拉萨河流域地表径流氢氧同位素空间分布特征

余婷婷; 甘义群; 周爱国; 刘存富; 刘运德; 李小倩; 蔡鹤生

doi:10.3799/dqkx.2010.101

拉萨河流域地表径流氢氧同位素空间分布特征

doi: 10.3799/dqkx.2010.101

余婷婷^{1, 2},
甘义群^{1, 2, ,},
周爱国^{1, 2},
刘存富^{1, 2},
刘运德^{1, 2},
李小倩^{1, 2},
蔡鹤生^{1, 2}

1.
中国地质大学环境学院, 湖北武汉 430074
2.
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

基金项目:

国家自然科学基金项目 40602030

国家自然科学基金项目 40772156

中国地质调查局项目 1212010818093

详细信息

作者简介:
余婷婷(1985-), 女, 博士研究生, 主要从事环境同位素领域的研究

通讯作者:
甘义群, E-mail: yiqungan@gmail.com

中图分类号: X141
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- 被引次数: 0
出版历程
- 收稿日期: 2010-05-31
- 刊出日期: 2010-09-01

Characteristics of Oxygen and Hydrogen Isotope Distribution of Surface Runoff in the Lhasa River Basin

YU Ting-ting^{1, 2},
GAN Yi-qun^{1, 2
, ,},
ZHOU Ai-guo^{1, 2},
LIU Cun-fu^{1, 2},
LIU Yun-de^{1, 2},
LI Xiao-qian^{1, 2},
CAI He-sheng^{1, 2}

1.
School of Environmental Studies, China University of Geosciences, Wuhan 430074, China
2.
Key Laboratory of Biogeology and Environmental Geology of Ministry of Education, China University of Geosciences, Wuhan 430074, China

摘要

摘要: 为了探析径流过程中稳定同位素变化特征及其控制因子, 利用2008年拉萨河流域地表径流中δ¹⁸O和δD的监测数据以及相关气象和水文资料, 初步研究了流域δ¹⁸O和δD的空间分布特征.研究发现: (1)拉萨河流域以大气降水为主要补给来源, 且干流体现了较明显的蒸发效应; (2)河水偏正的d过量参数特征指示了冰雪融水的补给特征; (3)季风降水期间, 拉萨河流域由高程效应和水平距离所造成的δ¹⁸O递减率约为0.16‰·(100 m)^-1; (4)大循环尺度下, 流域内河水呈现了明显的大陆效应.研究表明高海拔地区地表径流氧氘同位素分布特征能够有效示踪流域水文循环过程, 并提供古高度变化研究的稳定同位素证据.
- 氘过量参数(d值) /
- 拉萨河流域 /
- 地表径流 /
- 冰雪融水 /
- 氧同位素(δ¹⁸O) /
- 氢同位素(δD)
Abstract: The variation characteristics of oxygen and hydrogen isotopes in surface runoff of the Lhasa River basin was studied based on the observations of δ¹⁸O and δD in river water and related meteorological and hydrological data in 2008. The results indicate that: (1) precipitation is the main recharge source and that the Lhasa River has experienced strong evaporation; (2) positive d values indicate the snow melting water recharge; (3) during the Tibetan plateau summer monsoon period, the lapse rate of δ¹⁸O in river water is approximately 0.16‰·(100 m)^-1 due to the "altitude effect"; (4) in large-scale circulation, the basin water presents a significant continental effect. This study demonstrates that it is possible to trace the hydrological cycle with oxygen isotope and deuterium distribution in land runoff in the high altitude areas and to provide the stable isotopic evidence of the ancient latitude variation.
- deuterium excess parameter (d value) /
- Lhasa River basin /
- surface runoff /
- snow melting water /
- oxygen isotope (δ¹⁸O) /
- hydrogen isotope (δD)

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图 1 拉萨河流域采样位置示意

Fig. 1. Sketch map of water sample locations in the Lhasa River basin

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图 2 拉萨河流域河水的δ¹⁸O-δD组成关系

Fig. 2. Relationship between δ¹⁸O and δD distribution of waters in the Lhasa River basin

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图 3 拉萨河流域河水中δ¹⁸O值随高程的变化

Fig. 3. Lapse characteristics of δ¹⁸O along the Lhasa River

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表 1 拉萨河流域水体氢氧同位素组成

Table 1. δD and δ¹⁸O values of water samples collected from the Lhasa River basin

取样位置	编号	纬度	经度	高程(m)	δ¹⁸O_VSMOW(‰)	δD_VSMOW(‰)	d值(‰)
雅鲁藏布江	01	29°19′53″	90°41′39″	3 597	-17.76	-132.2	9.9
雅鲁藏布江	02	29°18′37″	90°45′35″	3 583	-17.69	-134.6	6.9
拉萨河干流	03	29°23′48″	90°52′58″	3 600	-17.58	-131.2	9.4
拉萨河干流	04	29°26′40″	90°55′46″	3 605	-17.49	-130.8	9.1
拉萨河干流	05	29°29′59″	90°56′20″	3 612	-17.59	-131.1	9.6
拉萨河干流	06	29°33′55″	90°59′34″	3 625	-17.98	-134.2	9.6
拉萨河干流	07	29°33′55″	90°59′39″	3 634	-17.38	-128.4	10.7
拉萨河干流	08	29°38′34″	91°06′50″	3 655	-17.32	-129.0	9.6
拉萨河干流	09	29°38′23″	91°09′39″	3 655	-17.23	-127.9	9.9
拉萨河干流	10	29°40′03″	91°18′04″	3 685	-17.25	-129.0	9.1
拉萨河干流	11	29°40′22″	91°23′16″	3 696	-17.26	-127.2	10.9
拉萨河干流	12	29°48′58″	91°33′36″	3 753	-17.47	-128.6	11.2
拉萨河干流	13	29°47′57″	91°35′59″	3 760	-17.41	-129.1	10.2
拉萨河干流	14	29°48′48″	91°40′08″	3 785	-17.42	-129.2	10.2
拉萨河干流	22	29°52′07″	91°45′27″	3 815	-18.01	-132.0	12.0
拉萨河干流	23	29°54′27″	91°48′42″	3 831	-17.83	-131.1	11.5
拉萨河干流	24	29°56′22″	91°51′52″	3 843	-17.89	-132.6	10.5
拉萨河干流	25	29°58′41″	91°52′51″	3 882	-17.80	-131.5	10.9
拉萨河干流	31	30°01′32″	90°51′16″	3 885	-17.63	-132.1	9.0
拉萨河干流	32	30°02′37″	91°49′11″	3 892	-17.59	-132.7	8.1
拉萨河干流	33	30°04′14″	91°46′32″	3 904	-17.77	-133.2	9.0
拉萨河干流	34	30°04′44″	91°43′55″	3 914	-17.43	-131.1	8.3
拉萨河干流	35	30°04′24″	91°37′48″	3 947	-17.44	-127.9	11.6
拉萨河干流	36	30°04′38″	91°34′21″	3 962	-17.37	-130.5	8.5
拉萨河干流	37	30°06′08″	91°29′25″	4 001	-17.24	-129.7	8.2
拉萨河干流	38	30°08′37″	91°24′52″	4 013	-17.21	-129.6	8.1
拉萨河干流	39	30°11′35″	91°20′45″	4 045	-16.95	-127.9	7.7
拉萨河干流	40	30°13′59″	91°21′59″	4 056	-16.86	-127.3	7.6
热振藏布	41	30°16′01″	91°23′21″	4 069	-16.67	-123.2	10.2
热振藏布	42	30°17′53″	91°27′46″	4 100	-16.82	-123.0	11.6
热振藏布	43	30°18′28″	91°31′07″	4 125	-16.64	-119.8	13.3
热振藏布	45	30°12′07″	91°20′08″	4 049	-17.18	-126.4	11.1
拉曲	46	30°15′26″	91°16′27″	4 076	-17.47	-127.7	12.0
拉曲	47	30°15′50″	91°12′49″	4 097	-17.36	-126.9	12.0
学绒藏布	26	30°00′06″	91°56′14″	3 899	-18.66	-137.8	11.5
学绒藏布	27	30°00′53″	92°01′07″	3 988	-18.59	-137.8	10.9
学绒藏布	28	30°01′37″	92°04′08″	4 047	-18.6	-140.2	8.6
学绒藏布	29	30°02′50″	92°07′45″	4 099	-18.69	-137.5	12.0
学绒藏布	30	30°05′23″	92°10′31″	4 179	-18.65	-134.8	14.5
墨竹曲	15	29°46′38″	91°52′28″	3 919	-18.12	-135.8	9.1
墨竹曲	16	29°45′23″	91°56′10″	3 981	-18.25	-136.2	9.8
墨竹曲	17	29°42′57″	92°02′25″	4 093	-18.33	-136.7	9.9
墨竹曲	18	29°42′38″	92°09′59″	4 256	-18.44	-137.7	9.8
墨竹曲	19	29°42′35″	92°14′52″	4 372	-18.32	-137.6	9.0
墨竹曲	20	29°41′23″	92°16′14″	4 398	-19.19	-143.4	10.1
墨竹曲	21	29°50′04″	91°44′37″	3 814	-18.24	-135.2	10.7
堆龙曲	50	29°40′15″	90°54′53″	3 692	-18.03	-133.4	10.9
堆龙曲	51	29°45′22″	90°47′11″	3 807	-18.31	-134.0	12.5
堆龙曲	52	29°55′11″	90°42′54″	3 935	-18.18	-135.0	10.5
堆龙曲	53	30°04′58″	90°33′31″	4 264	-18.41	-133.0	14.3

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表 2 阿尼玛卿山雪水及西藏羊八井河水氢氧同位素组成

Table 2. δD and δ¹⁸O values of the melt-water samples collected from the Animaqing Mountain and the river water samples from Yangbajing

样品编号	高程(m)	δ¹⁸O(‰)	δD(‰)	d值(‰)
山-1^a	4 700	-13.41	-87.0	20.3
山-2^a	5 700	-8.68	-49.0	20.4
山-3^a	6 050	-10.67	-65.2	20.2
W-24^b	/	-19.98	-141.0	18.8
W-78^b	/	-19.28	-135.5	18.7
注：a.雪水样，1983年，王勇峰取自阿尼玛卿山；b.河水样，选自卫克勤等(1983).

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