我国西部高寒山区同位素生态水文研究进展

A Review of Isotope Ecohydrology in the Cold Regions of Western China

摘要

我国西部高寒山区是亚洲水塔，是重要的生态屏障区.随着环境同位素测试技术的发展和相关理论的成熟，稳定同位素技术已成为集示踪、整合和指示等多项功能于一体的技术.本文基于前人的研究结果，对我国西部高寒山区同位素生态水文研究进行了梳理和总结，表明西部高寒山区大气降水线为δD=7.44δ¹⁸O+5.23（R ²=0.86）.降水稳定同位素的温度效应从南向北呈现增加趋势，而降水量效应呈现相反的变化趋势.研究区水汽来源复杂，当温度效应小于0时，水汽来源由西南季风主导；温度效应为0~0.3时，水汽来源由西南季风和西风共同主导；温度效应大于0.3时，水汽来源由西风主导.不同水体受水源补给、环境作用等的影响存在差异性，使得各水体稳定同位素局地蒸发线的斜率大小依次为：河水>冰雪融水>地下水.西部高寒山区降水中δ¹⁸O海拔效应为-1.3‰/100m，河水δ¹⁸O海拔效应为-0.17‰/100m.研究区植被水分来源主要是土壤水，对水分的利用率与植被类型及区域环境密切相关.水汽再循环已成为区域降水水汽来源的重要组成部分.然而，随着生态文明建设这一国家重大战略的纵深推进，作为国家重要生态屏障的西部高寒山区，变化环境下生态水文过程正在发生深刻而又剧烈的改变，已对区域水资源安全、生态安全和可持续发展带来极大挑战，为寒区同位素生态水文学的发展提供了广阔舞台，未来亟需从观测、采样、模型和理论4个方面全面创新.

关键词

高寒山区 / 稳定同位素 / 环境效应 / 生态水文 / 环境保护

Key words

mountainous alpine / stable isotopes / environmental effects / eco-hydrology / environmental protection

0 引言

我国寒区特别是以青藏高原为主体的高原及周边高寒山地是世界上众多大江、大河的发源地，也是对气候变化响应极为敏感的关键地带（姚檀栋等，2013；程国栋和金会军，2013）.全球变化背景下，寒区水体多相态加速转换导致水文过程剧烈变化（Li et al.， 2019b），进而引起水循环的结构、速度、时空过程、要素组成及其水文与生态效应发生改变.因此寒区水文过程和生态过程研究已成为近年来全球变化与区域响应研究的焦点（Chen et al.， 2014；秦大河等，2014）.

同位素技术在水循环过程中的应用始于20世纪50年代（Dansgaard，1964）.1961年，国际原子能机构（IAEA）和世界气象组织（WMO）建立了全球大气降水同位素监测网（GNIP）. Craig（1961）得到全球降水线（global meteoric water line， 简称 GMWL）的线性关系：δ²H=8δ¹⁸O+10. Dansgaard （1964）最早分析了降水同位素与温度、纬度、高度、降水量和距海岸距离的关系.此后，氢氧稳定同位素技术在河川径流的研究中迅速展开（Turner et al.， 1992； Maurya et al.， 2011； Yang et al.， 2011； Kong and Pang， 2012； Pu et al.， 2013）.

我国同位素水文研究历经50多年，取得了重要的进展.1966年在珠穆朗玛峰的科学考察拉开了我国降水稳定同位素研究的序幕（Zhang et al.， 1973）.1983年以后我国先后有20多个监测站被纳入IAEA全球观测网，2004年开始建立中国大气降水同位素网络（简称CHNIP）（宋献方等，2020）.我国水体稳定同位素研究从最初的分析降水中δ¹⁸O和δD的时空变化特征（郑淑蕙等，1983； 田立德等，1998； Yao et al.， 1999； Tian et al.， 2007），到探究不同水体稳定同位素环境效应，讨论局地气象因子、水汽来源、局地水汽再循环等对水体稳定同位素的影响（Kong and Pang， 2012； Li et al.， 2014， 2015a， 2016a，， 2019a； Wang et al.， 2016； Gui et al.， 2020， 2022），各水体稳定同位素的研究也逐渐由现象描述、成因分析转向对产生同位素环境效应的深层机制的挖掘，对于各水体同位素及其环境效应以及影响机制的认识在不断提高，已有研究还量化了中国降水同位素温度效应和降水量效应的空间范围，并提出了空间覆盖完整的中国大气降水线方程（Wang et al.， 2022），同时水体稳定同位素为追踪水汽来源、反映全球和区域水循环机制与大气环流模式等研究提供了重要依据（Yao et al.， 2013；田立德等，2021）.

作为国家重要生态屏障的西部高寒山区，变化环境下生态水文过程正在发生深刻而又剧烈的改变，已对区域水资源安全、生态安全和可持续发展带来了挑战.西部高寒山区水资源变化直接影响到河川径流和“亚洲水塔”的水源涵养功能，在我国乃至全球尺度水循环、水平衡及水资源研究中具有重要的科学价值（Kang et al.， 2010；汤秋鸿等，2019）.目前，中国西部地区的同位素生态水文研究，已取得了不少成果，这些研究主要集中在单一的流域或单一站点（Wang et al.， 2016； Kong and Pang， 2016； Adhikari et al.， 2019； Li et al.， 2020）.因此本文基于前人的研究结果，综述了西部高寒山区不同水体稳定同位素时空变化特征以及水体同位素影响因素，总结降水稳定同位素的温度效应、降雨量效应、海拔效应等环境效应，并从径流分割、水汽来源、植物水分利用以及局地水汽再循环方面分析水体稳定同位素生态水文效应，以期为高寒区同位素水文过程的研究提供一定的参考.

1 研究区概况

我国西部高寒山区（73.67°~107.64°E，21.01°~49.01°N）（图1）是指海拔大于1 500 m的西部地区，主要分布在青藏高原及其邻近山区，区域气候复杂且水循环过程错综多变（Li et al.， 2019b），特殊的地形和气候等条件使其成为研究水循环的理想区域.西部高寒山区西起帕米尔高原，东至横断山脉，北部是阿尔泰山脉，南部为喜马拉雅山脉（Li et al.， 2019b），面积约为3.36×10⁶ km²，平均海拔超过 3 800 m，年均气温3 ℃左右，年均降水约306 mm（彭守璋，2019， 2020）.区内地势较高，积雪、冰川广布，主要分布在昆仑山山系、天山山系以及念青唐古拉山等山系，冰川数量共约48 571条，面积约51 766.08 km²，冰储量约4 494.00 ±175.93 km³（刘时银等，2015），同时分布大量的多年冻土，其中青藏高原地区多年冻土面积约为1.06×10⁶ km²（Zou et al.， 2017）.区内植被类型丰富，垂直分带性明显，包括高寒草原、高寒草甸、高山灌丛、落叶阔叶林、荒漠和温带草原等类型（石芳忠等，2018）.

2 数据来源

本文所用数据来源于国家青藏高原科学数据中心（https://data.tpdc.ac.cn/zh-hans/）和已发表文献（表1），共收集到降水同位素点124个、河水同位素点961个、地下水同位素点159个以及冰雪融水同位素点25个（图1）.

3 不同水体稳定同位素的时空特征

3.1　降水稳定同位素

3.1.1　局地大气降水线（LMWL）

全球自然水体中的δ¹⁸O和δD之间存在线性关系，Craig（1961）将其定义为全球大气水线（GMWL）：δD=8δ¹⁸O+10.不同区域由于气温、地形和地理位置的差异，降水线也存在不同（Liu et al.， 2007； Pang et al.， 2011； Guo et al.， 2015； Li et al.， 2020；Wu et al.， 2022）.西部高寒山区大气降水线为：δD=7.44δ¹⁸O+5.23（R ²=0.86，n=103）（图2），其斜率和截距均低于全球大气水线，以及我国西部地区、祁连山地区和我国一些湿润地区，但高于西北干旱区以及天山地区（表2）.这反映了降水同位素的区域差异性和水汽来源的不同，此外强烈的云下二次蒸发作用也会导致LMWL的斜率及截距均偏小（Wang et al.， 2016； Gui et al.， 2020）.西部高寒山区大气水线斜率和截距的空间分布如图3所示，LMWL的斜率在空间上差异较大.整体上，LMWL的斜率从西北到东南呈减小趋势，高值主要分布在昆仑山地区，低值分布在祁连山和阿尔泰山地区.同时在季风过渡段的祁连山地区的LMWL斜率与GMWL比较接近（7.99）（Gui et al.， 2020），而在非季风区的天山地区的LMWL明显低于GMWL（7.51）（孙从建等，2019）.受到水汽循环和蒸发过程影响，河西走廊地区的疏勒河流域、石羊河流域、托来河流域和排露沟流域大气水线的斜率和截距较低 （Li et al.， 2016d； Zhao et al.， 2016； 冯芳等，2017； 李永格等，2018）.这一现象说明：（1）水汽来源差异对西部高寒山区降水稳定同位素的影响较大；（2）蒸发作用和水汽再循环对该区域大气降水稳定同位素也产生了显著影响.

3.1.2　降水稳定同位素的时间分布特征

西部高寒山区降水稳定同位素值年际变化较大，其中降水中δ¹⁸O的变化范围为-18.6‰到-1.6‰，δD从-144.2‰变化到-5.2‰.，降水稳定同位素值较大的差异性表明研究区气候的极端性和水汽来源的复杂性.降水稳定同位素值在时间尺度上，也表现出一定的规律性.在青藏高原南部（Yao et al.， 2013）、天山地区（Pang et al.， 2011； Wang et al.， 2016）、祁连山地区（Li et al.， 2016c， 2016d， Gui et al.， 2020）、以及青藏高原北部（Tian et al.， 2007）等地区降水稳定同位素表现为夏、秋季偏正，冬、春季偏负的特征.喜马拉雅山降水中δ¹⁸O最大值出现在5月，最小值出现在9月或10月（章新平等，2001）.西南地区氢氧同位素组成则表现出夏半年偏低，冬半年偏高的特征（张贵玲等，2015）.降水稳定同位素组成的季节变化反映了水汽来源和水汽运输路径的季节性变化 （田立德等，1998； Tian et al.， 2001， 2007； Yao et al.， 2013； 田立德等，2021；Guo et al.， 2022）.

3.1.3　降水稳定同位素的空间分布特征

西部高寒山区降水稳定同位素整体上随着纬度的增加而增加（图4）.研究表明西北内陆地区降水中的δ¹⁸O远高于青藏高原南部地区，这与中亚腹部干旱的气候条件和大陆内部的局地水汽循环有关（田立德等，1998； Liu et al.， 2008b）.Liu et al.（2008b）发现在西部高寒区，氢氧同位素的低值区分布在青藏高原喜马拉雅山、阿尔泰山等山地，并指出这主要与显著的海拔效应有关.章新平和姚檀栋（1998）指出受到不同气团的影响，我国西北地区的大气降水中δ¹⁸O较高，而青藏高原南部的δ¹⁸O则较低，青藏高原南部地区较低的稳定同位素值一方面与海拔效应以及该地区水汽来源有关，另一方面与低纬度海洋水汽在喜马拉雅山南坡爬升过程中强烈的洗涤作用有关.因此西部高寒山区降水稳定同位素空间分布的差异性主要受到气候条件、水汽来源以及水汽再循环等因素的影响（Yao et al.， 2013； Kong and Pang， 2016； Gui et al.， 2020）.但需要强调的是，造成稳定同位素空间差异的原因不是单一的水汽输送或强烈的蒸发作用等，而是多种因素共同作用的结果.

3.2　河水稳定同位素

气候变化是影响高寒山区河道径流形成过程的主导因素（常启昕等，2022）.西部高寒山区河水的稳定同位素值存在区域差异性，河水δ¹⁸O的变化范围为-21.1‰到5.5‰，平均值为-10.2‰；河水中的δD从-157.4‰变化到-8.5‰，平均值为-86.7‰，在空间上由南到北、从西向东呈增加趋势（图5），高值主要分布在天山地区和祁连山地区，这些差异能够很好地解释区域气候和水文过程（Hren et al.， 2009； Bershaw et al.， 2012）.对青藏高原喜马拉雅山源头（Boral et al.， 2019）、雅鲁藏布江流域（刘忠方等，2008）、风火山流域（刘光生，2012）、北麓河流域（杨玉忠，2013）、长江源流域（李宗杰，2020）、慕士塔格地区（姚檀栋等， 2009）、祁连山地区（Li et al.， 2014， 2016a）、乌鲁木齐河流域（Sun et al.， 2015， 2016a）等地区河水中稳定同位素的研究表明，河水稳定同位素时空异质性主要受径流补给源、水体蒸发程度、局地水文过程等因素的交互影响.

西部高寒山区河水中δ¹⁸O随着海拔升高而逐渐降低（图6），河水δ¹⁸O海拔效应为-0.17‰/100m（P<0.01），反映出河水从高海拔到低海拔汇流过程中经历了强烈的蒸发作用，而且降水径流的不断汇入对河流稳定同位素浓度有一个明显的稀释作用（李宗杰，2020）.河水稳定同位素的海拔效应存在区域差异性，青藏高原地区拉萨河流域河水海拔梯度为-0.35‰/100m（余婷婷等，2010）.青藏高原喜马拉雅山南麓、青藏高原中部、青藏高原北部河水海拔梯度分别为-0.33‰/100m、-0.26‰/100m、-0.09‰/100m（刘琴，2014）.雅鲁藏布江流域河水海拔梯度为-0.21‰/100m（刘忠方等，2008）.李宗杰（2020）研究发现长江源地区在强消融期表现出明显的海拔效应（2016年： -0.16‰/100m； 2018年：-0.14‰/100m）.祁连山地区石羊河流域河水海拔梯度为-0.33‰/ 100m，黑河源区河水δ¹⁸O值随海拔升高，未展现出明显的海拔效应（Li et al.， 2016c）.天山吉木乃诸河河水中稳定同位素与海拔呈现正相关关系，海拔梯度为0.06‰/100m（宋梦媛等，2020）.

由于收集河水稳定同位素数据主要集中在青藏高原南部地区，存在区域不均匀性，因此笔者将研究区局地蒸发线（LEL）进行区域划分（图7），得到青藏高原地区河水蒸发线为δD=8.41δ¹⁸O+15.20， （R ²=0.95，n=412），祁连山地区河水蒸发线为δD=6.43δ¹⁸O+3.31，（R ²=0.86，n=96）以及天山地区河水蒸发线为δD=5.93δ¹⁸O-5.87，（R ²=0.91，n=36），在整个区域上，河水稳定同位素蒸发线的截距和斜率随着纬度的增加呈下降趋势，最高值在青藏高原地区，而低值在天山山区，再次体现出河水稳定同位素显著的空间差异性.青藏高原地区河水蒸发线与Hren et al.（2009）研究相近（δD=8.5δ¹⁸O+17.5），表明该区域河水除了受降水补给外，还受到局地再循环水汽和蒸发作用的较大影响.昆仑山地区、天山地区、祁连山地区和青海湖流域河水蒸发线的斜率均小于该区域大气降水线（崔步礼，2011；杨玉忠，2014；孙从建等，2019； Gui et al.， 2020），表明汇流过程中河水受到蒸发作用和降水补给的稀释作用.更为重要的是，各区域LEL与LMWL交点处的氢氧稳定同位素值与降水稳定同位素值最为接近，其次是地下水，表现出降水是河水的主要补给源.

3.3　地下水稳定同位素

本文中综述的地下水主要包括冻土层上水、井水、浅层地下水以及冻土地下冰等.研究区地下水稳定同位素值在空间上由西南向东北呈增加趋势，在祁连山地区地下水同位素值最为偏正，而在青藏高原南部同位素值较为偏负，这种差异性主要受地下水补给源以及土壤植被蒸散发的区域差异性影响（Li et al.， 2015a， 2016a， 2016b，， 2016c）.

西部高寒山区地下水LEL为δD=6.54δ¹⁸O‒11.04，（R ²=0.86，n=296），并且存在区域差异性，其明显较低的斜率和截距值反映了水体受到强烈的蒸发影响或者非平衡动力分馏（图8）.同时分析表明，冻土层上水和地下冰稳定同位素位于LMWL的右下部，反映了蒸散发过程和冻结过程中的同位素分馏效应（杨玉忠，2014； Li et al.， 2016a）.浅层地下水、井水和泉水较为接近大气降水线，这些特征表明寒区不同水源先充分混合为地下水后再补给河道，且河水入渗补给地下水以后还受到了蒸发的影响.更为重要的是，在青藏高原地区，地下水LEL与LMWL交点处的氢氧稳定同位素值与河水稳定同位素的值最为接近，而在天山和祁连山地区与降水稳定同位素值最为接近，表现出地下水补给源的区域差异性.

3.4　冰雪融水稳定同位素

西部高寒山区冰雪融水稳定同位素呈现出显著的差异性（图9a），冰雪融水δ¹⁸O的变化范围为从-68.1‰到-6.6‰，相比其他水体值较为偏负.在空间上冰雪融水稳定同位素值从西南到东北呈增加趋势.对乌鲁木齐河源1号冰川（李小飞，2013）、玉龙雪山（Pu et al.， 2020）、玉珠峰冰川、冬克玛底冰川和姜古迪如冰川（李宗杰，2020）、祁连山十一冰川（Li et al.， 2015b）等冰融水的研究表明，冰雪融水稳定同位素浓度受到消融强度、消融持续时间和新雪融水的影响，同时降雨或降雪的补给使得稳定同位素浓度更加贫化.如图9b所示青藏高原南部地区冰雪融水蒸发线为δD=8.37δ¹⁸O+24.04，（R ²=0.93，n=30），祁连山地区冰雪融水蒸发线为δD=7.21δ¹⁸O+13.86，（R ²=0.96，n=8），天山地区冰雪融水蒸发线为δD=8.35δ¹⁸O+21.71，（R ²=0.91，n=10），冰雪融水稳定同位素蒸发线的截距和斜率随着纬度的增加呈下降趋势，再次体现出冰雪融水稳定同位素显著的空间差异性.各区域冰雪融水的LEL斜率和截距与河水LEL极为接近，表明在低海拔出山口的冰川末端融水径流，冰雪融水是其主要的补给源.

4 稳定同位素的环境效应

4.1　温度效应

西部高寒山区δ¹⁸O与气温的相关系数空间分布如图10所示，整个研究区降水中δ¹⁸O的温度系数自东南向西北呈增加趋势.唐古拉山以南地区与青海湖地区温度与降水同位素呈负相关，不存在温度效应，但唐古拉山以北温度系数范围为0.01~1.36，存在温度效应.已有研究根据西南季风与西风带对降水δ¹⁸O影响，将青藏高原地区分为西风区、过渡区和季风区（姚檀栋等，2009；Yao et al.， 2013）.在青藏高原季风区的聂拉木和拉萨地区，夏季季风活动时期降水δ¹⁸O偏负，降水δ¹⁸O与气温之间不存在相关性（Tian et al.， 2003， 2007）；青藏高原过渡区的玉树、那曲、沱沱河、改则和狮泉河等地区，在全年尺度上，除了那曲以外，其他地区降水δ¹⁸O与气温存在一定的正相关（田立德等，1998， 2008）；西风区以西宁、德令哈、和田、慕士塔格为代表区，降水δ¹⁸O与气温存在显著的正相关关系（田立德等，2008）.在天山（王圣杰，2015）和祁连山等地区（Gui， et al.， 2020），降水δ¹⁸O与气温存在更为显著的正相关关系.

基于此，本文根据降水δ¹⁸O与气温的相关性大致界定了青藏高原季风向北的最大范围.当温度系数小于0时，几乎不存在温度效应，降水δ¹⁸O主要受到季风作用的影响，包括喜马拉雅山区、唐古拉山地区以及横断山脉地区等青藏高原南部地区；温度系数为0~0.3时，存在微弱的温度效应，降水δ¹⁸O主要受到季风和西风共同作用的影响，包括玉树、那曲、沱沱河等地区；温度系数大于0.3时，温度效应显著，降水δ¹⁸O主要受到西风作用的影响，包括天山、祁连山北部、阿尔泰山等地区.这一界限也是温度对降水稳定同位素分馏效应的边界.

4.2　海拔效应

西部高寒山区降水δ¹⁸O随着海拔升高而逐渐降低（图11），表现出明显的海拔效应，δ¹⁸O海拔梯度为-1.3‰/100m（P<0.01）；表明一方面在西部高寒山区高海拔采样点受云下蒸发的影响相对较低，降水中δ¹⁸O值较偏负；另一方面，高海拔区受到了较强的局地再循环水汽的影响.已有研究表明除同位素递减率较高的极端纬度地区外，全球降水δ¹⁸O垂直变化梯度的平均值为-0.28‰/100m（海拔5 000 m以下地区）（Poage and Chamberlain.， 2001），表3为西部高寒山区部分采样点δ¹⁸O的海拔效应，我国青藏高原地区、祁连山区、天山山区、横断山脉、喜马拉雅山脉等地降水稳定同位素总体上表现出明显的海拔效应（姚檀栋等，2009； Kumar et al.，2010；宋春林等，2015；Gui et al.， 2020； Li et al.， 2022）.但也有研究表明，天山背风一侧δ¹⁸O与海拔之间存在0.12‰/100m的正梯度，表现出相反的变化特征，这主要是由于受到局地云下二次蒸发和水分再循环过程的影响（Kong et al.， 2016）.同时受到水汽来源、水汽再循环和蒸发作用的影响，不同季节降水中δ¹⁸O的海拔梯度差异很大（王圣杰，2015； Li et al.， 2016d； Gui et al.， 2020）.祁连山区在夏半年和冬半年δ¹⁸O的海拔效应分别为-0.17‰/100m和-0.053‰/100m；天山地区海拔效应分别为-0.12‰/100m（夏半年）和0.03‰/100m（冬半年），乌鞘岭地区北坡年均、夏季和冬季δ¹⁸O的海拔梯度分别为-0.2‰/100m、-0.14‰/100m和-0.28‰/100m，在南坡，年均、夏季和冬季的δ¹⁸O海拔梯度分别为-0.32‰/100m、-0.29‰/100m和-0.38‰/100m.

4.3　降水量效应

我国西部高寒山区水汽来源复杂，在青藏高原低纬度显著受季风降水影响区，前人发现降水同位素存在“降水量效应”（Tian et al.， 2003； Yao et al.， 2013）.如表4所示，在青藏高原南部地区，降水量效应显著，并随着纬度的增加，降水量效应逐渐减小，而逐渐表现出温度效应.西北地区降水稳定同位素在季节尺度上并未表现出明显的降水量效应（Tian et al.， 2001）.王宁练等（2008）在祁连山单站点尺度发现了夏季降水的降水量效应.Wu et al. （2010）研究证实祁连山黑河流域大气降水稳定同位素浓度在降水事件尺度也展现出降水量效应.同时越往西北内陆深处，如疏勒河（郭小燕，2015）、新疆天山地区（王圣杰，2015）等，事件降水的降水量效应很弱，甚至不存在.

4.4　水汽来源

西部高寒山区水汽来源复杂，南北差异较大，其总体特征为：以青藏高原季风区为界，北部地区以西风水汽为主，南部以西南季风为主.前人研究表明西南季风达到北界的位置在青藏高原唐古拉山附近（田立德等，2006）.长江源区大气降水主要水汽来源为西南季风水汽（43%）、局地蒸发水汽（36%）及西风水汽（21%）（汪少勇等，2019）.西北干旱区水汽来源主要受西风控制.Wang et al.（2017）指出，中亚干旱地区的水汽来源主要是欧洲和中亚地区蒸发的陆地水分.王圣杰（2015）研究表明天山地区水汽来源主要是西风水汽.李捷等（2016）发现阿勒泰地区受到西风带水汽和北冰洋水汽的双重影响.祁连山地区主要受到西风的影响，约占祁连山地区所有降水事件的78%（Gui et al.， 2020）.祁连山北坡中段降水的水汽来源主要为西风水汽（张百娟等，2019）.石羊河流域全年基本以西风输送水汽为主，夏半年西风水汽输送约占70%左右，来自东南方向的水汽可占15%左右，来自偏北方向的水汽约占15%；而冬半年水汽运移路径基本上全部来自于西风水汽输送（袁瑞丰，2020）.我国西南地区降水的水汽主要来源于低纬度海洋（章新平等，2009）；贡嘎山地区雨季水汽来源较为复杂，主要有西风输送、东部季风和局地水汽内循环3个来源（宋春林，2015等）.

5 稳定同位素的生态水文效应

5.1　稳定同位素径流分割

多样的下垫面条件使得西部高寒山区径流补给来源多样.在高寒山区的水文循环研究中，同位素被广泛应用于流域径流分割（Liu et al.， 2008b； Maurya et al.， 2011； Kong and Pang， 2012； Pu et al.， 2013）.本文总结了高寒山区径流分割的主要成果（图12）.研究区不同补给源对径流的贡献具有区域差异性，总体上在流域出山口主要以降水补给为主，但在靠近冰川末端融水中，以冰雪融水补给为主.

祁连山地区降水对径流的补给率在20%~80%间，大多都在65%以上.黑河源区、八宝河流域和葫芦沟流域降水对河水的补给率分别为65%、71.9%和68%（Li et al.， 2014， 2015a， 2016c）.黑河源区马粪沟小流域径流主要为降水、冻土层上水和冰雪融水混合转化为地下水后补给（Yang et al.， 2011）.大气降水和冻土层上水对安远河径流的平均补给比例分别为76%和24%（Gui et al.， 2019）.黑河上游海拔3 600 m以上的地区产流量占出山径流量的80.2%（王宁练等，2008）.在大通河流域木里煤田聚乎更矿区，冻土层上水是河水的主要补给来源（邢剑伟等，2022）.

在天山地区，地下水对径流补给率在14%~87%间.降水和冰雪融水对天山乌鲁木齐河流域的径流贡献率为17.6%和14.7%，其余均为地下水补给（Sun et al.， 2015）.冰雪融水和地下水对榆树沟径流的贡献率分别为63%和37%（Wang et al.， 2015）.阿克苏河中36.0%~44.4%的径流来自冰川雪融水（Sun et al.， 2016b）.Fan et al. （2015）证实提孜那甫河冰川融水对径流的贡献为43%.Kumalak河协和拉水文站出山径流中冰雪融水的贡献率为57%~64%（Kong and Pang， 2012）.天山Kyrgyzstan河的径流有15%源自冰雪融水贡献，在消融季节这一贡献率将增大1.5~3倍，而且在有些冰川源头的小流域，冰雪融水的贡献量高达80%（Hagg et al.， 2007）.

玉龙雪山白水河流域冰雪融水对径流的贡献率为53.4%，其余来自降水（Pu et al.， 2013）.小海螺沟流域冰川融雪水占出口径流量的72.84%~80.30%（Xing et al.， 2015）.Liu et al.（2008a）在黑水河流域得出雪水和冰川融水的贡献在63.8%~92.6%之间.恒河流域冰川融雪、降水和地下水分别占径流的32%、53%和15%（Maurya et al.， 2011）.

5.2　植物水分来源

植物水分来源取决于植物获取水分的能力，同时也由环境中有效水的多少及其时空分布决定（刘飞等，2020）.在我国西部高寒山区，应用稳定同位素技术研究植物水分来源主要集中在塔里木河下游（陈亚宁等，2018）、青海湖地区（Wu et al.， 2018）、天山北麓地区（杨广等，2017）、祁连山黑河下游（Zhao et al.， 2020）以及柴达木盆地等地区（陈小丽等，2014）（表5）.地下水埋深是造成不同区域植被水分利用策略差异的根本原因（陈亚宁等，2018），同时与植被根系的分布有关（Fu et al.， 2014）.黑河下游平均地下水埋深在3 m左右，土壤浅层（1 m内）最大含水率可达29%（Fu et al.， 2014），塔里木河大部分地区的平均地下水埋深仍保持在6~8 m，地下2 m内土壤最大含水率仅15%（陈亚鹏等，2011），而天山北麓地下水潜水埋深波动范围为2~4 m（杨广等，2017）.植被水分来源主要是土壤水，不同土壤深度植被对水分的利用类型不同，同时植被对水分的利用率与植被类型及区域环境密切相关.

5.3　水汽再循环

气候变暖背景下，水汽再循环已成为区域降水水汽来源的重要组成部分（Cui et al.， 2015； Gui et al.， 2022）.当前人们在西部高寒山区应用稳定同位素示踪模型确定了部分地区的水汽再循环率.在青藏高原地区，崇测冰川和藏色岗日冰川水汽再循环率分别为15.0%±82.6%、24.7%±81.6%（An et al.， 2017），五道梁、风火山、沱沱河和唐古拉站的水汽再循环率分别为31.6%±4.8%、18.6%±3.7%、14%±3.8%和21.7%±3.9%（Zhu et al.， 2020）.青海湖和纳木错湖水汽再循环率为23.42%、28.4%~31.1%（Xu et al.， 2011； Cui et al.， 2015）.整个祁连山地区，蒸发水汽、蒸腾水汽和平流输送水汽对降水的贡献分别为8%、14%和78%，水汽再循环对大气降水的贡献量相当于71 mm降水（Gui et al.， 2022）.在内陆河源区，生长季内水汽再循环对区域降水的贡献率为27%，相当于117 mm降水（Li et al.， 2016c）；石羊河流域生长季水汽再循环对降水的贡献率为23%，相当于55.6 mm降水（Li et al.， 2016d）；在祁连山北坡，山区生长季水汽再循环对大气降水的贡献量相当于78 mm降水，走廊平原地区相当于16 mm降水，分别占同期降水量的24%和14.5% （Li et al.， 2019a）.在天山乌鲁木齐市水汽再循环对降水贡献率达16.2%，而石河子市等，其贡献率为5%左右（王圣杰，2015）.土壤与水体蒸发水汽对乌鲁木齐地区大气降水的贡献率可达15%左右（Kong et al.， 2013）.

6 总结与展望

综上，随着环境同位素测试技术的发展和相关理论的成熟，稳定同位素技术已成为集示踪、整合和指示等多项功能于一体的技术，而且具有检测快速、结果准确、无干扰等特点，使得水文学家成功地监测了诸多复杂水文过程的时空变化，目前已被广泛应用于寒区生态水文、水循环及水资源研究中，研究成果丰硕（图13）.然而，随着生态文明建设这一国家重大战略的纵深推进，作为国家重要生态屏障的西部高寒山区，变化环境下生态水文过程正在发生深刻而又剧烈的变化，已对区域水资源安全、生态安全和可持续发展带来了挑战，亟待深入探索，这又为寒区同位素生态水文学的发展提供了广阔舞台，未来亟需从以下几个方面深入推进：

（1）观测方面：系统而又合理的流域尺度水文过程观测是开展生态水文研究的重要基础.当前的观测研究在水文要素变化及其水文过程方面有了良好的积累，而水体稳定同位素也随着水循环过程发生不断的分馏，其时空模态及其环境效应随之发生显著改变，使得水体稳定同位素的局地性更加凸显，进而影响示踪研究的结果.因此，亟需依托建立在高寒山区的野外观测研究站，开展与水循环协同的水体稳定同位素分馏机制观测，目前位于祁连山南坡的高寒山区同位素生态水文与国家公园观测研究站正在开展类似的观测研究工作，有望为高寒山区系统的水体同位素联网观测研究开展探索性积累.

（2）采样方面：系统、科学与合理的各类样品采集是同位素生态水文学研究的基础，20世纪80年代以来随着同位素水文学的蓬勃发展，已经积累了大量的降水样品，并据此取得了一系列创新研究成果.然而，由于水循环本身的复杂性及其驱动机制的综合性，加之水文水资源效应的不确定性，使得仅通过降水同位素来开展寒区生态水文研究已凸显出诸多不足.因此，一方面，亟需从流域生态水文过程的基本规律入手，系统采集全要素样品，包括大气水汽、大气降水、河水、地下水、植物水、土壤水、冻土层上水、冰雪融水和积雪等；另一方面，还要科学设定采样的时空周期，确保全域尺度上高时空分辨率的样品积累，以便多要素、全过程示踪区域或流域尺度的生态水文过程.

（3）模型方面：在多手段、多学科综合与多要素、多领域集成研究背景下，稳定同位素示踪技术已成为寒区生态水文学的重要研究手段，该方法不仅可突破研究区的限制并拓展到整个区域尺度，而且作为实测数据可为模型验证提供强有力的数据支持，但对复杂的多参数水文模型与稳定同位素示踪的耦合研究还较少.因此，在能量平所衡‒水量平衡的生态水文模型框架体系下，耦合稳定同位素示踪模型、陆面过程模型和植物动态生长模型等，采用径流量、蒸散发与水体稳定同位素数据等共同约束模型参数，构建基于稳定同位素示踪的生态水文新模型，实现清晰、准确地刻画生态水文过程，是寒区同位素生态水文学研究的前沿领域和难点，也是亟待解决的关键科学问题.

（4）理论方面：首先应通过对过去研究成果的梳理总结，结合系统观测研究，凝练提升各水体稳定同位素在高寒山区的分馏演化机制，构建高寒山区水体同位素的分馏理论；探究各水体稳定同位素在不同时空尺度下的演化规律及模态，构建高寒山区水体同位素的时空变异理论；深入分析各水体稳定同位素与环境要素的辩证关系及演化机理，构建高寒山区水体同位素的环境效应理论；探究水体稳定同位素在示踪生态水文过程中的时空演化及驱动机制，凝练高寒山区水体稳定同位素的示踪理论；通过构建基于稳定同位素示踪的分布式生态水文模型，实现对过去生态水文过程变化的准确模拟及对未来变化的高精度预测，进而构建高寒山区基于水体稳定同位素的模型理论；由此创建高寒山区同位素水文学，并逐步将其发展成为集理论创新、技术革新与成果应用推陈出新的新兴交叉学科，成为支撑国家西部生态屏障建设的骨干学科，以及能够支撑生态文明建设体制机制创新的引领性学科.

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基金资助

国家自然科学基金区域发展联合基金重点项目(U22A20592)

国家重点研发计划项目专题(2020YFA0607702)

第二次青藏高原综合科学考察研究项目专题(2019QZKK0405)

中国科学院青年交叉团队项目(JCTD-2022-18)

中国科学院“西部之光”交叉团队项目‒重点实验室合作研究专项

甘肃省创新群体项目(20JR10RA038)