktonic foraminifera of the core BAR9427

      图  4  MD81349、MD77181和BAR9427岩心二、八月表层海水盐度变化曲线

      Fig.  4.  Curves of the sea surface salinity of February and August from cores MD81349, MD77181 and BAR9427

      图  5  BAR9427碳酸盐含量、碎壳率、浮游及底栖有孔虫堆积速率、蛋白石含量和蛋白石堆积速率变化曲线

      Fig.  5.  Curves of CaCO3 content, fragments of foraminifera, opal content, MAR of planktonic and benthic foraminifers and opal of BAR9427

    • [1] Bé, A. W. H., 1977. An ecological, zoogeographic and taxo-nomic reviewof recent planktonic foraminifera. In: Ram-say, A. T. S., ed., Oceanic micropaleontology. AcademicPress, London, 1-100.
      [2] Cullen, J. L., 1981. Microfossil evidence for changing salinity patterns in the Bay of Bengal over the last 20000 years. Paleogeography Palaeocli matology Palaeoecology, 35: 315-356. doi: 10.1016/0031-0182(81)90101-2
      [3] Ding, X., Fang, N. Q., Chen, P., et al., 2003. Upwelling ac-tions in the Bay of Bengal during marine isotope stages 2 and 3: Evidence for Indian winter monsoon. Quaternary Sciences, 23 (1): 54-59 (in Chinese with English abstract).
      [4] Ding, X., Fang, N. Q., Wan, X. Q., 1999. The study of theglacial-interglacial paleoproductivity evolution duringLate Quaternary in the Bay of Bengal. Marine Geology & Quaternary Geology, 19 (3): 49-58 (in Chinese with English abstract).
      [5] Ding, X., Fang, N. Q., Wan, X. Q., 2000. Monsoon cli mateand its paleoceanographic records of the Bay of Bengalduring Late Quaternary. Geoscience, 14 (3): 295-300 (in Chinese with English abstract).
      [6] Duplessy, J. C., 1982. Glacial to interglacial contrasts in theNorthern Indian Ocean. Nature, 295: 494-498. doi: 10.1038/295494a0
      [7] Fairbanks, R. G., Sverdlove, M., Free, R., et al., 1982. Vertical distribution and isotopic fractionation of livingplanktonic foraminifera from the Panama basin. Na-ture, 298: 841-844.
      [8] Fang, N. Q., Chen, X. F., Ding, X., et al., 2001. Paleoceano-graphical records under impact of the Indian monsoonfromthe Bengal deep sea fan and Ninetyeast Ridge during the last 260 ka. Science in China (Series D), 44 (Suppl.): 351-359.
      [9] Fang, N. Q., Ding, X., Chen, X. F., et al., 1999. Rapid climatic change in oxygen isotope stage 3: Evidence fromthe rhythmic sedimentary recordin core MD77190, Bengal Bay. Quaternary Sciences, 19 (6): 511-517 (in Chinese with English abstract).
      [10] Fang, N. Q., Ding, X., Hu, C. Y., et al., 2004. A significant paleoceanographic event taking placein northeastern Indian Ocean during oxygen isotope stage 6. Earth Science—Journal of China University of Geosciences, 29 (2): 127-134 (in Chinese with English abstract).
      [11] Herguera, J. C., Berger, W. H., 1991. Paleoproductivity frombenthic foraminifera abundance: Glacial to postglacialchange in the west-equatorial Pacific. Geology, 19 (1): 1173-1176.
      [12] Huang, B. Q., Jian, Z. M., Lin, H. L., 2000. Late Quaternarychanges of paleoproductivity in the northeastern South China Sea. Marine Geology & Quaternary Geology, 20 (2): 65-68 (in Chinese with English abstract).
      [13] Kroon, D., Steens, T. N. F., Troelstra, S. R., 1991. Onset of monsoonal related upwelling in the western Arabian Seaas revealed by planktonic foraminifera. Proceeding ofthe Ocean Drilling Program Scientific Results, 117: 257-263.
      [14] Martinson, D. G., Pisias, W. G., Hays, J. D., et al., 1987. Age dating and the orbital theory of the ice age: Development of a high resolution 0 to 300000 year chronostratigraphy. Quaternary Research, 27: 1-29. doi: 10.1016/0033-5894(87)90046-9
      [15] Mortlock, R. A., Froelich, P. N., 1989. A si mple method forthe rapid determination of biogenic opal in the pelagic marine sediment. Deep Sea Res., 36 (9): 1415-1426. doi: 10.1016/0198-0149(89)90092-7
      [16] Otto, J., Hermelin, R., 1995. Impact of productivity eventson the benthic foraminaferal fauna in the Arabian Seaover the last 150000 years. Plaeoceanography, 10 (1): 85-116. doi: 10.1029/94PA02514
      [17] Pflaumann, U., Jian, Z., 1999. Modern distribution patternsof planktonic foraminifera in the South China Sea andwestern Pacific: A new transfer technique to esti materegional sea-surface temperatures. Marine Geology, 156: 41-83. doi: 10.1016/S0025-3227(98)00173-X
      [18] Prell, W. L., Curry, W. B., 1981. Faunal and isotopic indicesof monsoonal upwelling: Western Arabian Sea. Oceanal Acta, 4: 91-98.
      [19] Ren, J. Z., Ding, Z. L., Liu, D. S., et al., 1996. Cli mate chan-ges on millennial ti me scales—Evidence from a high-resolutionloess record. Science in China (Series D), 39 (5): 449-459.
      [20] Shi, Y. F., Jia, Y. L., Yu, G., et al., 2002. Features, impacts and causes of the high temperature and large precipitation event in the Tibetan plateau and its adjacent area during 40-30 kaBP. Journal of Lake Sciences, 14 (1): 1-11 (in Chinese with English abstract). doi: 10.18307/2002.0101
      [21] Shi, Y. F., Liu, X. D., Li, B. Y., et al., 1999. A very strongsummer monsoon event during 30-40 kaBP in the Qinghai-Xizang (Tibet) plateau and its relation to precessional cycle. Chinese Science Bulletin, 44 (20): 1851-1858. doi: 10.1007/BF02886339
      [22] Shi, Y. F., Yao, T. D., 2002. MIS3b (54-44 ka BP) cold pe-riod and glacial advance in middle and low latitudes. Journal of Glaciology and Geocryology, 24 (1): 1-9 (in Chinese with English abstract).
      [23] Shi, Y. F., Yu, G., 2003. Warm-humid cli mate and transgres-sions during 40-30 kaBP. and their potential mecha-nisms. Quaternary Sciences, 23 (1): 1-11 (in Chinese with English abstract).
      [24] Thunell, R. C., Reynolds, L. A., 1984. Sedi mentation of Planktonic foraminiafera: Seasonal changes in species flux in the Panama basin. Micropaleontology, 30 (3): 243-262. doi: 10.2307/1485688
      [25] Wang, L., Sarnthein, M., Erlenkeuser, H., et al., 1999. EastAsian monsoon cli mate during the Late Pleistocene: High resolution sediment records fromthe South China Sea. Marine Geology, 156: 245-284. doi: 10.1016/S0025-3227(98)00182-0
      [26] Xu, J., Wang, P. X., Huang, B. Q., et al., 2004. Mid-Pleisto-cene revolution recorded by Pullenitina obliquiloculatain the southern South China Sea. Earth Science—Journal of China University of Geosciences, 29 (1): 7-14 (in Chinese with English abstract).
      [27] Zheng, F., Li, Q. Y., Chen, M. H., et al., 2005. Late Pleisto-cene paleoceanographic characteristics of the southwest-ern South China Sea since 500 ka. Earth Science—Journal of China University of Geosciences, 30 (5): 534-543 (in Chinese with English abstract).
      [28] 丁旋, 方念乔, 陈萍, 等, 2003. 孟加拉湾深海氧同位素2、3期上升流活动. 第四纪研究, 23 (1): 54-59. https://www.cnki.com.cn/Article/CJFDTOTAL-DSJJ200301005.htm
      [29] 丁旋, 方念乔, 万晓樵, 1999. 孟加拉湾晚第四纪冰期和间冰期古生产力演变研究. 海洋地质与第四纪地质, 19 (3): 49-58. https://www.cnki.com.cn/Article/CJFDTOTAL-HYDZ903.008.htm
      [30] 丁旋, 方念乔, 万晓樵, 2000. 孟加拉湾晚第四纪的季风气候及其古海洋学记录. 现代地质, 14 (3): 295-300. doi: 10.3969/j.issn.1000-8527.2000.03.010
      [31] 方念乔, 丁旋, 陈学方, 等, 1999. 孟加拉湾MD77190柱状样第3期的韵律沉积记录及快速气候变化. 第四纪研究, 19 (6): 511-517. doi: 10.3321/j.issn:1001-7410.1999.06.003
      [32] 方念乔, 丁旋, 胡超涌, 2004. 氧同位素第6期北印度洋的一次重大古海洋学事件. 地球科学——中国地质大学学报, 29 (2): 127-134. https://www.cnki.com.cn/Article/CJFDTOTAL-DQKX200402000.htm
      [33] 黄宝琦, 翦知湣, 林慧玲, 2000. 南海东北部晚第四纪古生产力变化. 海洋地质与第四纪地质, 20 (2): 65-68. https://www.cnki.com.cn/Article/CJFDTOTAL-HYDZ200002013.htm
      [34] 施雅风, 贾玉莲, 于革, 等, 2002.40-30 kaBP青藏高原及邻区高温大降水事件的特征、影响及原因探讨. 湖泊科学, 14 (1): 1-11.
      [35] 施雅风, 姚檀栋, 2002. 中低纬度MIS3b (54~44 kaBP) 冷期与冰川前进. 冰川冻土, 24 (1): 1-9. doi: 10.3969/j.issn.1000-0240.2002.01.001
      [36] 施雅风, 于革, 2003.40-30 kaBP. 中国暖湿气候和海侵的特征与成因探讨. 第四纪研究, 23 (1): 1-11. https://www.cnki.com.cn/Article/CJFDTOTAL-DSJJ200301000.htm
      [37] 徐建, 汪品先, 黄宝琦, 等, 2004. 南海南部普林虫与"中更新世革命". 地球科学——中国地质大学学报, 29 (1): 7-14. https://www.cnki.com.cn/Article/CJFDTOTAL-DQKX200401001.htm
      [38] 郑范, 李前裕, 陈木宏, 等, 2005. 南海西南部晚更新世500ka以来的古海洋学特征. 地球科学——中国地质大学学报, 30 (5): 534-543. https://www.cnki.com.cn/Article/CJFDTOTAL-DQKX200505003.htm
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    • 收稿日期:  2006-08-06
    • 刊出日期:  2006-11-25

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