| Qingdao Institute of marine geology, China Geological Survey | Host |
| Citation: |
XU Ye, CHANG Fengming, LI Tiegang, ZHAO Song, CUI Yikun. The hydroclimate changes in the northern Okinawa Trough during middle Holocene: Evidence from planktonic foraminiferal assemblages[J]. Marine Geology & Quaternary Geology, 2019, 39(1): 113-123. doi: 10.16562/j.cnki.0256-1492.2017122101
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The hydroclimate changes in the northern Okinawa Trough during middle Holocene: Evidence from planktonic foraminiferal assemblages
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Abstract
Planktonic foraminifera assemblages in the northern East China Sea are significantly influenceed by both the Changjiang Diluted Water and Kuroshio Current. A total of 28 species in the coaser faction (>150μm) are identified based on planktic foraminifera analysis of 178 samples from core NOKT-3 in the northern Okinawa Trough. The results show that variations in percentage of Globigerina quinqueloba is characterized by sharp fluctuation in early Mid-Holocene and gradual decline in late Mid-Holocene. This low temperature and low salt salinity species is an indicator of the Changjiang Diluted Water, which is controlled by the East Asian summer monsoon precipitation. Therefore, the evolution of precipetation in the middle and lower reaches of the Yangtze River between 6330 and 3890aBP can be divided into three major stages based on variations in its content: (1) high precipetation during the period of 6330~4950aBP, which correspondes to the Holocene optimum; (2) a decreased trend of precipetation from 4950 to 4600aBP, implying termination of the Holocene optimum; (3) a marked decrease in the monsoon precipitation between 4600 and 3890aBP, indicating an arid climate condition. This precipetation pattern could be related to the general weakening and southeastward retreat of the East Asian summer monsoon resulted from the decreased solar-radiation in the northern hemisphere during the Middle Holocene. Moreover, remarkably high abundance of P. obliquiloculat during 6330~5100aBP, which is normally an indicator species of the Kuroshio Current, suggests that influence of the Kuroshio Current in the Okinawa Through was persistently strong. The abundance of P. obliquiloculata sharply decreased during 5100~4000aBP, well corresponding to the so-called Pulleniatina minimum event (PME). Our results show that there were not a cold climate condition corresponding to the PME during the period of late Mid-Holocene. In addition, enhancement of the El Niño-like condition in the tropical Pacific region during this time window also can not fully explain the occurrence of PME in the northern Okinawa Trough.
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References
[1] 郑伟鹏, 俞永强.一个耦合气候系统模式模拟的中全新世时期亚洲季风系统变化[J].第四纪研究, 2009, 29(6): 1135-1145. doi: 10.3321/j.issn:1001-7410.2004.01.004 ZHENG Weipeng, YU Yongqiang. Simulations of East Asian climate at 6kaBP[J]. Quaternary Sciences, 2004, 24(1): 28-38. doi: 10.3321/j.issn:1001-7410.2004.01.004 [2] Chen Z Y, Song B P, Wang Z H, et al. Late Quaternary evolution of the sub-aqueous Yangtze Delta, China: sedimentation, stratigraphy, palynology, and deformation[J]. Marine Geology, 2000, 162: 423-441. doi: 10.1016/S0025-3227(99)00064-X [3] Yi S, Saito Y, Zhao Q H, et al. Vegetation and climate changes in the Changjiang (Yangtze River) Delta, China, during the past 13, 000 years inferred from pollen records[J]. Quaternary Science Reviews, 2003, 22(14): 1501-1519. doi: 10.1016/S0277-3791(03)00080-5 [4] Du Y, Cai S M, Zhang X Y, et al. Interpretation of the environmental change of Dongting Lake, middle reach of Yangtze River, China, by 210Pb measurement and satellite image analysis[J]. Geomorphology, 2001, 41(2-3): 171-181. doi: 10.1016/S0169-555X(01)00114-3 [5] Yu K F, Zhao J X, Wei G J, et al. Mid-late Holocene monsoon climate retrieved from seasonal Sr/Ca and δ18O records of Porites lutea corals at Leizhou Peninsula, northern coast of South China Sea[J]. Global and Planetary Change, 2005, 47(2-4): 301-316. doi: 10.1016/j.gloplacha.2004.10.018 [6] Li B, Liu H, Wu L, et al. Linking the vicissitude of Neolithic cities with mid Holocene environment and climate changes in the middle Yangtze River, China[J]. Quaternary International, 2014, 321: 22-28. doi: 10.1016/j.quaint.2013.11.018 [7] Dykoski C A, Edwards R L, Cheng H, et al. A high-resolution, absolute-dated Holocene and deglacial Asian monsoon record from Dongge Cave, China[J]. Earth and Planetary Science Letters, 2005, 233(1-2): 71-86. doi: 10.1016/j.epsl.2005.01.036 [8] Hu C Y, Henderson G M, Huang J H, et al. Quantification of Holocene Asian monsoon rainfall from spatially separated cave records[J]. Earth and Planetary Science Letters, 2008, 266(3-4): 221-232. doi: 10.1016/j.epsl.2007.10.015 [9] Dong J G, Wang Y J, Edwards R L, et al. A high-resolution stalagmite record of the Holocene East Asian monsoon from Mt Shennongjia, central China[J]. The Holocene, 2010, 20(2): 257-264. doi: 10.1177/0959683609350393 [10] Chang Y P, Wang W L, Yokoyama Y, et al. Millennial-scale planktic foraminifer faunal variability in the East China Sea during the Past 40000 Years (IMAGES MD012404 from the Okinawa Trough)[J]. Terrestrial, Atmospheric and Oceanic Sciences, 2008, 19(4): 389-401. doi: 10.3319/TAO.2008.19.4.389(IMAGES) [11] Diekmann B, Hofmann J, Henrich R, et al. Detrital sediment supply in the southern Okinawa Trough and its relation to sea-level and Kuroshio dynamics during the late Quaternary[J]. Marine Geology, 2008, 255(1-2): 83-95. doi: 10.1016/j.margeo.2008.08.001 [12] Kawahata H, Ohshima H. Vegetation and environmental record in the northern East China Sea during the late Pleistocene[J]. Global and Planetary Change, 2004, 41(3-4): 251-273. doi: 10.1016/j.gloplacha.2004.01.011 [13] 叶银灿, 庄振业, 刘杜娟, 等.东海全新世沉积强度分区[J].青岛海洋大学学报, 2002, 32(6): 941-948. doi: 10.3969/j.issn.1672-5174.2002.06.010 YE Yincan, ZUANG Zhenye, LIU Dujuan, et al. Holocene depositional strength zoning in the East China Sea[J]. Journal of Qingdao Ocean University, 2002, 32(6): 941-948. doi: 10.3969/j.issn.1672-5174.2002.06.010 [14] Yang Z S, Saito Y, Guo Z G, et al. Distal mud area as a material sink in the East China Sea[M].Japan:Hokkido University Press, 1994:1-6. [15] Ujiié Y, Ujiié H. Distribution and oceanographic relationships of modern planktonic foraminifera in the Ryukyu Arc region, Northwest Pacific Ocean[J]. The Journal of Foraminiferal Research, 2000, 30(4): 336-360. doi: 10.2113/0300336 [16] 李铁刚, 常凤鸣.冲绳海槽古海洋学[M].北京:海洋出版社, 2009:34-35. LI Tiegang, CHANG Fengming. Paleoceanography in the Okinawa Trough[M]. Beijing: Ocean press, 2009:34-35. [17] Schiebel R, Hemleben C. Planktic Foraminifers in the Modern Ocean[M]. Berlin: Springer Nature, 2017. [18] Bé A. An ecological, zoogeographic and taxonomic review of recent planktonic foraminifera[M]. London: Academic Press, 1977, 1: 1-100. [19] Schmuker B, Schiebel R. Planktic foraminifers and hydrography of the eastern and northern Caribbean Sea[J]. Marine Micropaleontology, 2002, 46: 387-403. doi: 10.1016/S0377-8398(02)00082-8 [20] Naidu P D, Malmgren B A. A High-resolution record of Late Quaternary upwelling along the Oman Margin, Arabian Sea based on planktonic foraminifera[J]. Paleoceanography, 1996, 11(1): 129-140. doi: 10.1029/95PA03198 [21] Conan S H, Brummer G J. Fluxes of planktic foraminifera in response to monsoonal upwelling on the Somalia Basin margin[J]. Deep-Sea Research Ⅱ, 2000, 47: 2207-2227. doi: 10.1016/S0967-0645(00)00022-9 [22] Schiebel R, Zeltner A, Treppke U F, et al. Distribution of diatoms, coccolithophores and planktic foraminifers along a trophic gradient during SW monsoon in the Arabian Sea[J]. Marine Micropaleontology, 2004, 51(3-4): 345-371. doi: 10.1016/j.marmicro.2004.02.001 [23] Bé A, Tolderlund S D. Distribution and ecology of living planktonic foraminifera in surface waters of the Atlantic and Indian Oceans[J]. Micropaleontology of Oceans, 1971: 105-149. [24] Watkins J M, Mix A C, Wilson J. Living planktic foraminifera: tracers of circulation and productivity regimes in the central equatorial Pacific[J]. Deep Sea Research Part Ⅱ: Topical Studies in Oceanography, 1996, 43(4-6): 1257-1282. doi: 10.1016/0967-0645(96)00008-2 [25] Reynolds L A, Thunell R C. Seasonal production and morphologic variation of neogloboquadrina pachyderma (ehrenberg) in the northeast Pacific[J]. Micropaleontology, 1986, 32(1): 1-18. doi: 10.2307/1485696 [26] Ujiié H, Hatakeyam Y, Gu X X, et al. Upward decrease of organic C/N ratios in the Okinawa Trough cores: proxy for tracing the post-glacial retreat of the continental shoreline[J]. Palaeogeography, Palaeoclimatology, Palaeoecology, 2001, 165: 129-140. doi: 10.1016/S0031-0182(00)00157-7 [27] Zheng X F, Li A C, Wan S M, et al. ITCZ and ENSO pacing on East Asian winter monsoon variation during the Holocene: Sedimentological evidence from the Okinawa Trough[J]. Journal of Geophysical Research: Oceans, 2014, 119(7): 4410-4429. doi: 10.1002/2013JC009603 [28] Li T G, Xu Z K, Lim D, et al. Sr-Nd isotopic constraints on detrital sediment provenance and paleoenvironmental change in the northern Okinawa Trough during the late Quaternary[J]. Palaeogeography, Palaeoclimatology, Palaeoecology, 2015, 430: 74-84. doi: 10.1016/j.palaeo.2015.04.017 [29] Jian Z M, Wang P X, 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. doi: 10.1016/S0012-821X(00)00321-6 [30] Ujiié Y, Ujiié H, Taira A, et al. Spatial and temporal variability of surface water in the Kuroshio source region, Pacific Ocean, over the past 21000 years: evidence from planktonic foraminifera[J]. Marine Micropaleontology, 2003, 49(4): 335-364. doi: 10.1016/S0377-8398(03)00062-8 [31] Kao S J, Lin F J, Liu K K. Organic carbon and nitrogen contents and their isotopic compositions in surficial sediments from the East China Sea shelf and the southern Okinawa Trough[J]. Deep Sea Research Part Ⅱ: Topical Studies in Oceanography, 2003, 50(6-7): 1203-1217. doi: 10.1016/S0967-0645(03)00018-3 [32] Iseki K, Okamura K, Kiyomoto Y. Seasonality and composition of downward particulate fluxes at the continental shelf and Okinawa Trough in the East China Sea[J]. Deep-Sea Research Ⅱ, 2003, 50: 457-473. [33] Sautter L R, Thune R C. Seasonal variability in the 18O and 13C of planktonic foraminifera from an upwelling environment: sediment trap results from San Pedro Basin, southern California[J]. Paleoceanography, 1991, 6(3): 307-334. doi: 10.1029/91PA00385 [34] Xu X D, Oda M. Surface-water evolution of the eastern East China Sea during the last 36000 years[J]. Marine Geology, 1999, 156: 285-304. doi: 10.1016/S0025-3227(98)00183-2 [35] 李枫, 吴立, 朱诚, 等.江汉平原12.76 cal. kaBP以来环境干湿变化的高分辨率研究[J].地理科学, 2012, 32(7): 878-884. LI Feng, WU Li, ZHU Cheng, et al. A high-resolution study of moisture evolution in the Jianghan Plain since 12.76 cal.kaBP[J]. Geography, 2012, 32(7): 878-884. [36] An Z S, Porter C S, Kutzbach E J, et al. Asynchronous Holocene optimum of the East Asian monsoon[J]. Quaternary Science Reviews, 2000, 19: 743-762. doi: 10.1016/S0277-3791(99)00031-1 [37] 王晓翠, 朱诚, 吴立, 等.湖北江汉平原JZ-2010剖面沉积物粒度特征与环境演变[J].湖泊科学, 2012, 24(3): 480-486. doi: 10.3969/j.issn.1003-5427.2012.03.022 WANG Xiaocui, ZHU Cheng, WU Li, et al. Grain-size characteristics and sedimentary environment change of JZ-2010 section in Jianghan Plain, Hubei Province[J]. Journal of Lake Sciences, 2012, 24(3): 480-486. doi: 10.3969/j.issn.1003-5427.2012.03.022 [38] 安芷生, 吴锡浩, 王苏民, 等.中国中东部全新世气候适宜期与东亚夏季风变迁[J].科学通报, 1993, 38(14): 1302-1305. AN Zhisheng, WU Xihao, WANG Sumin, et al. Holocene optimum in center and eastern China and the evolution of the East Asian monsoon[J]. Chinese Science Bulletin, 1993, 38: 1302-1305. [39] Li T G, Nan Q Y, Jiang B, et al. Formation and evolution of the modern warm current system in the East China Sea and the Yellow Sea since the last deglaciation[J]. Chinese Journal of Oceanology and Limnology, 2009, 27(2): 237-249. doi: 10.1007/s00343-009-9149-4 [40] Ujiié Y, Asahi H, Sagawa T, et al. Evolution of the North Pacific Subtropical Gyre during the past 190ka through the interaction of the Kuroshio Current with the surface and intermediate waters[J]. Paleoceanography, 2016, 31: 1498-1513. doi: 10.1002/2015PA002914 [41] 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(3-4): 153-170. doi: 10.1016/j.marmicro.2006.02.003 [42] Li T G, Liu Z X, Hall A M. Heinrich event imprints in the Okinawa Trough: evidence from oxygen isotope and planktonic foraminifera[J]. Palaeogeography, Palaeoclimatology, Palaeoecology, 2001, 176(1-4): 133-146. doi: 10.1016/S0031-0182(01)00332-7 [43] Wu W X, Liu T S. Possible role of the "Holocene Event 3" on the collapse of Neolithic Cultures around the Central Plain of China[J]. Quaternary International, 2004, 117(1): 153-166. [44] Sawada K, Handa N. Variability of the path of the Kuroshio Current over the past 25000 years[J]. Nature, 1998, 392: 592-595. doi: 10.1038/33391 [45] Moy C M, Seltzer G O, Rodbell D T, et al. Variability of El Niño/Southern Oscillation activity at millennial timescales during the Holocene epoch[J]. Nature, 2002, 420(6912): 159-162. doi: 10.1038/nature01163 [46] Sandweiss D H, Richardson J B, Reitz E J, et al. Geoarchaeological evidence from Peru for a 5000 Years B.P. onset of El Niño[J]. Science, 1996, 273: 1531-1533. doi: 10.1126/science.273.5281.1531 -
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XU Ye, CHANG Fengming, LI Tiegang, ZHAO Song, CUI Yikun. The hydroclimate changes in the northern Okinawa Trough during middle Holocene: Evidence from planktonic foraminiferal assemblages[J]. Marine Geology & Quaternary Geology, 2019, 39(1): 113-123. doi: 10.16562/j.cnki.0256-1492.2017122101
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Figure 1.
Modern air circulation in East Asian and major ocean circulation in East China Sea
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Figure 2.
Vertical variations in percentage of clay, silt and sand in core NOKT-3
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Figure 3.
Vertical variations in plankton foraminifer species, abundance and percentage of dominant species in core NOKT-3
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Figure 4.
Comparisons of summer insolation at 60°N (A) to percentage of G. quinqueloba (B) in core NOKT-3 and the δ18O of stalagmite from Heshang (C)[8], Sanbao (D) [9] and Dongge Cave (E)[7]
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Figure 5.
Comparisons of the percentage of P. obliquiloculata, N. dutertrei and G. bulloides to warm-species percentage and the ratio of warm species with cold species in core NOKT-3 (Shade area indicates the PME)