青藏高原古高程定量恢复研究进展

doi:10.11867/j.issn.1001-8166.2015.03.0334

目前在青藏高原使用的古高程定量恢复的方法有：氧同位素古高程计（包含热动力学模型和经验模型）、△47古温度—古高程计、氢同位素古高程计、古植物古高程计（包含共存分析法、叶相分析法）和古环境分析。详细分析了各古高程计的原理、应用条件、影响因素和优缺点,进一步总结了各种研究方法取得的成果和存在的问题,探讨了各研究方法在青藏高原定量古高程研究方向的应用潜力和发展前景,并对完善现有的古高程计和今后开发新的古高程计提出相关建议。关键词：青藏高原;古高程; 定量研究;新生代

关键词: Tibetan Plateau, Paleoelevation, Quantitative research, Cenozoic.

Quantitative estimation of paleoelevation is crucial to constrain uplift history of the Tibetan Plateau. So far, there are four kinds of paleoaltimeter used to reveal Cenozoic paleoelevation of the Tibetan Plateau, including oxygen-isotope paleoaltimeter, △47 paleotemperaturepaleoaltimeter, Hydrogen-isotope paleoaltimeter, Paleobotanic paleoaltimeter, and Analysis of paleoenvironment. The oxygen-isotope paleoaltimeter, which is based on the relationship between the oxygen isotope value (¹⁸O) of surface water and elevation, includes empirical relationship equation and model relationship equation. △47 paleotemperature-paleoaltimeter is a new approach to reconstruct paleoelevation, which has been used in just one position in Tibet. Paleobotanic paleoaltimeter contains co-existence analysis and leaf physiognomic approach, and Analysis of paleoenvironment is a semi-quantitative method. Through detailed comparison of various principles, application condition, influencing factors, and pros-cons of the different paleoaltimeters, we focused on summarizing achievements and problems of these research methods, and further discussed their application potential and prospects. In the future work, we need to pay more attention to obtain new modern data to improve the above paleoaltimeters and introduce new paleoaltimeters.

Key words: Tibetan Plateau, Paleoelevation, Quantitative research, Cenozoic.

中图分类号:

P542

图1 青藏高原定量古高程恢复分布(现代海拔边界据文献 ^{[

5
]}修改,分水岭据文献 ^{[

6
]};投点数据见表1 ;地层分区据文献 ^{[

7
]}修改])

Fig.1 Distribution of paleoelevation dates in Qinghai-Tibet Plateau (modern altitude boundary modified after reference ^{[

3
]}; watershed mountains after reference ^{[

4
]}; paleoelevation date refer to Table 1 ; stratigraphy division after reference ^{[

7
]})

表1 青藏高原定量古高程恢复统计表

Table 1 Paleoelevation dates of Qinghai-Tibet Plateau

代号	地点	时代	研究方法	材料	高程结果	参考文献
LZ	林周盆地	60~48 Ma	热动力学模型	古土壤、湖相碳酸盐、泥灰岩	（4 500±400） m	^{[ 1 ]}
H	黑狐岭	51~28 Ma	热动力学模型经验公式	土壤、湖相碳酸盐、泥灰岩	>5 000 m	^{[ 8 ]}
Z₁	扎达盆地	9.2 Ma	热动力学模型	腹足类壳体化石	>6000 m	^{[ 9 ]}
Z₂	扎达盆地	中新世	热动力学模型	腹足类壳体化石	>现在高程1 000~1 500 m	^{[ 10 ]}
LP₁	伦坡拉盆地	35 Ma	热动力学模型	土壤、湖相碳酸盐	4260+475/-575 m	^{[ 11 ]}
Oi₁	南木林盆地	15 Ma	热动力学模型	土壤碳酸盐	5200+1370/-605 m	^{[ 12 ]}
F	风火山盆地	中新世	热动力学模型	湖相碳酸盐	2040+1460/-1130 m	^{[ 13 ]}
T	塔口拉地堑	晚中新世	经验公式	湖相、土壤碳酸盐	5450±897 m	^{[ 14 ]}
LM	黎明镇	晚始新世	经验公式	古土壤碳酸盐	3300±450 m	^{[ 15 ]}
Z₃	扎达盆地	9~4 Ma	△47古温度-古高程计	湖相、土壤碳酸盐	5400±500 m	^{[ 16 ]}
Q	柴达木盆地北缘	15 Ma以来	氢同位素	植物脂类化石	10.4 Ma达到现在高程	^{[ 17 ]}
E	珠穆朗玛峰	早中新世晚期	氢同位素	变质岩中含水矿物	（5 100±400） m （5 400±350） m	^{[ 18 ]}
Hh	可可西里盆地	始新世—中新世	氢同位素	植物脂类化石	隆升1 700~2 600 m	^{[ 19 ]}
LP₂	伦坡拉盆地	始新世中新世	氢同位素	植物脂类化石	3 600~4 100 m(始新世) 4 500~4 900 m(中新世)	^{[ 19 ]}
LP₃	伦坡拉盆地	25.5~19.8 Ma	碳、氢同位素	植物脂类化石	（2 770±530 ）m （3 040±560） m	^{[ 20 ]}
LP₄	伦坡拉盆地	25.5~19.8 Ma	共存分析	孢粉化石	（3 190±100） m	^{[ 21 ]}
X	希夏邦马峰	上新世	共存分析	孢粉化石	2 500~3 500 m	^{[ 2 , 22 ]}
Oi₂	南木林盆地	中新世	共存分析	孢粉化石	2 500~3 000 m	^{[ 22 ]}
Oi₃	南木林盆地	15 Ma	叶相分析	叶片化石	4689±895 m	^{[ 23 ]}
Z₄	扎达盆地	4.2~3.1 Ma	古环境分析	食草动物牙齿化石	>2 500 m	^{[ 24 ]}
KL	昆仑山	3~2 Ma	古环境分析	食草动物牙齿化石	隆升（2 700±1 600） m	^{[ 25 ]}
Gy	吉隆盆地	7 Ma	古环境分析	食草动物牙齿化石	<2900~3400 m	^{[ 26 ]}
K	凯拉斯盆地	26 Ma	古环境分析	湖相、土壤碳酸盐	>4 500 m	^{[ 27 ]}
N	尼玛盆地	26~24 Ma	古环境分析	湖相、土壤碳酸盐	4 500~5 000 m	^{[ 5 ]}
LP₅	伦坡拉盆地	18~16 Ma	古环境恢复	哺乳动物化石	约3 000 m	^{[ 28 ]}

表1 青藏高原定量古高程恢复统计表

Table 1 Paleoelevation dates of Qinghai-Tibet Plateau

代号	地点	时代	研究方法	材料	高程结果	参考文献
LZ	林周盆地	60~48 Ma	热动力学模型	古土壤、湖相碳酸盐、泥灰岩	（4 500±400） m	^{[ 1 ]}
H	黑狐岭	51~28 Ma	热动力学模型经验公式	土壤、湖相碳酸盐、泥灰岩	>5 000 m	^{[ 8 ]}
Z₁	扎达盆地	9.2 Ma	热动力学模型	腹足类壳体化石	>6000 m	^{[ 9 ]}
Z₂	扎达盆地	中新世	热动力学模型	腹足类壳体化石	>现在高程1 000~1 500 m	^{[ 10 ]}
LP₁	伦坡拉盆地	35 Ma	热动力学模型	土壤、湖相碳酸盐	4260+475/-575 m	^{[ 11 ]}
Oi₁	南木林盆地	15 Ma	热动力学模型	土壤碳酸盐	5200+1370/-605 m	^{[ 12 ]}
F	风火山盆地	中新世	热动力学模型	湖相碳酸盐	2040+1460/-1130 m	^{[ 13 ]}
T	塔口拉地堑	晚中新世	经验公式	湖相、土壤碳酸盐	5450±897 m	^{[ 14 ]}
LM	黎明镇	晚始新世	经验公式	古土壤碳酸盐	3300±450 m	^{[ 15 ]}
Z₃	扎达盆地	9~4 Ma	△47古温度-古高程计	湖相、土壤碳酸盐	5400±500 m	^{[ 16 ]}
Q	柴达木盆地北缘	15 Ma以来	氢同位素	植物脂类化石	10.4 Ma达到现在高程	^{[ 17 ]}
E	珠穆朗玛峰	早中新世晚期	氢同位素	变质岩中含水矿物	（5 100±400） m （5 400±350） m	^{[ 18 ]}
Hh	可可西里盆地	始新世—中新世	氢同位素	植物脂类化石	隆升1 700~2 600 m	^{[ 19 ]}
LP₂	伦坡拉盆地	始新世中新世	氢同位素	植物脂类化石	3 600~4 100 m(始新世) 4 500~4 900 m(中新世)	^{[ 19 ]}
LP₃	伦坡拉盆地	25.5~19.8 Ma	碳、氢同位素	植物脂类化石	（2 770±530 ）m （3 040±560） m	^{[ 20 ]}
LP₄	伦坡拉盆地	25.5~19.8 Ma	共存分析	孢粉化石	（3 190±100） m	^{[ 21 ]}
X	希夏邦马峰	上新世	共存分析	孢粉化石	2 500~3 500 m	^{[ 2 , 22 ]}
Oi₂	南木林盆地	中新世	共存分析	孢粉化石	2 500~3 000 m	^{[ 22 ]}
Oi₃	南木林盆地	15 Ma	叶相分析	叶片化石	4689±895 m	^{[ 23 ]}
Z₄	扎达盆地	4.2~3.1 Ma	古环境分析	食草动物牙齿化石	>2 500 m	^{[ 24 ]}
KL	昆仑山	3~2 Ma	古环境分析	食草动物牙齿化石	隆升（2 700±1 600） m	^{[ 25 ]}
Gy	吉隆盆地	7 Ma	古环境分析	食草动物牙齿化石	<2900~3400 m	^{[ 26 ]}
K	凯拉斯盆地	26 Ma	古环境分析	湖相、土壤碳酸盐	>4 500 m	^{[ 27 ]}
N	尼玛盆地	26~24 Ma	古环境分析	湖相、土壤碳酸盐	4 500~5 000 m	^{[ 5 ]}
LP₅	伦坡拉盆地	18~16 Ma	古环境恢复	哺乳动物化石	约3 000 m	^{[ 28 ]}

图2 Kali Gandaki流域河流水δ ¹⁸O与高程的关系图（据参考文献 ^{[

4
]}修改）

Fig.2. δ ¹⁸O vs. altitude for Kali Gandaki tributaries (modified from reference ^{[

4
]})

图3 塔口拉地堑中碳酸盐岩中双壳类化石的生长纹层 ^{[

43
]}

Fig.3 Annual growth bands of fossil bivalves in carbonate from Thakholagraben ^{[

43
]}

图4 氢同位素古高程计关系式（a）贡嘎山植被脂类化石中δD_wax值与土壤水中δD_p值线性关系; （b）植被脂类化石中δD_wax值与海拔二次拟合关系^{[

60
]}

Fig.4 Equations of hydrogen-based istopepaleoelevation （a）Correlations of n-alkane δD_wax with predicted δDp; （b） Correlations of n-alkane δD_wax with altitude^{[

60
]}

图5 植被脂类中氢同位素影响因素示意图 ^{[

69
]}

Fig.5 Schematic showing the model predictions for the effects on plant-wax n-alkane δD values ^{[

69
]}

图6 青藏高原定量古高程恢复结果对比（现代海拔 ^{[

17
]};切线位置见图1 ;古高程数据来源见表1 ）

Fig.6 Comparison of paleoelevation date in Qinghai-Tibet Plateau. (modern altitude ^{[

17
]}; the location of topographic cross-section refer to Fig.1 ; paleoelevation refer to Table 1 )

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Research Progress of Quantitative Paleoelevation Reconstruction of Tibetan Plateau