Indonesian Throughflow Actions during Last Glacial Maximum
-
摘要: 印度尼西亚穿越流是西太平洋和印度洋之间热量传输的重要载体, 穿越流的活动由潜在地影响El Nino和季风现象进而影响到全球气候变化.通过对爪哇海SHI9006岩心LGM以来氧同位素、有孔虫与CaCO3沉积量、浮游有孔虫浅层水种与深层水种比值反映的古温跃层变化等的研究, 得出结论: 研究区末次冰期氧同位素2期穿越流活动微弱, 冰后期穿越流活动增强; 特别是冰消期终止期ⅠA, 穿越流活动由弱迅速增强, 是冰川消融、海平面上升, 印度尼西亚岛弧古海水通道开放的结果.Abstract: Indonesian throughflow is the important carrier of the heat transport between the western Pacific Ocean and the Indian Ocean. Throughflow actions affect the global climate changes by influencing potentially El Nino events and monsoon actions. Based on the studies of the oxygen isotope, the mass accumulation rates of foraminifera and CaCO3, the thermocline estimated by the ratio of the planktonic foraminifera shallow-dwelling species and deep-dwelling species, we know that the throughflowwasweak during the last glacial oxygen isotope stage 2, and enhanced during the interglacial oxygen isotope stage 1. Especially in the deglaciation termination ⅠA, the throughflow changed rapidly from weak to strong. This is due to the ice sheetmelting, sea level rising, and the Indonesian Archipelagowater pathways opening.
-
Key words:
- Indonesian Archipelago /
- throughflow /
- last glacial maximum /
- foraminifera /
- paleothermocline /
- paleoproductivity
-
图 1 现代印尼海区八月表层洋流活动示意和SHI9006岩心位置
Fig. 1. Surface currents of the Indonesian archipelago in August and location of core SHI9006
图 2 SHI9006岩心氧同位素、浮游有孔虫部分属种的相对丰度变化及表层海水温度曲线(阴影区表示终止期ⅠA及LGM)
Fig. 2. Curve of δ18O, relative abundance of some planktonic foraminiferal taxa and SST in core SHI9006 (the shadow areas indicate termination ⅠA and LGM)
-
[1] Arnold, B.E., Maurice, M.P., 1987. Retreat velocity of the North Atlantic polarfront during the last deglaciation determined by 14C accelerator mass spectrometry. Nature, 328: 791-794. doi: 10.1038/328791a0 [2] Barrows, T.T., Juggins, S., DeDeckker, P., et al., 2000. Sea-surface temperatures of the southwestPacific Ocean during the last glacial maximum. Paleoceanography, 15(1): 95-109. doi: 10.1029/1999PA900047 [3] Bray, N.A., Hautala, S., Chong, J., et al., 1996. Large-scale sea level, thermocline, and wind variations in the Indonesian throughflow region. J. Geophys. Res. , 101: 12239-12254. [4] Ding, X., Guichard, F., Bassinot, F., et al., 2002. Evolution of heat transport pathways in the Indonesian Archipelago during last deglaciation. Chinese Science Bulletin, 47(22): 1912-1917. doi: 10.1360/02tb9418 [5] Duplessy, J.C., Arnold, M., Maurice, P., et al., 1986. Directdating of the oxygen-isotope record of the last deglaciation by 14C accelerator mass spectrometry. Nature, 320: 350-352. doi: 10.1038/320350a0 [6] Duplessy, J.C., Delibrias, G., Turon, J.L., et al., 1981. Deglacial warming of the northeastern Atlantic Ocean: Correlation with the paleoclimate evolution of European continent. Palaeog. Palaeocl. Palaeoeco. , 35: 121-144. doi: 10.1016/0031-0182(81)90096-1 [7] Fairbanks, R.G., 1989. A 17 000-year glacio-eustatic sea level record: Influence of glacial melting rates on the Younger Dryas event and deep-ocean circulation. Nature, 342: 637-642. doi: 10.1038/342637a0 [8] Fairbanks, R.G., Sverdlove, M., Free, R., et al., 1982. Vertical distribution and isotopic fractionation on living planktonic foraminifera from the Panama basin. Nature, 198: 841-844. [9] Gordon, A.L., Fine R.A., 1996. Pathways ofwaterbetween the Pacific and Indian Oceans in the Indonesian seas. Nature, 379: 146-149. doi: 10.1038/379146a0 [10] Hirst, A.C., Godfrey, J.S., 1993. The role of Indonesian throughflow in a global ocean GCM. J. Phys. Oceanogr. , 23: 1057-1085. doi: 10.1175/1520-0485(1993)023<1057:TROITI>2.0.CO;2 [11] Marine Geology Department of Tongji University, 1989. Paleoceanography. Tongji University Press, Shanghai(in Chinese). [12] Martinez, J.I., De Deckker, P., Barrows, T.T., 1999. Palaeoceanography of the last glacial maximum in the eastern Indian Ocean: Planktonic foraminiferal evidence. Palaeog. Palaeocl. Palaeoco. , 147: 73-99. doi: 10.1016/S0031-0182(98)00153-9 [13] Martinez, J.I., De Dekker, P., Chivas, A.R., 1997. New estimate for salinity changes in the western Pacific warm pool during the last glacial maximum: Oxygen-isotope evidence. Marine Micropaleontology, 32: 311-340. doi: 10.1016/S0377-8398(97)00029-7 [14] Martinez, J. I., Lynda, T., De Deckker, P., 1998. Planktonic foraminifera from the eastern Indian Ocean: Distribution and ecology in relation to the western Pacific warm pool(WPWP). Marine Micropaleontology, 34: 121-151. doi: 10.1016/S0377-8398(97)00045-5 [15] Martinson, D.G., Pisias, W.G., Hays, J.D., et al., 1987. Age dating and the orbital theory of the ice age: Developmentof a high resolution 0 to 300 000 year chronostratigraphy. Quaternary Research, 27: 1-29. doi: 10.1016/0033-5894(87)90046-9 [16] Pflaumann, U., Jian, Z.M., 1999. Modern distribution patterns of planktonic foraminifera in the South China Sea andwestern Pacific: A new transfer technique to estimate regional sea-surface temperatures. Mar. Geology, 156: 41-83. doi: 10.1016/S0025-3227(98)00173-X [17] Ravelo, A.C., Fairbanks, R.G., 1992. Oxygen isotopic composition of multiple species of planktonic foraminifera: Records of the modern photic zone temperature gradient. Paleoceanography, 7 (6): 815-831. doi: 10.1029/92PA02092 [18] Siedler, G., Church, J., Gould, J., 2001. Ocean circulation & climate: Observing and modelling the global ocean. International Geophysics Series, 77: 303-314. doi: 10.1016/S0074-6142(01)80125-X [19] 丁旋, Guichard, F., Bassinot, F., 等, 2003. 末次冰消期印度尼西亚多岛海热传输通道之演变. 科学通报, 48 (2): 199-204. doi: 10.3321/j.issn:0023-074X.2003.02.021 [20] 同济大学海洋地质系, 1989. 古海洋学概论. 上海: 同济大学出版社. -
下载:
点击查看大图
图(3)
计量
- 文章访问数: 3524
- HTML全文浏览量: 97
- PDF下载量: 3
- 被引次数: 0
