青藏高原东缘都江堰湖相沉积MIS3a阶段的快速气候变化记录

林晓; 常浩; 李云涛; 向树元; 王国灿

doi:10.3799/dqkx.2010.099

青藏高原东缘都江堰湖相沉积MIS3a阶段的快速气候变化记录

doi: 10.3799/dqkx.2010.099

林晓^{1, 2,},
常浩²,
李云涛²,
向树元^{2, 3},
王国灿^{2, 4}

1.
中国地质大学生物地质与环境地质教育部重点实验室, 湖北武汉 430074
2.
中国地质大学地球科学学院, 湖北武汉 430074
3.
中国地质大学地质调查研究院, 湖北武汉 430074
4.
中国地质大学地质过程与矿产资源国家重点实验室, 湖北武汉 430074

基金项目:

中国地质调查局项目 1212010610103

国家自然科学基金项目 40921062

国家自然科学基金项目 40830212

中国地质大学(武汉)优秀青年教师基金项目 CUGQNL0927

详细信息

作者简介:
林晓(1980-), 男, 讲师, 主要从事第四纪全球变化研究.E-mail: linxiao.cug@gmail.com

中图分类号: P534
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出版历程
- 收稿日期: 2010-05-31
- 刊出日期: 2010-09-01

Rapid Paleoclimate Changes during MIS3a Reflected by Lacustrine Deposits of Dujiangyan in the Eastern Margin of Qinghai-Tibet Plateau

LIN Xiao^{1, 2
,},
CHANG Hao²,
LI Yun-tao²,
XIANG Shu-yuan^{2, 3},
WANG Guo-can^{2, 4}

1.
Key Laboratory of Biogeology and Environmental Geology of Ministry of Education, China University of Geosciences, Wuhan 430074, China
2.
Faculty of Earth Sciences, China University of Geosciences, Wuhan 430074, China
3.
Geological Survey of China University of Geosciences, Wuhan 430074, China
4.
State Key Laboratory of Geological Process and Mineral Resources, China University of Geosciences, Wuhan 430074, China

摘要

摘要: 深海氧同位素第3阶段晚期(MIS3a)是青藏高原较为特殊的暖湿时期, 为了解这一时期高原东缘的气候变化细节, 利用AMS¹⁴C定年和粒度、总有机碳、正构烷烃等环境代用指标提取了四川都江堰湖相沉积剖面的相应记录.经过校正后的日历年龄显示此剖面沉积于43.6~34.6 kaBP期间, 记录了千年尺度的D-O旋回事件, 其分布时段分别为: DO11(43.6~41.8 kaBP), DO10(41.8~39.2 kaBP), DO9(39.2~37.7 kaBP), DO8(37.7~35.5 kaBP), DO7(35.5 kaBP~未见顶).该剖面总有机碳曲线与南京葫芦洞石笋和格陵兰冰心(GRIP)氧同位素曲线的对比表明, 该区域气候记录对全球高纬地区的冰量变化和亚洲季风演化具有响应; 而中纬度太阳辐射岁差对该区域气候波动的控制作用较强导致了细节上存在差异.
- 湖相沉积 /
- 古气候 /
- 都江堰 /
- D-O旋回
Abstract: The later phase of marine isotope stage 3 (i.e. MIS3a) on Qinghai-Tibet plateau was characterized by its special warm-humid climate. The constructed AMS¹⁴C calendar age-depth model, the component of n-alkanes, together with the grain size and total organic carbon (TOC) of lacustrine sediments in Dujiangyan S1 Section are used to elucidate the paleoclimate changes. The results indicate that rapid fluctuation on millennial scale was the main characteristic in the eastern margin of Qinghai-Tibet plateau during 43.6—34.6 kaBP. The Dansgaard-Oeschger events 11—7 can be reflected by these proxies, especially TOC. Comparison between TOC curve and oxygen isotope record from Hulu Cave and Greenland GRIP indicates that paleoclimate records in Dujiangyan respond to ice volume change in the high-latitude area and Asia monsoon oscillation. But the difference was shown because the influence of insolation values precession was strong in this area.
- lacustrine sediment /
- paleoclimate /
- Dujiangyan /
- Dansgaard-Oeschger oscillation

HTML全文

图 1 都江堰S1剖面地理位置示意

Fig. 1. Map showing the location of S1 Section in Dujiangyan City

下载: 全尺寸图片幻灯片

图 2 都江堰S1剖面粒度和碳酸盐含量变化

Fig. 2. Grain size and carbonate content of the lacustrine sediments of S1 Section in Dujiangyan City

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图 3 都江堰S1剖面总有机碳含量和正构烷烃参数变化

Fig. 3. TOC content and n-alkane proxies of the lacustrine S1 Section in Dujiangyan City

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图 4 都江堰S1剖面TOC与南京葫芦洞石笋和GRIP氧同位素曲线的对比

图中S1剖面与葫芦洞石笋采用同一时间标尺，GRIP冰心为另一时间标尺；数字代表D-O旋回，H4代表Heinrich事件，南京葫芦洞氧同位素取自MSD序列(Wang et al., 2001)；GRIP氧同位素数据来自http://www.ngdc.noaa.gov/paleo/icecore/greenland/summit/index.html；33°N辐射强度为夏季6~8月数据(Berger and Loutre, 1991)

Fig. 4. Comparison of TOC content in the S1 Section, δ¹⁸O of Hulu cave stalagmites in Nanjing and Greenland GRIP versus time

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表 1 都江堰湖相S1剖面AMS¹⁴C测年及日历年龄校正

Table 1. AMS¹⁴C dating and calendar calibration of the lacustrine S1 Section in Dujiangyan City

实验室编号	样品编号	深度 (cm)	AMS¹⁴C年龄 (aBP)	日历校正年龄 (aBP，距1 950 a)
BA07695	S1-1-1	1	29 780±140	34 611±140
BA07696	S1-1-121	121	33 040±195	37 824±567
BA07698	S1-2-36	313	39 420±290	43 565±321

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表 2 都江堰S1剖面正构烷烃含量、主峰碳和分子组成参数

Table 2. n-alkane's concentrations, main peaks and characteristic molecular proxies of the lacustrine S1 Section in Dujiangyan City

样品号	深度(cm)	年龄(kaBP)	总量^① (μg/g)	主峰碳	CPI₁^②	CPI₂^③	P_aq^④	TAR^⑤	C₃₁/(C₂₇₊₂₉)
1S1-1-1	1	34.61	0.33	C₂₃, C₁₇	1.75	1.99	0.65	1.13	0.286
S1-1-10	10	34.85	0.08	C₁₇, C₂₃	2.03	2.02	0.66	0.80	0.300
S1-1-20	20	35.12	0.13	C₂₃, C₁₇	1.93	1.79	0.68	1.14	0.276
S1-1-30	30	35.39	0.11	C₂₃	1.58	1.90	0.62	2.08	0.347
S1-1-40	40	35.65	0.22	C₂₃	1.51	1.93	0.60	1.95	0.347
S1-1-50	50	35.92	0.14	C₂₃	1.48	2.07	0.55	2.51	0.369
S1-1-60	60	36.19	0.23	C₂₃	1.54	2.02	0.58	2.24	0.387
S1-1-80	80	36.72	0.13	C₂₉	1.58	2.55	0.48	3.48	0.364
S1-1-90	90	36.99	0.28	C₂₃, C₁₇	1.74	1.63	0.71	1.04	0.258
S1-1-100	100	37.26	0.34	C₁₇	1.80	1.76	0.64	0.73	0.288
S1-1-110	110	37.53	0.38	C₁₇	2.36	2.15	0.55	0.94	0.331
S1-1-120	120	37.80	0.23	C₁₇	1.82	2.19	0.52	1.25	0.351
S1-1-130	130	38.09	0.23	C₂₉	1.50	2.34	0.51	2.77	0.350
S1-1-140	140	38.39	0.07	C₂₃, C₂₉	1.91	1.83	0.59	3.92	0.355
S1-1-150	150	38.69	0.31	C₁₇, C₂₃	1.56	1.77	0.64	0.96	0.296
S1-1-160	160	39.00	0.34	C₁₇, C₂₃	1.81	1.62	0.73	0.64	0.249
S1-1-170	170	39.30	0.25	C₂₃, C₂₉	1.51	2.04	0.58	1.65	0.300
S1-1-180	180	39.60	0.15	C₂₉	1.36	2.41	0.47	3.23	0.357
S1-1-190	190	39.90	0.25	C₂₉	1.43	2.47	0.44	2.77	0.398
S1-1-200	200	40.20	0.29	C₂₉	1.70	2.12	0.51	1.97	0.425
S1-1-210	210	40.50	0.27	C₂₉	1.52	1.70	0.63	1.41	0.324
S1-1-220	220	40.80	0.24	C₂₉	1.48	2.30	0.50	2.24	0.383
S1-1-230	230	41.10	0.19	C₂₉	1.53	2.47	0.49	2.80	0.428
S1-1-240	240	41.40	0.29	C₂₇	1.71	2.79	0.46	1.69	0.352
S1-2-10	260	42.00	0.06	C₃₁	0.48	3.95	0.28	13.47	0.657
S1-2-20	280	42.60	0.17	C₂₇	1.63	2.90	0.45	2.25	0.325
S1-2-30	300	43.20	0.10	C₂₇	1.54	2.56	0.49	3.07	0.376
S1-2-36	312	43.57	0.16	C₂₇	1.75	2.29	0.57	1.82	0.318
①烷烃总量=∑C_15-31；②CPI₁=(∑C_15-21奇/∑C_14-20偶+∑C_15-21奇/∑C_16-22偶)/2；③CPI₂=(∑C_23-33奇/∑C_22-32偶+ ∑C_23-33奇/∑C_24-34偶)/2；④P _aq=(C₂₃+C₂₅)/(C₂₃+C₂₅+C₂₉+C₃₁)；⑤TAR=(C₂₇+C₂₉+C₃₁)/(C₁₅+C₁₇+C₁₉).

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