Water isotope analysis for tracing ecosystem processes: measurement techniques, ecological applications, and future challenges
Xian-Hui TANG1, Yong-Le CHEN1,2, Fang LI1,2, Xin SONG,1,3,*1College of Life Sciences and Oceanography, Shenzhen University, Shenzhen, Guangdong 518060, China 2Key Laboratory of Optoelectronic Devices and Systems of Ministry of Education and Guangdong Province, College of Optoelectronic Engineering, Shenzhen University, Shenzhen, Guangdong 518060, China 3Shenzhen Key Laboratory of Marine Biotic Resources and Ecological Environment, Shenzhen University, Shenzhen, Guangdong 518060, China
Abstract Stable oxygen and hydrogen isotope analysis provides an important tool to trace, integrate or indicate water fluxes from leaf, whole-plant to ecosystem levels. Through measuring and analyzing the natural varitions in the hydrogen and oxygen isotope compositions of water from different components of ecosystem, we can partition evapotranspiration of ecosystem, determine source of plant water uptake, and study mechanism of leaf water isotope enrichment. As such, water isotope analysis has emerged as an indispensable technique to study the mechanism and ecological effects of different water cycle processes in ecosystem. In this paper, we briefly reviewed the history in development and application of water isotope analysis for terrestrial ecosystem studies, which then followed by more detailed introduction of the application principles and technical essentials. Furthermore, we reviewed progresses in diverse water-isotope based research field ranging from evapotranspiration partitioning, plant water uptake apportionment, sourcing of dew flux and precipitation vapor, to exploration leaf water isotope enrichment mechanisms and water-carbon coupling. Finally, we summarized technological and methodological challenges to be solved in the future ecological research, so as to fully realize the potential of water isotope analysis in various field of ecological research. Keywords：oxygen isotope;deuterium isotope;tracing;water cycle;ecosystem processes
PDF (1262KB)元数据多维度评价相关文章导出EndNote|Ris|Bibtex收藏本文 引用本文 汤显辉, 陈永乐, 李芳, 宋欣. 水同位素分析与生态系统过程示踪: 技术、应用以及未来挑战. 植物生态学报, 2020, 44(4): 350-359. DOI: 10.17521/cjpe.2019.0204 TANG Xian-Hui, CHEN Yong-Le, LI Fang, SONG Xin. Water isotope analysis for tracing ecosystem processes: measurement techniques, ecological applications, and future challenges. Chinese Journal of Plant Ecology, 2020, 44(4): 350-359. DOI: 10.17521/cjpe.2019.0204
水分是生态系统的核心因子, 影响和驱动着个体的生长、发育和繁殖, 以及生态系统的组成、演化和物质循环, 对于维持生态系统的功能和稳定具有重要意义(Chapin et al., 2011)。然而由于人类活动增加, 全球水循环和水资源格局发生剧烈变化, 水循环过程机理研究对于缓解水资源短缺、调节水循环以及提高生态系统服务功能具有重要意义。降水、植物蒸腾、土壤和水体蒸发、凝露等影响大气和生态系统水汽交换的生态水文过程中, 伴有不同程度的同位素分馏效应, 记录了不同的生态过程信息, 使得水同位素分析成为研究生态系统水循环的重要手段, 其实质是通过测量和分析生态系统关键组分如土壤、植物茎叶或大气中所含水分的氧氢同位素比值(δ)来探究生态系统水循环的过程、机制及生态学效应。例如, 量化土壤蒸发和叶片蒸腾水汽的δ值可为估算生态系统蒸散发来源(即蒸散发拆分)提供实现路径(Wen et al., 2016); 比较分析植物茎干木质部水分与其潜在水源的同位素关系可用来量化植物对不同来源水分的利用比例(Dawson & Ehleringer, 1991); 对叶片水同位素富集机理的探究则为解析树木年轮或叶蜡烷烃中所记录的气候或生理生态过程信息提供了理论基础(Cernusak et al., 2016)。
新窗口打开|下载原图ZIP|生成PPT 图1野外环境下簇状叶室与激光同位素仪相连测量蒸腾水汽同位素信号(δT)(引自Wang et al., 2012, 有改动)。实际测量中, 空气(水汽浓度为qA, 同位素信号为δA)以一定流速从叶室的进气口(5)进入叶室, 其与从叶室内叶片蒸腾出的水汽(T, δT)混合后(qM, δM)以同样的流速从叶室出气口(6)排出。进入叶室的空气以及排出叶室的混合气在经由电磁阀控制的多路控制系统(8)后按设定的测量周期(如4 min一个测量周期)交替通往水汽激光同位素仪(9)进行测量。在qA、δA、qM、δM以及气流流速都被测定的情况下, 通过进出叶室的水汽质量守恒可以计算出蒸腾通量, 再通过同位素质量守恒方程即可计算出δT。详细推导过程及注意事项参考Wang et al. (2012)。
Fig. 1Measurement of transpiration vapor isotopic signal (δT) by connecting conifer chamber with isotope ratio laser spectrometer in the field (cited from Wang et al., 2012 with change). In the measurement, the airs (vapor concentration qA and isotopic signal δA) enter the clustered chamber at a velocity from the inlet (5), mixing with the transpiration vapor from leaves (T, δT) in chamber, then (qM, δM) eject from the outlet (6) at the same flow rate. Passing by a solenoid valve controlled multi-channel system (8), the mixed airs are alternately connected to the isotope ratio laser spectrometer (9) in a set measurement period (e.g., a measurement period of 4 min). As qA, δA, qM, δA and flow rate are measured, the transpired vapor flux can be calculated by mass balance between vapor entering and outgoing the chamber, then δT of transpiration vapor can be calculated by isotopic mass balance equation. More details and derivational processes reference to Wang et al. (2012).
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VolkmannTHM, KühnhammerK, HerbstrittB, GesslerA, WeilerM (2016). A method for in situ monitoring of the isotope composition of tree xylem water using laser spectroscopy Plant, Cell & Environment, 39, 2055-2063. DOI:10.1111/pce.12725URLPMID:27260852 [本文引用: 1] Field studies analyzing the stable isotope composition of xylem water are providing important information on ecosystem water relations. However, the capacity of stable isotopes to characterize the functioning of plants in their environment has not been fully explored because of methodological constraints on the extent and resolution at which samples could be collected and analysed. Here, we introduce an in situ method offering the potential to continuously monitor the stable isotope composition of tree xylem water via its vapour phase using a commercial laser-based isotope analyser and compact microporous probes installed into the xylem. Our technique enables efficient high-frequency measurement with intervals of only a few minutes per sample while eliminating the need for costly and cumbersome destructive collection of plant material and laboratory-based processing. We present field observations of xylem water hydrogen and oxygen isotope compositions obtained over several days including a labelled irrigation event and compare them against results from concurrent destructive sampling with cryogenic distillation and mass spectrometric analysis. The data demonstrate that temporal changes as well as spatial patterns of integration in xylem water isotope composition can be resolved through direct measurement. The new technique can therefore present a valuable tool to study the hydraulic architecture and water utilization of trees.
WangLX, GoodSP, CaylorKK, CernusakLA (2012). Direct quantification of leaf transpiration isotopic composition Agricultural and Forest Meteorology, 154, 127-135. [本文引用: 5]
WangP, LiXY, WangL, WuX, HuX, FanY, TongY (2018). Divergent evapotranspiration partition dynamics between shrubs and grasses in a shrub-encroached steppe ecosystem New Phytologist, 219, 1325-1337. DOI:10.1111/nph.15237URLPMID:29862515 [本文引用: 1] Previous evapotranspiration (ET) partitioning studies have usually neglected competitions and interactions between antagonistic plant functional types. This study investigated whether shrubs and grasses have divergent ET partition dynamics impacted by different water-use patterns, canopy structures, and physiological properties in a shrub-encroached steppe ecosystem in Inner Mongolia, China. The soil water-use patterns of shrubs and grasses have been quantified by an isotopic tracing approach and coupled into an improved multisource energy balance model to partition ET fluxes into soil evaporation, grass transpiration, and shrub transpiration. The mean fractional contributions to total ET were 24 +/- 13%, 20 +/- 4%, and 56 +/- 16% for shrub transpiration, grass transpiration, and soil evaporation respectively during the growing season. Difference in ecohydrological connectivity and leaf development both contributed to divergent transpiration partitioning between shrubs and grasses. Shrub-encroachment processes result in larger changes in the ET components than in total ET flux, which could be well explained by changes in canopy resistance, an ecosystem function dominated by the interaction of soil water-use patterns and ecosystem structure. The analyses presented here highlight the crucial effects of vegetation structural changes on the processes of land-atmosphere interaction and climate feedback.
WangSJ, ZhangMJ, CheYJ, ChenFL, QiangF (2016). Contribution of recycled moisture to precipitation in oases of arid central Asia: a stable isotope approach Water Resources Research, 52, 3246-3257. [本文引用: 1]
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WassenaarLI, HendryMJ, ChostnerVL, LisGP (2008). High resolution pore water δ2H and δ18O measurements by H2O(liquid)-H2O(vapor) equilibration laser spectroscopy Environmental Science & Technology, 42, 9262-9267. DOI:10.1021/es802065sURLPMID:19174902 [本文引用: 1] A new H2O(liquid)-H2O(vapor) pore water equilibration and laser spectroscopy method provides a fast way to obtain accurate high resolution deltaD and delta18O profiles from single core samples from saturated and unsaturated geologic media. The precision and accuracy of the H2O(liquid)-H2O(vapor) equilibration method was comparable to or better than conventional IRMS-based methods, and it can be conducted on geologic cores that contain volumetric water contents as low as 5%. Significant advantages of the H2O(liquid)-H2O(vapor) pore water equilibration method and laser isotopic analysis method include dual hydrogen- and oxygen-isotope assays on single small core samples, low consumable and instrumentation costs, and the potential for field-based hydrogeologic profiling. A single core is sufficient to obtain detailed vertical isotopic depth profiles in geologic, soil, and lacustrine pore water, dramatically reducing the cost of obtaining pore water by conventional wells or physical water extraction methods. In addition, other inherent problems like contamination of wells by leakage and drilling fluids can be eliminated.
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Deuterium excess as a proxy for continental moisture recycling and plant transpiration 1 2014
Kinetic 17O effects in the hydrologic cycle: indirect evidence and implications 1 2004
... 氧元素在自然界有3种同位素, 由于17O自然丰度变异小且测量精度不够(林光辉, 2013), 以往17O在生态系统的研究应用很少.Meijer和Li (1998)通过电解水生成O2首次测量了液态水中的δ17O, 并认为由于δ17O和δ18O之间稳定的比例关系(0.528)而不能为生态系统提供更多有效信息.随着研究发现大气中O2的17O的非质量相关分馏可以用于光合作用和生物生产力的估算(Luz et al., 1999; Luz & Barkan, 2000; Blunier et al., 2002), d-excess可反演水源区温度和相对湿度信息(Merlivat & Jouzel, 1979; Gat, 1981), 17O-excess可用于恢复水源区相对湿度信息(Angert et al., 2004), 三氧同位素因为能提供更多的生态系统过程信息而在生态学研究中应用越来越广泛(Bao et al., 2016).目前水的δ17O的高精度测量主要是通过CoF3将水转化为O2, 再通过同位素比率质谱仪测量得到(Barkan & Luz, 2005), 也可以通过激光同位素仪实现测量和校准(Steig et al., 2014). ...
Triple oxygen isotopes: fundamental relationships and applications 1 2016
... 氧元素在自然界有3种同位素, 由于17O自然丰度变异小且测量精度不够(林光辉, 2013), 以往17O在生态系统的研究应用很少.Meijer和Li (1998)通过电解水生成O2首次测量了液态水中的δ17O, 并认为由于δ17O和δ18O之间稳定的比例关系(0.528)而不能为生态系统提供更多有效信息.随着研究发现大气中O2的17O的非质量相关分馏可以用于光合作用和生物生产力的估算(Luz et al., 1999; Luz & Barkan, 2000; Blunier et al., 2002), d-excess可反演水源区温度和相对湿度信息(Merlivat & Jouzel, 1979; Gat, 1981), 17O-excess可用于恢复水源区相对湿度信息(Angert et al., 2004), 三氧同位素因为能提供更多的生态系统过程信息而在生态学研究中应用越来越广泛(Bao et al., 2016).目前水的δ17O的高精度测量主要是通过CoF3将水转化为O2, 再通过同位素比率质谱仪测量得到(Barkan & Luz, 2005), 也可以通过激光同位素仪实现测量和校准(Steig et al., 2014). ...
Online CO2 and H2O oxygen isotope fractionation allows estimation of mesophyll conductance in C4 plants, and reveals that mesophyll conductance decreases as leaves age in both C4 and C3 plants 1 2016
X Water Worlds and how to investigate them: a review and future perspective on in situ measurements of water stable isotopes in soils and plants 1 2019
Deuterium and oxygen-18 variations in the ocean and marine atmosphere//Tongiorgi E. Proceedings of a Conference on Stable Isotopes in Oceanographic Studies and Palaeotemperatures 3 1965
... 自20世纪60年代以来, 水同位素理论和分析技术不断发展进步, 其在生态学中的应用大致可划分为以下三个不同阶段.第一阶段为水同位素研究的发轫和积累期(1966-1984年).在这一时期, 研究人员研发了低温真空抽提(Wershaw et al., 1970)水分提取技术, 为生态系统中不同“液态水”组分(如土壤和植物茎叶水)的测量清除了技术障碍.在此基础上, 围绕生态系统各组分水δ值的“普查式”测量揭示了以下重要的规律: 1)土壤垂直剖面存在明显的同位素梯度(Zimmermann et al., 1967; Fontes et al., 1983); 2)水分从根系进入植物茎干并在其木质部传输的过程中不存在同位素分馏(Zimmermann et al., 1967); 3)蒸腾导致叶片水的δ值显著高于茎干木质部水, 即叶片水的同位素相对富集(Craig & Gordon, 1965; Dongmann et al., 1974; Farris & Strain, 1978).第二阶段是对水同位素分馏机理认识不断深化的时期(1985-2004年)(Farquhar & Llyod, 1993; Roden et al., 2000), 也是基于同位素分析的生态学应用相继涌现的时期, 如植物水分来源区分(White et al., 1985; Dawson & Ehleringer, 1991), 蒸散发拆分(Moreira et al., 1997)等.第三阶段为水同位素测量技术的创新发展期(2005年至今).稳定同位素红外激光光谱技术的快速发展和推广使得同位素测量(特别是气态水的测量)变得前所未有地便捷(Lee et al., 2005), 这标志着“三高” (高频率、高通量、高精度)时代正式到来, 推动水同位素的研究从机理(Holloway-Phillips et al., 2016; Gerlein-Safdi et al., 2017)到应用(Wang et al., 2018; Dubbert & Werner, 2019)全方位走向繁荣.尽管水同位素分析在生态系统过程中已经有大量研究和进展, 但是水同位素测量技术进入创新发展期后, 对水同位素在生态系统过程中的应用、发展和未来挑战还缺乏系统论述. ...
... 氧元素在自然界有3种同位素, 由于17O自然丰度变异小且测量精度不够(林光辉, 2013), 以往17O在生态系统的研究应用很少.Meijer和Li (1998)通过电解水生成O2首次测量了液态水中的δ17O, 并认为由于δ17O和δ18O之间稳定的比例关系(0.528)而不能为生态系统提供更多有效信息.随着研究发现大气中O2的17O的非质量相关分馏可以用于光合作用和生物生产力的估算(Luz et al., 1999; Luz & Barkan, 2000; Blunier et al., 2002), d-excess可反演水源区温度和相对湿度信息(Merlivat & Jouzel, 1979; Gat, 1981), 17O-excess可用于恢复水源区相对湿度信息(Angert et al., 2004), 三氧同位素因为能提供更多的生态系统过程信息而在生态学研究中应用越来越广泛(Bao et al., 2016).目前水的δ17O的高精度测量主要是通过CoF3将水转化为O2, 再通过同位素比率质谱仪测量得到(Barkan & Luz, 2005), 也可以通过激光同位素仪实现测量和校准(Steig et al., 2014). ...
Atmospheric water balance The isotopic perspective 1 2000
... 同位素瑞利分馏模型可以示踪水汽来源(Dansgaard, 1964), 但是剩余水汽占气团的比例难以准确计算, 也没有考虑地表水体蒸发和云下二次蒸发对大气水汽δ值的影响, 只能模拟气团运行过程中分馏系数和气团内水汽含量变化等因素对降水δ值的影响(Gat, 2000).d-excess因为可以指示水汽源区相对湿度和温度等信息, 也被用于示踪水汽来源(Yamanaka et al., 2002; Pang et al., 2004).此外, δD和δ18O双同位素结合同位素质量平衡提供了更为简化的估算方法, Peng等(2011)研究认为, 假设降水水汽主要是土壤蒸发水汽、植物蒸腾水汽以及上风向平流输送的水汽混合后的结果, 如果3种来源的水汽混合均匀, 则可以建立一个三元混合模型, 通过上述蒸散发拆分中的方法可以确定土壤蒸发水汽的同位素值(δEv)和植物蒸腾水汽的同位素值(δTr), 降水的水汽同位素值(δPV)用降水同位素值经当地水汽蒸发线校准后计算得到(Gibson & Reid, 2014), 上风向平流输送的水汽同位素值(δadv)则可通过风向和两点之间的水汽同位素值得到(Wang et al., 2016).也有一些研究把降水和水汽同位素引入大气环流模型(Gao et al., 2011; Wang et al., 2015), 从更大尺度上确定水汽来源. ...
Effect of climate changes on the precipitation patterns and isotopic composition of water in a climate transition zone: case of the Eastern Mediterranean Sea area 1 1987
Uncertainties in the assessment of the isotopic composition of surface fluxes: a direct comparison of techniques using laser- based water vapor isotope analyzers 1 2012
... )(引自Wang et al., 2012, 有改动).实际测量中, 空气(水汽浓度为qA, 同位素信号为δA)以一定流速从叶室的进气口(5)进入叶室, 其与从叶室内叶片蒸腾出的水汽(T, δT)混合后(qM, δM)以同样的流速从叶室出气口(6)排出.进入叶室的空气以及排出叶室的混合气在经由电磁阀控制的多路控制系统(8)后按设定的测量周期(如4 min一个测量周期)交替通往水汽激光同位素仪(9)进行测量.在qA、δA、qM、δM以及气流流速都被测定的情况下, 通过进出叶室的水汽质量守恒可以计算出蒸腾通量, 再通过同位素质量守恒方程即可计算出δT.详细推导过程及注意事项参考Wang et al. (2012). Measurement of transpiration vapor isotopic signal (<i>δ</i><sub>T</sub>) by connecting conifer chamber with isotope ratio laser spectrometer in the field (cited from <xref ref-type="bibr" rid="b76">Wang <i>et al</i>., 2012</xref> with change). In the measurement, the airs (vapor concentration <i>q</i><sub>A</sub> and isotopic signal <i>δ</i><sub>A</sub>) enter the clustered chamber at a velocity from the inlet (5), mixing with the transpiration vapor from leaves (<i>T, δ</i><sub>T</sub>) in chamber, then (<i>q</i><sub>M</sub>, <i>δ</i><sub>M</sub>) eject from the outlet (6) at the same flow rate. Passing by a solenoid valve controlled multi-channel system (8), the mixed airs are alternately connected to the isotope ratio laser spectrometer (9) in a set measurement period (e.g., a measurement period of 4 min). As <i>q</i><sub>A</sub>, <i>δ</i><sub>A</sub>, <i>q</i><sub>M</sub>, <i>δ</i><sub>A</sub> and flow rate are measured, the transpired vapor flux can be calculated by mass balance between vapor entering and outgoing the chamber, then <i>δ</i><sub>T</sub> of transpiration vapor can be calculated by isotopic mass balance equation. More details and derivational processes reference to <xref ref-type="bibr" rid="b76">Wang <i>et al</i>. (2012)</xref>.Fig. 12.3 露水凝结来源拆分 露水主要是由低空近地层大气水汽、土壤蒸发水汽和植物蒸腾水汽在露点温度以下形成的凝露, 其同位素组成主要受3种来源δ值的影响, 但露水冷凝和蒸发的过程也会影响植物叶片水和大气水汽的同位素组成(Kim & Lee, 2011; Wen et al., 2012), 因此要实现三者拆分并不容易, Wen等(2012)研究认为, 低空近地层大气水汽通量向下, 而蒸散(土壤蒸发和植物蒸腾)的水汽通量向上, 可以通过通量廓线法得到生态系统净水汽通量和同位素值(δn), 通过露水与大气水汽的平衡分馏模型和冠层动力学分馏模型确定露水的同位素值(δd), 再用Craig-Gordon模型确定土壤蒸发和植物蒸腾的同位素值, 最后通过同位素质量守恒确定露水凝结不同来源的比例. ...
... .详细推导过程及注意事项参考Wang et al. (2012). Measurement of transpiration vapor isotopic signal (<i>δ</i><sub>T</sub>) by connecting conifer chamber with isotope ratio laser spectrometer in the field (cited from <xref ref-type="bibr" rid="b76">Wang <i>et al</i>., 2012</xref> with change). In the measurement, the airs (vapor concentration <i>q</i><sub>A</sub> and isotopic signal <i>δ</i><sub>A</sub>) enter the clustered chamber at a velocity from the inlet (5), mixing with the transpiration vapor from leaves (<i>T, δ</i><sub>T</sub>) in chamber, then (<i>q</i><sub>M</sub>, <i>δ</i><sub>M</sub>) eject from the outlet (6) at the same flow rate. Passing by a solenoid valve controlled multi-channel system (8), the mixed airs are alternately connected to the isotope ratio laser spectrometer (9) in a set measurement period (e.g., a measurement period of 4 min). As <i>q</i><sub>A</sub>, <i>δ</i><sub>A</sub>, <i>q</i><sub>M</sub>, <i>δ</i><sub>A</sub> and flow rate are measured, the transpired vapor flux can be calculated by mass balance between vapor entering and outgoing the chamber, then <i>δ</i><sub>T</sub> of transpiration vapor can be calculated by isotopic mass balance equation. More details and derivational processes reference to <xref ref-type="bibr" rid="b76">Wang <i>et al</i>. (2012)</xref>.Fig. 12.3 露水凝结来源拆分 露水主要是由低空近地层大气水汽、土壤蒸发水汽和植物蒸腾水汽在露点温度以下形成的凝露, 其同位素组成主要受3种来源δ值的影响, 但露水冷凝和蒸发的过程也会影响植物叶片水和大气水汽的同位素组成(Kim & Lee, 2011; Wen et al., 2012), 因此要实现三者拆分并不容易, Wen等(2012)研究认为, 低空近地层大气水汽通量向下, 而蒸散(土壤蒸发和植物蒸腾)的水汽通量向上, 可以通过通量廓线法得到生态系统净水汽通量和同位素值(δn), 通过露水与大气水汽的平衡分馏模型和冠层动力学分馏模型确定露水的同位素值(δd), 再用Craig-Gordon模型确定土壤蒸发和植物蒸腾的同位素值, 最后通过同位素质量守恒确定露水凝结不同来源的比例. ...
... ) by connecting conifer chamber with isotope ratio laser spectrometer in the field (cited from Wang et al., 2012 with change). In the measurement, the airs (vapor concentration qA and isotopic signal δA) enter the clustered chamber at a velocity from the inlet (5), mixing with the transpiration vapor from leaves (T, δT) in chamber, then (qM, δM) eject from the outlet (6) at the same flow rate. Passing by a solenoid valve controlled multi-channel system (8), the mixed airs are alternately connected to the isotope ratio laser spectrometer (9) in a set measurement period (e.g., a measurement period of 4 min). As qA, δA, qM, δA and flow rate are measured, the transpired vapor flux can be calculated by mass balance between vapor entering and outgoing the chamber, then δT of transpiration vapor can be calculated by isotopic mass balance equation. More details and derivational processes reference to Wang et al. (2012). Fig. 12.3 露水凝结来源拆分 露水主要是由低空近地层大气水汽、土壤蒸发水汽和植物蒸腾水汽在露点温度以下形成的凝露, 其同位素组成主要受3种来源δ值的影响, 但露水冷凝和蒸发的过程也会影响植物叶片水和大气水汽的同位素组成(Kim & Lee, 2011; Wen et al., 2012), 因此要实现三者拆分并不容易, Wen等(2012)研究认为, 低空近地层大气水汽通量向下, 而蒸散(土壤蒸发和植物蒸腾)的水汽通量向上, 可以通过通量廓线法得到生态系统净水汽通量和同位素值(δn), 通过露水与大气水汽的平衡分馏模型和冠层动力学分馏模型确定露水的同位素值(δd), 再用Craig-Gordon模型确定土壤蒸发和植物蒸腾的同位素值, 最后通过同位素质量守恒确定露水凝结不同来源的比例. ...
... of transpiration vapor can be calculated by isotopic mass balance equation. More details and derivational processes reference to Wang et al. (2012). Fig. 12.3 露水凝结来源拆分 露水主要是由低空近地层大气水汽、土壤蒸发水汽和植物蒸腾水汽在露点温度以下形成的凝露, 其同位素组成主要受3种来源δ值的影响, 但露水冷凝和蒸发的过程也会影响植物叶片水和大气水汽的同位素组成(Kim & Lee, 2011; Wen et al., 2012), 因此要实现三者拆分并不容易, Wen等(2012)研究认为, 低空近地层大气水汽通量向下, 而蒸散(土壤蒸发和植物蒸腾)的水汽通量向上, 可以通过通量廓线法得到生态系统净水汽通量和同位素值(δn), 通过露水与大气水汽的平衡分馏模型和冠层动力学分馏模型确定露水的同位素值(δd), 再用Craig-Gordon模型确定土壤蒸发和植物蒸腾的同位素值, 最后通过同位素质量守恒确定露水凝结不同来源的比例. ...
Divergent evapotranspiration partition dynamics between shrubs and grasses in a shrub-encroached steppe ecosystem 1 2018
... 自20世纪60年代以来, 水同位素理论和分析技术不断发展进步, 其在生态学中的应用大致可划分为以下三个不同阶段.第一阶段为水同位素研究的发轫和积累期(1966-1984年).在这一时期, 研究人员研发了低温真空抽提(Wershaw et al., 1970)水分提取技术, 为生态系统中不同“液态水”组分(如土壤和植物茎叶水)的测量清除了技术障碍.在此基础上, 围绕生态系统各组分水δ值的“普查式”测量揭示了以下重要的规律: 1)土壤垂直剖面存在明显的同位素梯度(Zimmermann et al., 1967; Fontes et al., 1983); 2)水分从根系进入植物茎干并在其木质部传输的过程中不存在同位素分馏(Zimmermann et al., 1967); 3)蒸腾导致叶片水的δ值显著高于茎干木质部水, 即叶片水的同位素相对富集(Craig & Gordon, 1965; Dongmann et al., 1974; Farris & Strain, 1978).第二阶段是对水同位素分馏机理认识不断深化的时期(1985-2004年)(Farquhar & Llyod, 1993; Roden et al., 2000), 也是基于同位素分析的生态学应用相继涌现的时期, 如植物水分来源区分(White et al., 1985; Dawson & Ehleringer, 1991), 蒸散发拆分(Moreira et al., 1997)等.第三阶段为水同位素测量技术的创新发展期(2005年至今).稳定同位素红外激光光谱技术的快速发展和推广使得同位素测量(特别是气态水的测量)变得前所未有地便捷(Lee et al., 2005), 这标志着“三高” (高频率、高通量、高精度)时代正式到来, 推动水同位素的研究从机理(Holloway-Phillips et al., 2016; Gerlein-Safdi et al., 2017)到应用(Wang et al., 2018; Dubbert & Werner, 2019)全方位走向繁荣.尽管水同位素分析在生态系统过程中已经有大量研究和进展, 但是水同位素测量技术进入创新发展期后, 对水同位素在生态系统过程中的应用、发展和未来挑战还缺乏系统论述. ...
Contribution of recycled moisture to precipitation in oases of arid central Asia: a stable isotope approach 1 2016
... 同位素瑞利分馏模型可以示踪水汽来源(Dansgaard, 1964), 但是剩余水汽占气团的比例难以准确计算, 也没有考虑地表水体蒸发和云下二次蒸发对大气水汽δ值的影响, 只能模拟气团运行过程中分馏系数和气团内水汽含量变化等因素对降水δ值的影响(Gat, 2000).d-excess因为可以指示水汽源区相对湿度和温度等信息, 也被用于示踪水汽来源(Yamanaka et al., 2002; Pang et al., 2004).此外, δD和δ18O双同位素结合同位素质量平衡提供了更为简化的估算方法, Peng等(2011)研究认为, 假设降水水汽主要是土壤蒸发水汽、植物蒸腾水汽以及上风向平流输送的水汽混合后的结果, 如果3种来源的水汽混合均匀, 则可以建立一个三元混合模型, 通过上述蒸散发拆分中的方法可以确定土壤蒸发水汽的同位素值(δEv)和植物蒸腾水汽的同位素值(δTr), 降水的水汽同位素值(δPV)用降水同位素值经当地水汽蒸发线校准后计算得到(Gibson & Reid, 2014), 上风向平流输送的水汽同位素值(δadv)则可通过风向和两点之间的水汽同位素值得到(Wang et al., 2016).也有一些研究把降水和水汽同位素引入大气环流模型(Gao et al., 2011; Wang et al., 2015), 从更大尺度上确定水汽来源. ...
Comparison of GCM-simulated isotopic compositions of precipitation in arid central Asia 1 2015
... 同位素瑞利分馏模型可以示踪水汽来源(Dansgaard, 1964), 但是剩余水汽占气团的比例难以准确计算, 也没有考虑地表水体蒸发和云下二次蒸发对大气水汽δ值的影响, 只能模拟气团运行过程中分馏系数和气团内水汽含量变化等因素对降水δ值的影响(Gat, 2000).d-excess因为可以指示水汽源区相对湿度和温度等信息, 也被用于示踪水汽来源(Yamanaka et al., 2002; Pang et al., 2004).此外, δD和δ18O双同位素结合同位素质量平衡提供了更为简化的估算方法, Peng等(2011)研究认为, 假设降水水汽主要是土壤蒸发水汽、植物蒸腾水汽以及上风向平流输送的水汽混合后的结果, 如果3种来源的水汽混合均匀, 则可以建立一个三元混合模型, 通过上述蒸散发拆分中的方法可以确定土壤蒸发水汽的同位素值(δEv)和植物蒸腾水汽的同位素值(δTr), 降水的水汽同位素值(δPV)用降水同位素值经当地水汽蒸发线校准后计算得到(Gibson & Reid, 2014), 上风向平流输送的水汽同位素值(δadv)则可通过风向和两点之间的水汽同位素值得到(Wang et al., 2016).也有一些研究把降水和水汽同位素引入大气环流模型(Gao et al., 2011; Wang et al., 2015), 从更大尺度上确定水汽来源. ...
High resolution pore water δ2H and δ18O measurements by H2O(liquid)-H2O(vapor) equilibration laser spectroscopy 1 2008
Footprint analysis using event-based isotope data for identifying source area of precipitated water 1 2002
... 同位素瑞利分馏模型可以示踪水汽来源(Dansgaard, 1964), 但是剩余水汽占气团的比例难以准确计算, 也没有考虑地表水体蒸发和云下二次蒸发对大气水汽δ值的影响, 只能模拟气团运行过程中分馏系数和气团内水汽含量变化等因素对降水δ值的影响(Gat, 2000).d-excess因为可以指示水汽源区相对湿度和温度等信息, 也被用于示踪水汽来源(Yamanaka et al., 2002; Pang et al., 2004).此外, δD和δ18O双同位素结合同位素质量平衡提供了更为简化的估算方法, Peng等(2011)研究认为, 假设降水水汽主要是土壤蒸发水汽、植物蒸腾水汽以及上风向平流输送的水汽混合后的结果, 如果3种来源的水汽混合均匀, 则可以建立一个三元混合模型, 通过上述蒸散发拆分中的方法可以确定土壤蒸发水汽的同位素值(δEv)和植物蒸腾水汽的同位素值(δTr), 降水的水汽同位素值(δPV)用降水同位素值经当地水汽蒸发线校准后计算得到(Gibson & Reid, 2014), 上风向平流输送的水汽同位素值(δadv)则可通过风向和两点之间的水汽同位素值得到(Wang et al., 2016).也有一些研究把降水和水汽同位素引入大气环流模型(Gao et al., 2011; Wang et al., 2015), 从更大尺度上确定水汽来源. ...
Soil-water movement and evapotranspiration: changes in the isotopic composition of the water//Geophysics in Vienna. Proceedings of the Symposium of Isotopes in Hydrology 3 1967
... 自20世纪60年代以来, 水同位素理论和分析技术不断发展进步, 其在生态学中的应用大致可划分为以下三个不同阶段.第一阶段为水同位素研究的发轫和积累期(1966-1984年).在这一时期, 研究人员研发了低温真空抽提(Wershaw et al., 1970)水分提取技术, 为生态系统中不同“液态水”组分(如土壤和植物茎叶水)的测量清除了技术障碍.在此基础上, 围绕生态系统各组分水δ值的“普查式”测量揭示了以下重要的规律: 1)土壤垂直剖面存在明显的同位素梯度(Zimmermann et al., 1967; Fontes et al., 1983); 2)水分从根系进入植物茎干并在其木质部传输的过程中不存在同位素分馏(Zimmermann et al., 1967); 3)蒸腾导致叶片水的δ值显著高于茎干木质部水, 即叶片水的同位素相对富集(Craig & Gordon, 1965; Dongmann et al., 1974; Farris & Strain, 1978).第二阶段是对水同位素分馏机理认识不断深化的时期(1985-2004年)(Farquhar & Llyod, 1993; Roden et al., 2000), 也是基于同位素分析的生态学应用相继涌现的时期, 如植物水分来源区分(White et al., 1985; Dawson & Ehleringer, 1991), 蒸散发拆分(Moreira et al., 1997)等.第三阶段为水同位素测量技术的创新发展期(2005年至今).稳定同位素红外激光光谱技术的快速发展和推广使得同位素测量(特别是气态水的测量)变得前所未有地便捷(Lee et al., 2005), 这标志着“三高” (高频率、高通量、高精度)时代正式到来, 推动水同位素的研究从机理(Holloway-Phillips et al., 2016; Gerlein-Safdi et al., 2017)到应用(Wang et al., 2018; Dubbert & Werner, 2019)全方位走向繁荣.尽管水同位素分析在生态系统过程中已经有大量研究和进展, 但是水同位素测量技术进入创新发展期后, 对水同位素在生态系统过程中的应用、发展和未来挑战还缺乏系统论述. ...
... ); 2)水分从根系进入植物茎干并在其木质部传输的过程中不存在同位素分馏(Zimmermann et al., 1967); 3)蒸腾导致叶片水的δ值显著高于茎干木质部水, 即叶片水的同位素相对富集(Craig & Gordon, 1965; Dongmann et al., 1974; Farris & Strain, 1978).第二阶段是对水同位素分馏机理认识不断深化的时期(1985-2004年)(Farquhar & Llyod, 1993; Roden et al., 2000), 也是基于同位素分析的生态学应用相继涌现的时期, 如植物水分来源区分(White et al., 1985; Dawson & Ehleringer, 1991), 蒸散发拆分(Moreira et al., 1997)等.第三阶段为水同位素测量技术的创新发展期(2005年至今).稳定同位素红外激光光谱技术的快速发展和推广使得同位素测量(特别是气态水的测量)变得前所未有地便捷(Lee et al., 2005), 这标志着“三高” (高频率、高通量、高精度)时代正式到来, 推动水同位素的研究从机理(Holloway-Phillips et al., 2016; Gerlein-Safdi et al., 2017)到应用(Wang et al., 2018; Dubbert & Werner, 2019)全方位走向繁荣.尽管水同位素分析在生态系统过程中已经有大量研究和进展, 但是水同位素测量技术进入创新发展期后, 对水同位素在生态系统过程中的应用、发展和未来挑战还缺乏系统论述. ...
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