云南省腾冲热海地热田水化学及同位素特征
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摘要
腾冲热海地热田位于中国西南边陲，云南腾冲县西南14 km处。其目前的水热活动十分活跃、热显示丰富，具有十分重要的地球化学的理论研究意义。
热海地热田热水的Cl、B、Na等溶质具有很好的线性相关性，表明热储水源统一、冷热水混合过程单一，混合端元分别为深部高Cl水、富CO_2蒸汽以及雨水三个端元。热水的~(18)O、D同位素显示地热田的补给主要来自大气降水，部分混有幔源水的成分，补给区位于高黎贡山和北侧高山，补给高程在1600 m～2300 m之间。
热海地热田逸出CO_2气体和水溶总CO_2(TDC)的δ~(13)C值分布在-5‰～1．99‰之间。TDC的δ~(13)C值在瑞利去气或绝热沸腾去气过程中都会降低，降低程度与系统温度、开启状态有关，温度越低，开启状态越好，降低速度越快，反之亦然。本文反演得出深部热储CO_2气体的δ~(13)C值在-2～0‰之间，明显具有幔源碳的特征。同时我们发现水中δ~(13)C-TDC与腾冲火山区断裂带和中更新世英安岩分布有很好的空间相关性，说明热海地热田底部的岩浆囊可能同早更新世喷发有内在的联系。
热海地热田逸出气体的~3He/~4He值同样显示出了与断裂带、岩浆囊的分布有很好的空间相关性，断裂带越深，比值越大。近期水热爆炸(1993-2008年)反映出有向深部发展的趋势，表明岩浆囊活动可能加剧，应引起重视。
根据氚法测定深层热水的补给有早于1952年前的雨水。大部分泉点因冷热水混合导致氚含量升高，亦或是1952到1961年的氚高峰期没有过去，导致部分泉点的氚含量高于当地雨水年平均氚含量。
结合地热温标揭示的热储层温度，以及地热区的水化学、气体特征反映出的热储层赋存条件，本文提出了热海底热田热储的概念模型。地热田热储可分为深部热储和浅部热储两层。浅部热储温度在220～230℃之间，水循环较快，埋深在250～320 m；深部热储温度应为270～280℃，埋深660～785 m，水循环较慢。热源温度为320～450℃。而深部流体的温度可达400～450℃。
The Rehai geothermal field lies about 14 km from the Tengchong Town, Southwestern Yunnan, China. The field is still very rich in active manifestations such as boiling spring, fumoroles and hydrothermal explosion and is of high significance due to its theoretical research sense.
Cl, B and other elements of the spring water demonstrate very good linear correlation, implying that the springs share a same deep hot reservoir and get mixed with groundwaters at different levels. ~(18)O and D isotopes of the hot springs form a line dipping towards to the "andesitic water", indicating an obvious contribution of mantle water. Also, with the inverse modeled ~(18)O and D of the reservoir, we identify that the geothermal field is charged from the Northern and Eastern mountainous areas at altitude of 1600 m to 2300 m. The more enriched ~3H in some hot springs than the annual mean ~3H of the local precipitation should be noted. Greater part of the deep hot water may be recharged before 1951; otherwise, the reservoir may be very young, with very quick circulation of precipitation.
~(13)C of total dissolved carbon (TDC) in hot spring water and CO_2 diffused from the springs or fumaroles is also investigated to estimate the process subground. It can be concluded that ~(13)C of TDC in water decreases with the progressively degassing of CO_2. The decreasing rate will be accelerated either due to continuing temperature dropdown or to larger extent of gas degassing. Also, we find that the springs with high ~(13)C-TDC cover areas which are either distributed with deep faults or intruded by the acid volcanic rocks.
~3He/~4He of the gas diffused from water or fumaroles demonstrate good spaticial correlation with faults and magma below. The deeper the faults reveals, or the nearer the spring is to the magma, the higher the ratio of ~3He/~4He is.
Chemical and isotopic geochemistry of spring water and gas provide us a deep insight into the reservoir and the subsurface process. Together with geothermometries of Na-K, SiO_2, CO_2-CH_4 etc, we put forward a conception model of the hot reservoir. The reservoir can be recognized as two aquifers at different depth; the shallower one is about 250-320 m subground with temperature of about 220-230℃and very quick water circulation; the deeper one is distributed at depth more than 660-785 m with temperature of 270-280℃, and the deep fluid is about 400-450℃.
热海地热田热水的Cl、B、Na等溶质具有很好的线性相关性，表明热储水源统一、冷热水混合过程单一，混合端元分别为深部高Cl水、富CO_2蒸汽以及雨水三个端元。热水的~(18)O、D同位素显示地热田的补给主要来自大气降水，部分混有幔源水的成分，补给区位于高黎贡山和北侧高山，补给高程在1600 m～2300 m之间。
热海地热田逸出CO_2气体和水溶总CO_2(TDC)的δ~(13)C值分布在-5‰～1．99‰之间。TDC的δ~(13)C值在瑞利去气或绝热沸腾去气过程中都会降低，降低程度与系统温度、开启状态有关，温度越低，开启状态越好，降低速度越快，反之亦然。本文反演得出深部热储CO_2气体的δ~(13)C值在-2～0‰之间，明显具有幔源碳的特征。同时我们发现水中δ~(13)C-TDC与腾冲火山区断裂带和中更新世英安岩分布有很好的空间相关性，说明热海地热田底部的岩浆囊可能同早更新世喷发有内在的联系。
热海地热田逸出气体的~3He/~4He值同样显示出了与断裂带、岩浆囊的分布有很好的空间相关性，断裂带越深，比值越大。近期水热爆炸(1993-2008年)反映出有向深部发展的趋势，表明岩浆囊活动可能加剧，应引起重视。
根据氚法测定深层热水的补给有早于1952年前的雨水。大部分泉点因冷热水混合导致氚含量升高，亦或是1952到1961年的氚高峰期没有过去，导致部分泉点的氚含量高于当地雨水年平均氚含量。
结合地热温标揭示的热储层温度，以及地热区的水化学、气体特征反映出的热储层赋存条件，本文提出了热海底热田热储的概念模型。地热田热储可分为深部热储和浅部热储两层。浅部热储温度在220～230℃之间，水循环较快，埋深在250～320 m；深部热储温度应为270～280℃，埋深660～785 m，水循环较慢。热源温度为320～450℃。而深部流体的温度可达400～450℃。
The Rehai geothermal field lies about 14 km from the Tengchong Town, Southwestern Yunnan, China. The field is still very rich in active manifestations such as boiling spring, fumoroles and hydrothermal explosion and is of high significance due to its theoretical research sense.
Cl, B and other elements of the spring water demonstrate very good linear correlation, implying that the springs share a same deep hot reservoir and get mixed with groundwaters at different levels. ~(18)O and D isotopes of the hot springs form a line dipping towards to the "andesitic water", indicating an obvious contribution of mantle water. Also, with the inverse modeled ~(18)O and D of the reservoir, we identify that the geothermal field is charged from the Northern and Eastern mountainous areas at altitude of 1600 m to 2300 m. The more enriched ~3H in some hot springs than the annual mean ~3H of the local precipitation should be noted. Greater part of the deep hot water may be recharged before 1951; otherwise, the reservoir may be very young, with very quick circulation of precipitation.
~(13)C of total dissolved carbon (TDC) in hot spring water and CO_2 diffused from the springs or fumaroles is also investigated to estimate the process subground. It can be concluded that ~(13)C of TDC in water decreases with the progressively degassing of CO_2. The decreasing rate will be accelerated either due to continuing temperature dropdown or to larger extent of gas degassing. Also, we find that the springs with high ~(13)C-TDC cover areas which are either distributed with deep faults or intruded by the acid volcanic rocks.
~3He/~4He of the gas diffused from water or fumaroles demonstrate good spaticial correlation with faults and magma below. The deeper the faults reveals, or the nearer the spring is to the magma, the higher the ratio of ~3He/~4He is.
Chemical and isotopic geochemistry of spring water and gas provide us a deep insight into the reservoir and the subsurface process. Together with geothermometries of Na-K, SiO_2, CO_2-CH_4 etc, we put forward a conception model of the hot reservoir. The reservoir can be recognized as two aquifers at different depth; the shallower one is about 250-320 m subground with temperature of about 220-230℃and very quick water circulation; the deeper one is distributed at depth more than 660-785 m with temperature of 270-280℃, and the deep fluid is about 400-450℃.
引文
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Craig, H. 1961. Isotopic variations in meteoric waters. Science, 133: 1702-1703;
Craig,H. 1963.The isotopic geochemistry of water and carbon in geothermal areas.In:E.Tongiorgi,(Ed.),Nuclear Geology on Geothermal Areas, Spoleto,1963.ConsiglioNazionale delle Ricerche, Laboratorio di GeologiaNucleare,Pisa: 17-53;
David Dolejs, Thomas Wagner, 2008. Thermodynamic modeling of non-ideal mineral-fluidequilibria in the system Si-Al-Fe-Mg-Ca-Na-K-H-O-Cl at elevated temperatures andpressures: Implications for hydrothermal mass transfer in granitic rocks. Geochimica etCosmochimica Acta. 72: 526-553;
Fabrizio Gherardi et al,2005. Isotope systematics of C-bearing gas compounds in the geothermalfluids of Larderello, Italy.Geothermics 34:442-470;
G. Capasso, M. L. Carapezza, C. Federico S. Inguaggiato, A. Rizzo.Bull Volcanol (2005) 68:118-134 DOI 10.1007/s00445-005-0427-5;
G. Chiodini, P. Allard, S. Callro, and F. Parello,2000. Geochimica et CosmochimicaActa.64(14):2479-2488;
Giggenbach, W. F., 1992. Isotopic shifts in waters from geothermal and volcanic systems alongconvergent plate boundaries and their origin. Earth Planet Sci.Lett.,113:495-510;
Giggenbach, W. F., 1988. Geothermal solute equilibaria. Derivation of Na-K-Mg-Cageoindicators. Geochimica et Cosmochimica Acta.52:2749-2765.
Giorgio Capasso,Rocco Favara and Salvatore Invuagiato, 1997. Chemical features and isotopiccomposition of gaseous manifestations on Vulcano Island, Aeolian Islands, Italy: An??interpretative model of fluid circulation. Geochimica et Cosmochimica Acta. 61(16):3425-3440;
Ian Clark and Peter Fritz, Environmental Isotopes in Hydrogeology, CRC Press LCC, 1997;
Ian G．Donaldson Malcolm A．Grant，地热系统——原理和典型地热系统分析，地质出版社， 1986：105-130；
J. K. AGGARWAL, et al. 2000. The boron isotope systematics of Icelandic geothermal waters: 1.Meteoric water charged systems. Geochimica et Cosmochimica Acta.64(4):579-585;
J.ZHANG, P.D.QUAY, and D.O. WILBUR. 1995.Carbon isotope fractionation during gas-waterand dissolution of CO_2 .Geochimica et Cosmochimica Acta.59(1): 107-114;
James D. Webster and Charles W. Mandeville, 2007. Fluid Immiscibility in VolcanicEnvironments. Reviews in Mineralogy & Geochemistry Vol. 65, pp. 313-362,2007;
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