疏勒河流域地下水~（14）C年龄校正
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摘要
地下水准确年龄的获取一直是水文地质学研究的热点和难点,受埋藏条件限制,水文地质参数获取困难,使得传统方法获取的地下水运移信息十分有限。环境同位素作为水体本身组成或溶解成分自始至终都随水体演化,从而成为追踪水文过程有力的工具,其中,放射性同位素14C就是估计地下水年龄最重要的手段,然而,由于地下水溶解无机碳来源复杂,如何恢复14C初始值成为地下水14C年龄校正的关键。论文针对这一问题,选取疏勒河流域为研究对象,通过分析微量元素特征以及离子相互关系,识别了研究区不同层位地下水发生的地球化学反应及其影响因子；对研究区水化学场、同位素场分析,结合水文地质条件,划分了研究区地下水典型水流系统；在以上研究的基础上,运用反向水文地球化学模拟技术,定量识别出不同地带地下水演化过程中14C浓度变化的主要反应路径及其影响程度,从而对地下水14C年龄进行了校正,主要成果如下：
疏勒河流域地下水从山前隔壁带到中游细土平原区再到下游荒漠区,地下水以碱土金属离子、弱酸根离子为优势成分逐渐演替为以碱金属、强酸根离子为主。阳离子由无明显离子特征过渡到以Na++K+为主,阴离子则从HCO3-过渡到无明显特征,最后向S042-型水演化。经过主成分分析,提取了两个主成分,其方差贡献率分别为58.159%和14.621%,分别指示了蒸发浓缩作用、溶滤作用以及地下水演化的碱性环境和同离子效应。
地下水87Sr/86Sr介于0.711041到0.714029,与蒸发岩特征值很接近,Sr2+分别于Ca2+和S042-具有很好的相互关系,说明研究区地下水发生了明显的蒸发岩溶解反应。结合离子相互关系,发现芒硝、石膏、岩盐、碳酸盐溶解沉淀,反向阳离子交换是研究区地下水主要的地球化学过程。根据Cl-与K+、HCO3-以及N03-关系识别出人为活动、补给水源等作用对潜水水化学演化影响较大。
玉门—踏实盆地地下水稳定同位素在垂向无明显分异,潜水与承压水联系紧密,交换频繁。瓜州盆地地下水随着井深的增加,稳定同位素在潜水和承压水中呈现不同的变化规律,呈现出同位素分层特点,指示各含水层岩组垂向水力联系较弱,地下水主要以水平径流为主。敦煌盆地下游承压水同位素垂向变化与瓜州盆地相似,但是在60m深度处潜水与承压水出现重叠分布,指示了在含水层过渡地带上下含水层发生联系。
瓜州水流路径GZ11-GZ10,GZ04-X01,敦煌DH01-DH03反向地球化学模拟结果显示,三条路径上均发生了阳离子交换,岩盐,芒硝的溶解反应,GZ11-GZ10路径上发生了明显的蒸发效应,蒸发因子为1.177,二氧化碳的溶解升高了地下水14C的浓度,该路径上地下水的运移时间约为740a。GZ04-X01路径上文石的溶解,Ca/Na、Mg/Na交换是促使碳酸盐变化的主要原因,该过程导致了起点地下水14C被稀释了3倍多,径流路径上的传输时间约为10281a。敦煌DH01-DH03水流路径上发生了混合作用,方解石,文石都参与了反应路径,但对地下水放射性碳影响不大,从起点到终点地下水运移经历了约12851a。
研究区第四纪地下水年龄分布范围较大,从现代到数万年,大多数承压水年龄分布在3000-7000年间,反映了中全新世大暖期暖湿的气候对地下水补给的重要作用。瓜州盆地东部补给区潜水很年轻,循环速率为16.2-17.5m/a。各盆地细土平原区深层潜水从现代到2000年不等,说明深部地下水循环交替也比较迟缓。研究区承压水普遍年龄很老,从3000年到1.6万年,地下水的循环速度介于2.4-3.7m/a,更新能力较差。
Groundwater age determining has been a focus and difficult problem in the hydrogeology, because it is very difficult to obtain accurate hydrogeological parameters from the aquifer system. Environmental isotopes extensively exist in various kinds of water in nature, and they can change into as part of the water molecule itself or dissolved constituents in the water system.14C, which is used widely in the groundwater age study. However, it is extraordinary hard to get the initial value of the14C, because it may influence by many processes and reactions. As an issue of concern about the difficulty in the14C age correction, this thesis attempts to carry out some works in the Shule River Basin. Firstly, the groundwater hydrochemical evolution would be determined by using relationship between the dissolved ions, trace element and87Sr/86Sr, Secondly, the groundwater flow system will be characterized by the stable isotope and chemical indices. Then, the groundwater14C age will be corrected using different method (experiential model and reverse hydrogeochemical model) which can quantify the initial radioisotopic14C along the groundwater evolution path in the different zones. The main conclusions are as follows:
The chemical type of the groundwater in the Shule River Basin changed from no-dominated to Na++K+for cations and HCO3-to no-dominated to SO42-for anions moving along the possible flow path from the piedmont of each basin to the fine soil plain areas and then downstream to the desert regions. The advantage of the alkaline earth metal ions replaced by the alkali metal cations, while the weak acid ions were permuted by the strong acid ions. The variance contribution were58.159%and14.621%calculated from the principal component analysis, which revealed that the groundwater chemistry is influenced mainly by evaporation and dissolution of evaporite minerals, as well as the alkalinity environment and common ion effect.. The dissolution of the Glauber's salt, halite, gypsum and the carbonate minerals play significant role in the groundwater'evolution. It is also found that the reverse cation exchange widely exist in the aquifers.
The87Sr/86Sr value was between0.711041to0.714029and the relationship between Sr2+and Ca2+and SO42-were good in the groundwater indicating the reaction of the evaporite rocks. In addition, recharge source of the surface water and the human activities influenced the phreatic water in some regions.
There is no distinct distribution of the stable isotope values with the depth showing that the groundwater system has close connection between phreatic groundwater confined groundwater in the Yumen-tashi Basin. The stable isotope of the Guazhou groundwater presents a different variation with increasing depth, and showing different character in unconfined and pressurized water. In the phreatic groundwater, the values increase above the depth of60m indicating the influence from the evaporation. However, it decreases below the60m denoting the groundwater was recharged by various stages. In the confined groundwater, the stable isotope was quite steady with low values indicating a steady-going flow system. These indicate that the vertical hydraulic connection between the phreatic groups and the confined layers are weak, groundwater mainly moves as horizontal flow from the east to the west. It has similar distribution in confined groundwater in the Dunhuang Basin, however, in the southwest of the basin, the overlapping aquifer may have close connection with the under layers.
It has found the dissolution of halite and Glauber's salt, as well as the reverse cation exchange were dominated process along the flow path of GZ11-GZ10and GZ04-X01in the Guazhou Basin and the path of DH01-DH03in the Dunhuang Basin. Evaporation acts on the flow path of GZ11-GZ10in the phreatic groundwater, the evaporation factor was1.177. The groundwater14C concentration elevated owing the dissolvtion of carbon dioxide along the flow path, and the time of transmission is about740a. On the path of GZ04-X01, the dissolution of aragonite and cation exchange of the Mg/Na and Mg/Na are the main process which changed the concentration of the carbon element, this reaction led to the groundwater14C of the starting point was diluted by nearly three times, and the groundwater flows through nearly10281a from the starting point of GZ04to the ending point of X01. Along the DH01-DH03flow of the Dunhuang basin, both of the calcite and aragonite were involved during the reaction path, but has little effect on concentration of the groundwater radiocarbon, the transmission time was approximately12851a.
The corrected14C age of the groundwater is between modern and16ka, indicating that the groundwater recharge mainly occurred during the Holocene and late Pleistocene. Most of the groundwater was recharged in the middle Holocene with the warm and humid climate. The circulation rate of the phreatic groundwater is between16.2-17.5m/a in the Guazhou Basin, indicating a well circulation condition, the confined groundwater has very slow circulation rate of2.4-3.7m/a in the whole basin, showing the groundwater resources are non-renewable.
疏勒河流域地下水从山前隔壁带到中游细土平原区再到下游荒漠区,地下水以碱土金属离子、弱酸根离子为优势成分逐渐演替为以碱金属、强酸根离子为主。阳离子由无明显离子特征过渡到以Na++K+为主,阴离子则从HCO3-过渡到无明显特征,最后向S042-型水演化。经过主成分分析,提取了两个主成分,其方差贡献率分别为58.159%和14.621%,分别指示了蒸发浓缩作用、溶滤作用以及地下水演化的碱性环境和同离子效应。
地下水87Sr/86Sr介于0.711041到0.714029,与蒸发岩特征值很接近,Sr2+分别于Ca2+和S042-具有很好的相互关系,说明研究区地下水发生了明显的蒸发岩溶解反应。结合离子相互关系,发现芒硝、石膏、岩盐、碳酸盐溶解沉淀,反向阳离子交换是研究区地下水主要的地球化学过程。根据Cl-与K+、HCO3-以及N03-关系识别出人为活动、补给水源等作用对潜水水化学演化影响较大。
玉门—踏实盆地地下水稳定同位素在垂向无明显分异,潜水与承压水联系紧密,交换频繁。瓜州盆地地下水随着井深的增加,稳定同位素在潜水和承压水中呈现不同的变化规律,呈现出同位素分层特点,指示各含水层岩组垂向水力联系较弱,地下水主要以水平径流为主。敦煌盆地下游承压水同位素垂向变化与瓜州盆地相似,但是在60m深度处潜水与承压水出现重叠分布,指示了在含水层过渡地带上下含水层发生联系。
瓜州水流路径GZ11-GZ10,GZ04-X01,敦煌DH01-DH03反向地球化学模拟结果显示,三条路径上均发生了阳离子交换,岩盐,芒硝的溶解反应,GZ11-GZ10路径上发生了明显的蒸发效应,蒸发因子为1.177,二氧化碳的溶解升高了地下水14C的浓度,该路径上地下水的运移时间约为740a。GZ04-X01路径上文石的溶解,Ca/Na、Mg/Na交换是促使碳酸盐变化的主要原因,该过程导致了起点地下水14C被稀释了3倍多,径流路径上的传输时间约为10281a。敦煌DH01-DH03水流路径上发生了混合作用,方解石,文石都参与了反应路径,但对地下水放射性碳影响不大,从起点到终点地下水运移经历了约12851a。
研究区第四纪地下水年龄分布范围较大,从现代到数万年,大多数承压水年龄分布在3000-7000年间,反映了中全新世大暖期暖湿的气候对地下水补给的重要作用。瓜州盆地东部补给区潜水很年轻,循环速率为16.2-17.5m/a。各盆地细土平原区深层潜水从现代到2000年不等,说明深部地下水循环交替也比较迟缓。研究区承压水普遍年龄很老,从3000年到1.6万年,地下水的循环速度介于2.4-3.7m/a,更新能力较差。
Groundwater age determining has been a focus and difficult problem in the hydrogeology, because it is very difficult to obtain accurate hydrogeological parameters from the aquifer system. Environmental isotopes extensively exist in various kinds of water in nature, and they can change into as part of the water molecule itself or dissolved constituents in the water system.14C, which is used widely in the groundwater age study. However, it is extraordinary hard to get the initial value of the14C, because it may influence by many processes and reactions. As an issue of concern about the difficulty in the14C age correction, this thesis attempts to carry out some works in the Shule River Basin. Firstly, the groundwater hydrochemical evolution would be determined by using relationship between the dissolved ions, trace element and87Sr/86Sr, Secondly, the groundwater flow system will be characterized by the stable isotope and chemical indices. Then, the groundwater14C age will be corrected using different method (experiential model and reverse hydrogeochemical model) which can quantify the initial radioisotopic14C along the groundwater evolution path in the different zones. The main conclusions are as follows:
The chemical type of the groundwater in the Shule River Basin changed from no-dominated to Na++K+for cations and HCO3-to no-dominated to SO42-for anions moving along the possible flow path from the piedmont of each basin to the fine soil plain areas and then downstream to the desert regions. The advantage of the alkaline earth metal ions replaced by the alkali metal cations, while the weak acid ions were permuted by the strong acid ions. The variance contribution were58.159%and14.621%calculated from the principal component analysis, which revealed that the groundwater chemistry is influenced mainly by evaporation and dissolution of evaporite minerals, as well as the alkalinity environment and common ion effect.. The dissolution of the Glauber's salt, halite, gypsum and the carbonate minerals play significant role in the groundwater'evolution. It is also found that the reverse cation exchange widely exist in the aquifers.
The87Sr/86Sr value was between0.711041to0.714029and the relationship between Sr2+and Ca2+and SO42-were good in the groundwater indicating the reaction of the evaporite rocks. In addition, recharge source of the surface water and the human activities influenced the phreatic water in some regions.
There is no distinct distribution of the stable isotope values with the depth showing that the groundwater system has close connection between phreatic groundwater confined groundwater in the Yumen-tashi Basin. The stable isotope of the Guazhou groundwater presents a different variation with increasing depth, and showing different character in unconfined and pressurized water. In the phreatic groundwater, the values increase above the depth of60m indicating the influence from the evaporation. However, it decreases below the60m denoting the groundwater was recharged by various stages. In the confined groundwater, the stable isotope was quite steady with low values indicating a steady-going flow system. These indicate that the vertical hydraulic connection between the phreatic groups and the confined layers are weak, groundwater mainly moves as horizontal flow from the east to the west. It has similar distribution in confined groundwater in the Dunhuang Basin, however, in the southwest of the basin, the overlapping aquifer may have close connection with the under layers.
It has found the dissolution of halite and Glauber's salt, as well as the reverse cation exchange were dominated process along the flow path of GZ11-GZ10and GZ04-X01in the Guazhou Basin and the path of DH01-DH03in the Dunhuang Basin. Evaporation acts on the flow path of GZ11-GZ10in the phreatic groundwater, the evaporation factor was1.177. The groundwater14C concentration elevated owing the dissolvtion of carbon dioxide along the flow path, and the time of transmission is about740a. On the path of GZ04-X01, the dissolution of aragonite and cation exchange of the Mg/Na and Mg/Na are the main process which changed the concentration of the carbon element, this reaction led to the groundwater14C of the starting point was diluted by nearly three times, and the groundwater flows through nearly10281a from the starting point of GZ04to the ending point of X01. Along the DH01-DH03flow of the Dunhuang basin, both of the calcite and aragonite were involved during the reaction path, but has little effect on concentration of the groundwater radiocarbon, the transmission time was approximately12851a.
The corrected14C age of the groundwater is between modern and16ka, indicating that the groundwater recharge mainly occurred during the Holocene and late Pleistocene. Most of the groundwater was recharged in the middle Holocene with the warm and humid climate. The circulation rate of the phreatic groundwater is between16.2-17.5m/a in the Guazhou Basin, indicating a well circulation condition, the confined groundwater has very slow circulation rate of2.4-3.7m/a in the whole basin, showing the groundwater resources are non-renewable.
引文
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