柴达木盆地察尔汗古湖贝壳堤剖面沉积地球化学与环境变化

常凤琴; 张虎才; 陈玥; 杨明生; 牛洁; 樊红芳; 雷国良; 张文翔; 类延斌; 杨伦庆

柴达木盆地察尔汗古湖贝壳堤剖面沉积地球化学与环境变化

常凤琴^{1, 2},
张虎才^{1, 2, ,},
陈玥²,
杨明生²,
牛洁²,
樊红芳²,
雷国良²,
张文翔²,
类延斌¹,
杨伦庆¹

1.
中国科学院南京地理与湖泊研究所湖泊与环境国家重点实验室，江苏南京 210008
2.
兰州大学资环学院，西部环境教育部重点实验室，甘肃兰州 730000

基金项目:

国家自然科学基金项目 40371117

详细信息

作者简介:
常凤琴（1976—），女，同位素与地球化学方向博士研究生

通讯作者:
张虎才, E-mail: zhanghc@niglas.ac.cn

中图分类号: P594
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- 被引次数: 0
出版历程
- 收稿日期: 2007-05-12
- 刊出日期: 2008-03-25

Sedimentation Geochemistry and Environmental Changes during Late Pleistocene of Paleolake Qarhan in the Qaidam Basin

1.
State Key Laboratory of Lake Science and Environment,Nanjing Institute of Geography and Limnology,CAS,Nanjing 210008,China
2.
Key Laboratory of Western China’s Environments,MOE;College of Earth Sciences and Environments,Lanzhou University,Lanzhou 730000,China

摘要

摘要: 通过对柴达木盆地察尔汗古湖贝壳堤剖面沉积物中总有机碳、有机质碳同位素及碳酸盐含量、碳氧同位素的分析, 并结合粒度数据, 将研究剖面所记录的古湖泊环境演化过程划分为5个阶段.其中254 (连续古湖泊沉积开始与第八层底部) ~210cm (距今39.7~35.8ka BP之间) 为湖泊发育期.210~185cm (距今35.8~33.6ka BP之间), 185~112cm (距今33.6~27.2ka BP之间) : TOC、CaCO₃含量较高、δ¹⁸ O值偏正, δ¹³ C_org偏负, Mz值较低, 反映了当时温度较高, 湖水水位较高; 而112~55cm (距今27.2~22.3ka BP之间) 和55~0cm (距今22.3~17.5ka BP之间) : TOC、CaCO₃含量较低、δ¹⁸ O值偏负, δ¹³ C_org偏正, Mz值较高, 表明了温度相对较低(但气候仍较温暖), 湖水水位较低, 湖泊处于退缩时期.其间分别在距今32.2~32.4ka BP、30.4~29.8ka BP和28.4~27.2ka BP出现了3次较大的退缩过程, 约22ka BP出现了一次气候突变.贝壳堤剖面揭示在39.7~18.5 ¹⁴C ka BP之间柴达木盆地气候较温暖湿润, 形成高湖面.从18.2ka BP开始, 湖泊进入退缩阶段.到17.5ka BP快速形成盐壳, 高湖面持续历史结束.
- 柴达木盆地 /
- 贝壳堤 /
- 碳氧同位素 /
- 古环境意义
Abstract: Based on the analysis of TOC, CaCO₃, δ¹³ C_org, δ¹⁸ O, δ¹³ C of shell bar sediments in the Qaidam basin and the comparison with grain size, the environmental change of the studied section are divided into five stages.From 39.7 to 35.8 ka BP is the period of high paleolake level development.From 35.8 to 33.6 ka BP and 33.6 to 27.2 ka BP, TOC and CaCO₃ contents, δ¹⁸ O value are high, while δ¹³ C_org value and median size content are low, which reflects a warm-humid climate and high lake level.During 27.2-22.3 ka BP and 22.3-17.5 ka BP, both the temperature and the lake level are lower than that of previous stages (but the climate was still warmer and more humid than that of today).The lake level decreased between 32.4 and 32.2 ka BP, 30.4 and 29.8 ka BP, 28.4 and 27.2 ka BP.Generally speaking, the climate was warm and humid in Qaidam basin and the high lake level sustained between 39.7 and 17.5 ka BP.The lake retreated abruptly at 17.5 ka BP, with a very strong increase of evaporation which resulted in the salt formation and the decrease of the high lake level.
- Qaidam basin /
- shell bar /
- stable oxygen and carbon isotopes /
- paleoenvironmental significance

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图 1 贝壳堤野外展布及剖面位置

Fig. 1. The field distribution pattern of the shell bar and the section site

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图 2 贝壳堤剖面碳酸盐碳氧同位素相关性

Fig. 2. The coefficient between δ¹³ C and δ¹⁸ O of the CaCO₃ in shell bar section

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图 3 贝壳堤和西宁黄土碳氧同位素相关性的比较

Fig. 3. Comparison of the carbonate δ¹⁸ O and δ¹³ C between shell bar section and Late Pleistocene loess in Xining

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图 4 贝壳堤剖面δ¹³ C、δ¹⁸ O、CaCO₃含量、TOC、δ¹³ C_org和中值粒径(Mz)

Fig. 4. The δ¹³ C, δ¹⁸ O of CaCO₃ and its content, TOC content and its δ¹³ C_org and median of the grain size

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参考文献(30)

[1]	Chen, J. A., Wan, G. J., Wang, F. S., et al., 2002. Research of the carbon environment records in the lake modern sediments. Science in China (Seri. D), 32: 73-80 (inChinese).
[2]	Jia, Y. L., Shi, Y. F., Wang, S. M., et al., 2001.4 times paleolake level risings and their formation mechanisms during last 40 ka on the Tibetan plateau. Science in China (Seri. D), 31 (Suppl. ): 241-251 (in Chinese).
[3]	Kelts, K., Talbot, M., 1990. Lacustrine carbonates as geochemical archives of environmental change and biotic/abiotic interactions. In: Tilzer, M. M., Serruya, C. C., eds., Ecological structure and function in large lake, Madison. Wis. Science Tech., 290-317.
[4]	Li, B. Y., 2000. The last greatest lakes onthe Xizang (Tibetan) plateau. Acta Geographica Sinica, 55 (2): 174-182 (in Chinese with English abstract).
[5]	Li, B. Y., Zhang, Q. S., Wang, F. B., 1991. Evolution of the lakes in the Karakorum-West Kunlun Mountains. Quaternary Sciences, (1): 64-71 (in Chinese with English abstract).
[6]	Lin, R. F., Wei, K. Q., 2000. A δ¹³ C record of the organic matter in lacustrine sediments of the core ZHJ from Lake Caohai and its palaeoclimate implications. Geochimica, 29 (4): 390-395 (in Chinese with Englishabstract).
[7]	Shen, J., Wang, S. M., Yang, X. D., 1996. Measurement of organic carbon stable isotope in lacustrine seiments and its significance on palaeoclimate and environment. Oceanologic and Limnologic Sinica, 27 (4): 400-404 (in Chinese with English abstract).
[8]	Shen, J., Wu, R. J., An, Z. S., 1998. Characters of the organic δ¹³ C and palaeoenvironment in the section of Dabusu Lake. Journal of Lake Sciences, 10 (3): 8-12 (in Chi-nese with English abstract). doi: 10.18307/1998.0302
[9]	Talbot, M. R., 1980. A review of the palaeohydrological interpretation of carbon and oxygenisotopic ratios in primary lacustrine carbonates. Chemical Geology, 80: 261-279.
[10]	Wu, J. L., Luecke, A., Li, S. J., et al., 2000. Modern climaticsignals fromrecords of contents of TOC and δ¹³ C_org in the Xingcuo Lake sediments in eastern Tibetan Plateau, China. Marine Geology and Quaternary Geology, 20 (4): 37-42 (in Chinese with English abstract).
[11]	Wu, J. L., Wang, S. M., 1996. Climate versus change inδ¹³ C values of the organic matter in lake sediments. Marine Geology and Quaternary Geology, 16 (2): 103-108 (inChinese with English abstract).
[12]	Zhang, H. C., 1997. The superficial elemental geochemistryand theoretical principles. Lanzhou Univ. Press, Lanzhou (in Chinese).
[13]	Zhang, H. C., Ma, Y. Z., Wüennemann, B., et al., 2000. A Holocene climatic recordfromarid northwestern China. Palaeog., Palaeoclim., Palaeoec., 162: 389-401. doi: 10.1016/S0031-0182(00)00139-5
[14]	Zhang, H. C., Ma, Y. Z., Peng, J. L., et al., 2002. Palaeolake and palaeoenvironment between 42-18 ka BP inTengger desert, NW China. Chinese Science Bulletin, 47 (24): 1847-1857 (in Chinese). doi: 10.1360/csb2002-47-24-1847
[15]	Zhang, H. C., Chang, F. Q., Li, B., et al., 2007. Branched aliphatic alkanes of the Late Pleistocene paleolake deposits from the Qaidam basin, NE Tibetan plateau. Chinese Science Bulletin, 52 (9): 1248-1256. doi: 10.1007/s11434-007-0167-3
[16]	Zhang, H. C., Wünnemann, B., 1997. Preliminary study on the chronology of lacustrine deposits and determination of high palaeo-lake level in Tengger desert since Late Pleistocene. Journal of Lanzhou University (Natural Sciences), 33 (2): 87-91 (in Chinese with English ab-stract).
[17]	Zhang, Y. F., Li, C. A., Chen, G. J., et al., 2005. Characteristics and paleoclimatic significence of magenetic susceptibilioty and stable organic carbon isotopes from a bore in Zhoulao Town, Jianghan plain. Earth Science—Journal of China University of Geosciences, 31 (1): 114-120 (in Chinese with English abstract).
[18]	陈敬安, 万国江, 汪福顺, 等, 2002. 湖泊现代沉积物碳环境记录研究. 中国科学(D辑), 32: 73-80. https://www.cnki.com.cn/Article/CJFDTOTAL-JDXK200201008.htm
[19]	贾玉连, 施雅风, 王苏民, 等, 2001.40ka以来青藏高原的4次湖涨期及其形成机制初探. 中国科学(D), 31 (增刊): 241-251. https://www.cnki.com.cn/Article/CJFDTOTAL-JDXK2001S1036.htm
[20]	李炳元, 2000. 青藏高原大湖期. 地理学报, 55 (2): 174-182. doi: 10.3321/j.issn:0375-5444.2000.02.005
[21]	李炳元, 张青松, 王富葆, 1991. 喀喇昆仑山—西昆仑山地区的湖泊演化. 第四纪研究, (1): 64-71. doi: 10.3321/j.issn:1001-7410.1991.01.008
[22]	林瑞芬, 卫克勤, 2000. 草海柱样沉积物有机质的记录及其古环境信息. 地球化学, 29 (4): 390-395. doi: 10.3321/j.issn:0379-1726.2000.04.012
[23]	沈吉, 王苏民, 羊向东, 1996. 湖泊沉积物中有机碳稳定同位素测定及其古气候意义. 海洋与沼泽, 27 (4): 400-404. https://www.cnki.com.cn/Article/CJFDTOTAL-HYFZ199604009.htm
[24]	沈吉, 吴瑞金, 安芷生, 1998. 大布苏湖沉积剖面有机碳同位素特征与古环境. 湖泊科学, 10 (3): 8-12. https://www.cnki.com.cn/Article/CJFDTOTAL-FLKX199803001.htm
[25]	吴敬禄, Luecke, A., 李世杰, 等, 2000. 兴措湖沉积物有机碳及其同位素记录所揭示的近代环境与气候. 海洋地质与第四纪地质, 20 (4): 37-42. https://www.cnki.com.cn/Article/CJFDTOTAL-HYDZ200004008.htm
[26]	吴敬禄, 王苏民, 1996. 湖泊沉积物中有机碳同位素特征及其古气候. 海洋地质与第四纪地质, 16 (2): 103-108. https://www.cnki.com.cn/Article/CJFDTOTAL-HYDZ602.013.htm
[27]	张虎才, 1997. 元素表生地球化学特征及理论基础. 兰州: 兰州大学出版社.
[28]	张虎才, 马玉贞, 彭金兰, 等, 2002. 距今42-18ka BP腾格里沙漠古湖泊及环境. 科学通报, 47 (24): 1847-1857. https://www.cnki.com.cn/Article/CJFDTOTAL-KXTB200224001.htm
[29]	张虎才, Wüennemann, B., 1997. 腾格里沙漠晚更新世以来湖相沉积年代学及高湖面期的初步确定. 兰州大学学报, 33 (2): 97-91. https://www.cnki.com.cn/Article/CJFDTOTAL-LDZK702.018.htm
[30]	张玉芬, 李长安, 陈国金, 等, 2005. 江汉平原湖区周老镇钻孔磁化率和有机碳稳定同位素特征及其古气候意义. 地球科学——中国地质大学学报, 31 (1): 114-120. https://www.cnki.com.cn/Article/CJFDTOTAL-DQKX200501016.htm