收稿日期: 2009-05-08
修回日期: 2009-05-15
网络出版日期: 2009-06-10
基金资助
国家重点基础研究发展计划项目“大洋碳循环与气候演变的热带驱动”(编号：G2007CB815903);国家自然科学创新研究群体科学基金项目“西太平洋暖池与东亚古环境：沉积记录的海陆对比”(编号：40321603);同济大学国家大学生创新训练计划项目联合资助.
Responses of Sea Surface Temperature and Productivity to the Changes of the Kuroshio Current in the Northern Okinawa Trough during the Holocene
Received date: 2009-05-08
Revised date: 2009-05-15
Online published: 2009-06-10
在冲绳海槽北部B-3GC孔高分辨率地层年代框架的基础上，利用多种分子生物标志物和生源组分指标，重建了该地区全新世以来表层海水温度和生产力的变化历史。研究发现，UK′37—表层海水温度和生产力的变化指示了全新世黑潮及对马暖流分支的变迁。10.6~7.3 ka BP期间，冲绳海槽北部主要受东海陆架冷水团影响，陆源物质输入量增加，初级生产力比较高，表层海水温度较低。7.3~4.6 ka BP期间，黑潮暖流对该区的影响迅速增强，表层海水快速增温，陆源物质输入减少，但是各种生产力指标显示出上升趋势，与该区上升流的出现和迅速发育有关。4.6~2.7 ka BP期间，即全新世普林虫低值事件(PME) 期间，表层海水温度明显降低了0.8~1.4℃，陆源物质输入增加，初级生产力和各种生源组分的含量也达到较高水平，说明此时黑潮强度减弱，或者黑潮主流轴向太平洋方向发生偏移，该区再次受到陆架冲淡水的影响。2.7 ka BP以来，虽然黑潮暖流再次影响到该海区，但初级生产力和生源物质输出量继续大幅增高，可能与该地区上升流的持续发育有关。
黄小慧 , 王汝建 , 翦知湣 , 王吉良 . 全新世冲绳海槽北部表层海水温度和初级生产力对黑潮变迁的响应[J]. 地球科学进展, 2009 , 24(6) : 652 -661 . DOI: 10.11867/j.issn.1001-8166.2009.06.0652
Based upon a high resolution stratigraphic and chronologic framework of core B-3GC in the northern Okinawa Trough during the Holocene, multi-proxies, including a set of marine biomarkers, contents of total organic carbon, opal and CaCO3, are used to reconstruct the past changes of sea surface temperature (SST) and productivity. Evident fluctuations of UK′37-SST and sea surface productivity records could indicate directly the variability of the Kuroshio-Tsushima Current. During 10.6~7.3 ka BP, when the northern Okinawa Trough was dominated by cold coastal water mass from the East China Sea, increasing terrigenous matter input enhanced the primary productivity, whereas the UK′37-SST remained lowering. During 7.3~4.6 ka BP, when the northern Okinawa Trough was abruptly influenced by the Kuroshio Current, the UK′37-SST increased and terrigenous matter input decreased. Although the Kuroshio Current prevented the intrusion from the coastal waters, contents of biomarkers and biogenic components still continuously increased, which was probably caused by the strengthened upwelling in this region. During 4.6~2.7 ka BP (Pulleniatina Minimum Event, PME), the UK′37-SST recorded an evident cooling signal of 0.8~1.4℃, meanwhile, terrigenous matter input, productivity as well as biogenic components all greatly increased. All these changes suggest that the influence of the Kuroshio Current sharply weakened or its main axis may shift to the open Pacific Ocean in this interval. The northern Okinawa Trough was again affected by the coastal waters. During 2.7 ka BP to the present, the Kuroshio Current probably reentered this region, resulting in a warm SST condition. However, primary productivity and biogenic components drastically increased, which may be induced by the persistently enhanced upwelling in the northern Okinawa Trough.
[1] Hsueh Y, Lie H J, Ichikawa H. On the branching of the Kuroshio west of Kyushu[J].Journal of Geophysical Research,1996,101(C2):3 851-3 857.
[2] Lie H J, Cho C H. On the origin of the Tsushima warm current[J].Journal of Geophysical Research,1994,99(C12): 25 081-25 091.
[3] Guo Binghuo, Ge Renfeng. Role of Kuroshio frontal eddy in exchange between shelf water and Kuroshio water in East China Sea[J].Acta Oceanologica Sinica,1997, 19(6): 1-11.[郭炳火,葛人峰.东海黑潮锋面涡旋在陆架水与黑潮水交换中的作用[J]. 海洋学报, 1997, 19(6): 1-11.]
[4] Ujiié H, Ujiié Y. Late Quaternary course changes of the Kuroshio current in the Ryukyu arc region, northwestern Pacific Ocean[J].Marine Micropaleontology,1999, 37:23-40.
[5] Jian Z, Wang P, Saito Y, et al. Holocene variability of the Kuroshio Current in the Okinawa Trough, Northwestern Pacific Ocean[J].Earth and Planetary Science Letters,2000, 184: 305-319.
[6] Ujii Y, Ujii H, Taira A, et al. Spatial and temporal variability of surface water in the Kuroshio source region, Pacific Ocean, over the past 21 000 years: Evidence from planktonic foraminifera[J].Marine Micropaleontology,2003, 49:335-364.
[7] Xu X, Oda M. Surface-water evolution of the eastern East China Sea during the last 36 000 years[J].Marine Geology,1999, 156: 285-304.
[8] Ijiri A, Wang L J, Oba T, et al. Paleoenvironmental changes in the northern area of the East China Sea during the past 42 000 years[J].Palaeogeography, Palaeoclimatology, Palaeoecology, 2005, 219: 239-261.
[9] Li Tiegang, Sun Rongtao, Zhang Deyu, et al. Evolution and variation of the Tsushima warm current during the late Quaternary: Evidence from planktonic foraminifera, oxygen and carbon isotopes[J].Science in China (Series D),2007,50(5):725-735.[李铁刚, 孙荣涛, 张德玉,等. 晚第四纪对马暖流的演化和变动: 浮游有孔虫和氧碳同位素证据[J].中国科学:D辑,2007,37(5):660-669.]
[10] Bond G, Showers W, Cheseby R L, et al. A pervasive millennial-scale cycle in North Atlantic Holocene and glacial climates[J].Science,1997,278:1 257-1 266.
[11] Gupta A K, Anderson D M, Overpeck J T. Abrupt changes in the Asian southwest monsoon during the Holocene and their links to the North Atlantic Ocean[J].Nature,2003, 421: 354-357.
[12] Wang Y J, Chen H, Edwards R L, et al. The Holocene Asian Monsoon: Links to solar changes and North Atlantic climate[J].Sciences,2005, 308: 854-857.
[13] Li B, Jian Z, Wang P, et al. Pulleniatina obliquiloculata as a paleoceanographic indicator in the south Okinawa Trough during the last 20 000 years[J].Marine Micropaleontology, 1997, 32: 59-69.[14] Lin Y S, Wei K Y, Lin I T, et al. The Holocene Pulleniatina Minimum Event revisited: Geochemical and faunal evidence from the Okinawa Trough and upper reaches of the Kuroshio current[J].Marine Micropaleontology,2006, 59: 153-170.
[15] Jian Zhimin, Li Baohua, Pflaumann U, et al. Late Holocene cooling event in the western Pacific[J].Science in China (Series D),1996, 39(5): 543-550.[翦知湣, 李保华, Pflaumann U,等.西太平洋晚全新世变冷事件[J]. 中国科学:D辑, 1996, 26(5): 461-466.]
[16] Sun Y B, Oppo D W , Xiang R, et al. Last deglaciation in the Okinawa Trough: Subtropical northwest Pacific link to Northern Hemisphere and tropical climate[J].Paleoceanography,2005, 20, A4005. doi:10.1029/2004PA001061.
[17] Xiang R, Sun Y, Li T, et al. Paleoenvironmental change in the middle Okinawa Trough since the last deglaciation: Evidence from the sedimentation rate and planktonic foraminiferal record[J]. Palaeogeography, Palaeoclimatology, Palaeoecology,2007, 243: 378-393.
[18] Chang F, Li T, Zhuang L, et al. A Holocene paleotemperature record based on radiolaria from the northern Okinawa Trough (East China Sea)[J].Quaternary International,2008,183:115-122.
[19] Nan Qingyun, Li Tiegang, Chen Jinxia, et al. Paleoproductivity variation and its correlation with climate changes: An approach of long-chain alkenone[J].Quaternary Sciences,2008, 28(3): 482-490.[南青云, 李铁刚, 陈金霞,等. 南冲绳海槽7000年 BP以来基于长链不饱和烯酮指标的古海洋生产力变化及其与气候的关系[J]. 第四纪研究, 2008, 28(3): 482-490.]
[20] Li Qing, Li Tiegang, Chang Fengming, et al. Evolution of upwelling in the north of the Okinawa Trough since about 7 300 a BP[J].Marine Geology & Quaternary Geology,2008, 28(2): 65-70.[李青, 李铁刚, 常凤鸣,等.近7 300 aBP以来冲绳海槽北部上升流的演化[J]. 海洋地质与第四纪地质, 2008, 28(2): 65-70.]
[21] Jin Xianglong,ed. Geology of the East China Sea[M]. Beijing: Ocean Press, 1992.[金翔龙主编.东海地质[M]. 北京: 海洋出版社,1992.]
[22] Song Changqing, Sun Xiangjun, Saito Y. Paleoenvironmental information recorded by pollen in B-3GC gravity core in Okinawa Trough[J].Chinese Science Bulletin,2001, 46(11): 938-942.[宋长青, 孙湘君, Saito Y.冲绳海槽B-3GC钻孔柱状样花粉记录的古环境信息[J].科学通报, 2001,46(2):153-157.][23] Müller P J, Kirst G, Ruhland G, et al. Calibration of the alkenone paleotemperature index UK′37 based on core-tops from the eastern South Atlantic and the global ocean (60°N～60°S)[J]. Geochimica et Cosmochimica Acta,1998,62:1 757-1 772.
[24] Mortlock R A, Froelich P N. A simple method for the rapid determination of biogenic opal in the pelagic marine sediment[J].Deep-Sea Research,1989,36(9):1 415-1 426.
[25] Zhao M, Huang C Y, Wei K Y. A 28 000 year UK′37 sea-surface temperature record of ODP Site 1 202B, the southern Okinawa Trough[J].Terrestrial Atmosphere Ocean Sciences,2005, 16(1): 45-56.
[26] Zhou H, Li T, Jia G, et al. Sea surface temperature reconstruction for the middle Okinawa Trough during the last glacial-interglacial cycle using C37 unsaturated alkenones[J]. Palaeogeography, Palaeoclimatology, Palaeoecology,2007, 246(2/4): 440-453.
[27] Xing Lei, Zhao Meixun, Zhang Hailong, et al. Biomarker reconstruction of phytoplankton productivity and community structure changes in the middle Okinawa Trough during the last 15 ka[J].Chinese Science Bulletin,2008, 53(16):2 552-2 559.[邢磊,赵美训,张海龙,等.冲绳海槽中部过去15 ka来浮游植物生产力和种群结构变化的生物标志物重建[J].科学通报, 2008,53(12):1 448-1 455.]
[28] Tanaka Y. Coccolith flux and species assemblages at the shelf edge and in the Okinawa Trough of the East China Sea[J].Deep-Sea Research: Part 2,2003, 50: 503-511.
[29] Shieh Y T, Chen M P. The ancient Kuroshio Current in the Okinawa Trough during the Holocene[J].Acta Oceanography Taiwan,1995, 34(4): 73-80.
[30] Li T G, Liu Z X, Hall M A, et al. Heinrich event imprints in the Okinawa Trough: Evidence from oxygen isotope and planktonic foraminifera[J].Palaeogeography,Palaeoclimatology, Palaeoecology, 2001,176:133-146.
[31] He J, Zhao M, Li L, et al. Biomarker evidence of relatively stable community structure in the northern South China Sea during the last glacial and Holocene[J].Terrestrial Atmosphere Ocean Sciences,2008,19(4): 377-387.
[32] Stax R, Stein R. Long-term changes in the accumulation of organic carbon in Neogene sediments of ODP-Leg 130 (Ontong Jave plateau)[R].Proceedings of the Ocean Drilling Program, Scientific Results,130,1993:573-584.
[33] Wang P.Response of Western Pacific marginal seas to glacial cycles:Paleoceanographic and sedimentological features[J].Marine Geology,1999,156: 5-39.
[34] Sawada K, Handa N. Variability of the path of the Kuroshio ocean current over the past 25 000 years[J].Nature,1998, 392: 592-595.
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