云南祥云县王家庄碱性温泉水化学特征与成因分析
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摘要
位于云南省祥云县刘厂镇的王家庄温泉水样YMD10-1(王家热水井)与YMD10-2(聚龙温泉宾馆热水井)的矿化度为1.49～1.65 g/L,主要阳离子为Na~+,主要阴离子为HCO_3~-,水化学类型均为HCO_3-Na型。YMD10-1和YMD10-2的p H值野外测定数据分别为10.8和7,因YMD10-2暴露于空气使其p_(CO2)较高导致其p H野外观测值偏低;实验室p H测定值分别为8和7.6,主要受到p_(CO2)差异影响导致水中碳酸组分发生变化而改变了其p H值。水样的δ~2H-δ~(18)O数据显示温泉的补给来源为大气降水。利用Si O_2温标估算了温泉的地下热储温度为89～92℃。利用~(226)Ra-~(222)Rn法估算出YMD10-1的热水年龄为446.84 a,YMD10-2的热水年龄为319.56 a。估算的地下热水的循环深度为3 808～3 898 m,利用δ~2H和δ~(18)O估算热水补给高程为2 845～2 865 m,补给区为周边的山区。地下水获得大气降水入渗补给后,经历深循环并获得深部热流加热,沿断裂带上升穿透浅部第四系出露地表。温泉显示碱性是由于长石与水和CO_2发生反应,产生大量的HCO_3~-,HCO_3~-在溶液中有可能水解消耗H~+产生OH~-。王家庄温泉被当地人们用来晒制土碱,与热水Na~+和碳酸的含量高有关。
The Wangjiazhuang hot spring is located in the Liuchang Township in Xiangyun County of Yunnan,China.The water samples YMD10-1(from the Wangjia geothermal well)and YMD10-2(from the Julong hot spring well)range in TDS from 1.49 to 1.65 g/L.The cation and anion are predominated by Na~+and HCO_3~-and the hot water is of HCO_3-Na type.The pH values of the water samples are 10.8 and 7,respectively.Because of the high p_(CO2)in the YMD10-2 sample,the pH value measured in the field is lower than expected.The p H values measured in laboratory are 8 and 7.6,respectively,which are mainly affected by the difference in p_(CO2),resulting in changes in the carbonate compositions in the water samples.δ~2H andδ~(18)O data of the hot water samples indicate that the hot spring is of meteoric origin.The recharge altitude of the hot water is estimated as 2 845-2 865 m,the temperature of the geothermal reservoir as 89-92℃,and the depth of the groundwater circulation as approximately 3 808-3 898 m.The age of the hot spring is estimated as 319-447 a with the~(226)Ra-~(222)Rn method.After receiving recharge from infiltration of precipitation in the surrounding mountain areas,the groundwater undergoes deep circulation and is heated by heat flow,and flows up along the fault zone through the Quaternary sediments and emerges on the lad surface.The alkalinity of the hot spring is attributed to the reaction of feldspar with water and CO_2,resulting in high concentrations of HCO_3~-,and hydro-lysis of HCO_3~-in solution possibly consumes H~+to produce OH~-.The Wangjiazhuang hot spring is used to produce alkali by local people due to high contents of Na~+,HCO~-_3and CO_3~(2-)in the hot water.
The Wangjiazhuang hot spring is located in the Liuchang Township in Xiangyun County of Yunnan,China.The water samples YMD10-1(from the Wangjia geothermal well)and YMD10-2(from the Julong hot spring well)range in TDS from 1.49 to 1.65 g/L.The cation and anion are predominated by Na~+and HCO_3~-and the hot water is of HCO_3-Na type.The pH values of the water samples are 10.8 and 7,respectively.Because of the high p_(CO2)in the YMD10-2 sample,the pH value measured in the field is lower than expected.The p H values measured in laboratory are 8 and 7.6,respectively,which are mainly affected by the difference in p_(CO2),resulting in changes in the carbonate compositions in the water samples.δ~2H andδ~(18)O data of the hot water samples indicate that the hot spring is of meteoric origin.The recharge altitude of the hot water is estimated as 2 845-2 865 m,the temperature of the geothermal reservoir as 89-92℃,and the depth of the groundwater circulation as approximately 3 808-3 898 m.The age of the hot spring is estimated as 319-447 a with the~(226)Ra-~(222)Rn method.After receiving recharge from infiltration of precipitation in the surrounding mountain areas,the groundwater undergoes deep circulation and is heated by heat flow,and flows up along the fault zone through the Quaternary sediments and emerges on the lad surface.The alkalinity of the hot spring is attributed to the reaction of feldspar with water and CO_2,resulting in high concentrations of HCO_3~-,and hydro-lysis of HCO_3~-in solution possibly consumes H~+to produce OH~-.The Wangjiazhuang hot spring is used to produce alkali by local people due to high contents of Na~+,HCO~-_3and CO_3~(2-)in the hot water.
引文
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[22]王恒纯.同位素水文地质概论[M].北京:地质出版社,1991:145-146.
[23]王洁青,周训,李晓露,等.云南兰坪盆地羊吃蜜温泉水化学特征与成因分析[J].现代地质,2017,31(4):822-831.
[24]GRAIG H. Isotopic variations in meteoric waters[J]. Science,1961,133:1702-1703.
[25]YU Jinsheng,ZHANG Hongbin,YU Fuji. Oxygen and hydrogen isotopic compositions of meteoric waters in the eastern Part of Xizang[J]. Geochemistry,1984,3(2):93-101.
[26]DANSGAARD W. Stable isotopes in precipitation[J]. Tellus,1964,16(4):436-468.
[27]龙汨,周训,李婷,等.北京延庆县松山温泉的特征与成因[J].现代地质,2014,28(5):1053-1060.
[28]CHERDYNTSEV V V. Uranium-234[M]. Jersalem:Keter Press,1971:44-54.
[29]MOREY G E,FOURNIER R O,ROWE J J. The solubility of quartz in water in the temperature interval from 25℃to 300℃[J]. Geochimica et Cosmochima Acta,1962,26:1029-1043.
[30]FOURNIER R O. Chemical geothermometers and mixing models for geothermal systems[J]. Geothermics,1977,5(1):41-50.
[31]赵璐,邬立,罗湘赣.由地球化学温标推算贵阳市乌当区地热田热储温度[J].工程勘察,2010(S1):832-836.
[32]吴乾蕃,祖金华,谢毅真,等.云南地区地热基本特征[J].地震地质,1988,10(4):177-183.
[2]GIGGENBACH W F. Geothermal solute equilibria:Derivation of Na-K-Mg-Ca geoindicators[J]. Geochimica et Cosmochimica Acta,1988,52:2749-2765.
[3]沈照理,朱宛华,钟佐燊.水文地球化学基础[M].北京:地质出版社,1993:10-15.
[4]王莹,周训,于湲,等.应用地热温标估算地下热储温度[J].现代地质,2007,21(4):605-612.
[5]姚永仲,唐小莉.弥渡温泉地质构造背景探析[J].有色金属设计,2010,37(1):1-5.
[6]姚永仲,张世涛,胡光英.祥云推覆构造地质背景[J].有色金属设计,2009,36(4):24-28.
[7]姚永仲.弥渡硖石洞温泉地质特征及成因模式分析[J].有色金属设计,2009,36(1):1-6,37.
[8]郝彦珍,潘明,吕勇,等.云南昌宁柯街断裂带温泉水化学特征[J].地质科技情报,2014,33(4):191-196.
[9]房艳国,李茂华,付调金,等.云南大理州洱源盆地温泉分布特征及成因分析[J].资源环境与工程,2015,29(5):701-705.
[10]LAMBRAKIS N,ZAGANA E,KATSANOU K. Geochemical patterns and origin of alkaline thermal waters in Central Greece(Platystomo and Smokovo areas)[J]. Environmental Earth Science,2013,69(8):2475-2486.
[11]JEAN Jinshuh,LIAO Libing,KAR Sandeep,et al. Hydrochemistry of hot springs in geothermal fields of central,northern,and northeastern Taiwan:implication on occurrence and enrichment of arsenic[J]. Environmental Earth Sciences,2016,75(19):1316.
[12]云南省地质矿产局.云南省区域地质志[M].北京:地质出版社,1990:附图.
[13]云南省地质矿产局.云南省岩石地层[M].武汉:中国地质大学出版社,1996:310-312.
[14]周真恒,向英才,赵晋明.滇西地热场特征[J].地震研究,1995,18(1):41-48.
[15]迟恩先,兰波,肖延卿.溶液温度及CO2含量对长石溶解度的影响[J].水资源与水工程学报,2014,25(2):230-232.
[16]周训,金晓媚,梁四海,等.地下水科学专论(第二版.彩色版)[M].北京:地质出版社,2017:75-76,125-126.
[17]张人权,梁杏,靳孟贵,等.水文地质学基础(第六版)[M].北京:地质出版社,2011:53-54.
[18]FREEZE R A,CHERRY J A. Groundwater[M]. London:Prentice-Hall Inc,1979:98-100.
[19]鲁通,韦存容,马宏佳.强碱弱酸正盐溶液pH与温度变化关系的再探究[J].化学教与学,2017(2):76-78.
[20]李友银,石璞,任腾菲.对强碱弱酸盐溶液pH与温度关系的研究[J].化学教育,2014,35(23):63-66.
[21]钱会,刘国东.不同pCO2条件下水溶液的pH值及溶液中化学组分平衡分布的计算[J].中国岩溶,1994,13(2):133-140.
[22]王恒纯.同位素水文地质概论[M].北京:地质出版社,1991:145-146.
[23]王洁青,周训,李晓露,等.云南兰坪盆地羊吃蜜温泉水化学特征与成因分析[J].现代地质,2017,31(4):822-831.
[24]GRAIG H. Isotopic variations in meteoric waters[J]. Science,1961,133:1702-1703.
[25]YU Jinsheng,ZHANG Hongbin,YU Fuji. Oxygen and hydrogen isotopic compositions of meteoric waters in the eastern Part of Xizang[J]. Geochemistry,1984,3(2):93-101.
[26]DANSGAARD W. Stable isotopes in precipitation[J]. Tellus,1964,16(4):436-468.
[27]龙汨,周训,李婷,等.北京延庆县松山温泉的特征与成因[J].现代地质,2014,28(5):1053-1060.
[28]CHERDYNTSEV V V. Uranium-234[M]. Jersalem:Keter Press,1971:44-54.
[29]MOREY G E,FOURNIER R O,ROWE J J. The solubility of quartz in water in the temperature interval from 25℃to 300℃[J]. Geochimica et Cosmochima Acta,1962,26:1029-1043.
[30]FOURNIER R O. Chemical geothermometers and mixing models for geothermal systems[J]. Geothermics,1977,5(1):41-50.
[31]赵璐,邬立,罗湘赣.由地球化学温标推算贵阳市乌当区地热田热储温度[J].工程勘察,2010(S1):832-836.
[32]吴乾蕃,祖金华,谢毅真,等.云南地区地热基本特征[J].地震地质,1988,10(4):177-183.