Zircon U-Pb geochronology, geochemical characteristics and tectonic implications of Caledonian granites from the Xuanhe area, Southwestern Fujian Province
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摘要:
龙岩宣和岩体是闽西南地区呈北东向弧形出露，最大的燕山期-加里东期复式岩体，但是有关该岩体的形成时代及成岩环境的认识仍存在分歧，进而制约了对闽西南地区构造环境的探讨。文章以出露于闽西南地区的宣和正长花岗岩为研究对象，在详细野外地质调查基础上，开展了岩石学、LA-ICP-MS锆石U-Pb地质年代学、岩石地球化学及Sr-Nd同位素测试等工作，在此基础上探讨了宣和岩体的岩石类型、岩浆来源和成岩构造环境。宣和岩体主要由含斑细粒、少斑中细粒、似斑状中粒、似斑状中粗粒及斑状细粒正长花岗岩等组成，4个样品的锆石LA-ICP-MS U-Pb年龄为（424.6±2.8）Ma、（426.7±2.6）Ma、（435.5±2.4）Ma及（447±3.6）Ma，表明其形成时代不是原来认为的印支期，而是加里东期。地球化学特征上，具高硅、高钾（K2O>Na2O），低TiO2、FeO、MgO的特征，A/CNK平均值1.23，属高钾钙碱性过铝质系列岩石；稀土元素含量高，稀土配分曲线右陡倾，轻重稀土分馏明显，Eu中等负异常；富集大离子亲石元素K、Rb、Pb、Nd及高场强元素Th、U，相对亏损Sr、Ba、Nb、Ce，显示高分异的S型花岗岩的特征。其Sr同位素初始比值介于0.71291~0.71399，εNd（t）值变化于-9.1~-13.4，对应的二阶段Nd模式年龄为1.91~2.27 Ga，推测宣和岩体是由与麻源群变质岩相当的地壳物质部分熔融形成的，为华南加里东期板内造山作用的产物。
Abstract:The NE-trending Xuanhe granitic mass is the largest Yanshanian-Caledonian complex rock mass in southwestern Fujian, which is exposed in southwestern Fujian Province in the arc form. However, there are still different opinions in the formation age of rock mass and its petrogenetic environment, which restricts the discussion of the tectonic environment of southwestern Fujian. Based on detailed field geological survey, the authors investigated the Xuanhe syenogranites, mainly on the basis of the LA-ICP-MS zircon U-Pb geochronology, petrochemistry and Sr-Nd isotope analysis, and discussed the rock types, magma source and tectonic environment. The Xuanhe granites are mainly composed of syenogranites in the forms of speckle fine grain, oligophyric medium-fine grain, porphyritic fine grain, porphyritic fine coarse grain and porphyritic fine grain. The LA-ICP-MS zircon U-Pb age of four samples from the granites are (424.6±2.8)Ma, (426.7±2.6)Ma, (435.5±2.4)Ma and (447±3.6)Ma respectively, indicating that the formation age of Xuanhe granite is Caledonian instead of Indosinian as previously held. The rocks belong to high-K calc alkaline peraluminous rock series, characterized geochemically by high Si, high K (K2O>Na2O), low TiO2, low FeO and low MgO, with average A/CNK value being 1.23. The rocks are S-type grantie, with the characteristics of high content of rare earth elements, obvious right steeply inclined REE fractionation curve, middle negative Eu anomaly, enrichment of large ion lithophile elements such as K, Rb, Pb and Nd and high field strength elements of Th, U and Ba, and relative depletion of Sr, Nb and Ce. The initial Sr isotope ratios are from 0.71291 to 0.71399, the values of εNd(t) vary from -9.1 to -13.4, and two stage Nd model ages correspond to 1.91-2.27 Ga. It is inferred that the granites were formed by partial melting of crustal material of Mayuan Group metamorphic rocks, being probably a product of intraplate Caledonian orogeny in South China.
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1. 引言
砷(As)在自然界普遍存在，是国际癌症研究机构(IARC)列出的第Ⅰ类明确致癌物(WHO, 2011；Shahid et al., 2018)。饮用水砷浓度最敏感的毒性阈值尚未确定，世界卫生组织推荐的饮用水砷浓度限值为10 μg/L(WHO, 2011)。美国环境保护署(EPA)和国家研究委员会(NRC)指出，长期饮用浓度低至5 μg/L甚至3 μg/L的水可能会对人类健康造成慢性影响，引发癌症(Taheri et al., 2017)。饮用高砷地下水是人类遭受砷暴露风险的主要途径，全球有超过1亿人承受高砷地下水的暴露风险，其中中国有1900万(Duan et al., 2017; Li et al., 2017；Cao et al., 2018；Shahid et al., 2018)。
高砷地下水在全球分布广泛，南亚、东南亚是地下水砷污染的典型地区，已经开展过深入而广泛的地球化学研究，解析高砷地下水的形成演化过程，追溯砷的来源及其溶出释放机制(Tang et al., 1996；Wang et al., 1998；Deng et al., 2009; Xie et al., 2012；Li et al., 2013；Gan et al., 2014；Hu et al., 2015；Gupta et al., 2017；Zhang et al., 2017；Han et al., 2017；Li et al., 2018；Gillispie et al., 2019；Gao et al., 2020)。含砷矿物氧化溶解及还原活化是高砷地下水形成的主要机制(Gupta et al., 2017; Zhang et al., 2017; Shahid et al., 2018; Gillispie et al., 2019; Stopelli et al., 2020)。中国高砷地下水主要分布在大同盆地、江汉平原、河套盆地、银川盆地等内陆平原区；淮河流域是中国新发现的高砷地下水集中分布区，高砷地下水分布范围广，影响人口众多。根据2010年代开展的淮河流域地下水分析数据统计预测，淮河流域大部分地区的砷暴露风险概率大于0.4，统计发现流域内各村庄监测水井As浓度超过10 μg/L的比例达17%，最高检测值为620 μg/L(Li et al., 2017)。
高砷地下水的形成是在水岩相互作用过程中多因素共同作用的结果。淮河流域富砷地下水砷污染系原生成因，以前的研究工作主要集中在地下水As的水文地球化学分布、饮水型砷中毒地方病的地理分布等方面(Zhang et al., 2010；Chen et al., 2013; Li et al., 2017)。淮河流域高砷地下水的研究程度低，缺乏对高砷地下水的形成过程及其影响因素的深入解析，高砷地下水的形成演化机制不明。本次研究选择淮河平原代表性的高砷地下水小尺度流场，针对以往研究的薄弱环节，运用地下水水文地球化学分析方法，主要研究目标为：(1)分析典型高砷地下水的水文地球化学特征，评估其污染风险；(2)解析高砷地下水的形成演化过程；(3)追溯砷污染物的来源及溶出释放过程。开展高砷地下水的形成演化过程研究，为淮河流域高砷地下水的治理与公共健康风险控制提供科学依据。
2. 研究区概况
淮河流域地处中国东部，流域西起桐柏山、伏牛山，东临黄海，南以大别山、江淮丘陵、通扬运河及如泰运河分界，北以黄河、泰山为界与黄河流域毗邻，地理坐标：111°55′~121°25′E，30°55′~36°36′N，面积为27万km2。该流域处于中国南北气候过渡带，属暖温带半湿润季风气候区，年平均气温11~16℃。其地质构造上位于华北板块、扬子板块、秦岭造山系3个构造单元的交接地带(Zhang et al., 2015) (图 1)。
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图 1 淮河流域安徽太和县地质背景、采样部署及水文地质剖面Figure 1. Geological background, sampling sites and hydrogeological profile of Taihe County of Anhui Province in Huaihe River Basin研究区安徽省太和县位于淮河流域中部，以冲积平原地貌为主，海拔高程一般15~50 m，地势由西北向东南微倾。研究区分布最广的地下水类型为松散岩类孔隙水，水文地质分区划分为淮河中游淮北冲积平原区。自新近纪(23 Ma)以来，淮河流域形成了巨厚的新近系、第四系松散沉积物，为区域地下水的形成与分布提供了良好的水文地质条件。研究区地下水系统自上而下划分为浅层、中深层、深层含水系统(Li et al., 2018)。浅层地下水赋存于50 m以浅的全新统、上更新统地层，与大气降水、地表水关系密切，地下水埋深一般为2~4 m，均在极限蒸发深度以内，蒸发是浅层地下水的主要排泄途径。中深层地下水赋存于50~150 m的中、下更新统地层，深层地下水主要赋存于150~500 m的新近系(图 1)。由于中、深层地下水埋藏较深(埋深大于50 m)，含水层之间有着黏性土层相隔，不能直接接受大气降水的补给，径流缓慢，人工开采是深层地下水的主要排泄途径。
3. 调查研究方法
太和县是淮河平原典型的高砷地下水分布区(图 1)，本次研究选择太和县马集镇及相邻区的高砷地下水小尺度流场为天然实验场，采集测试地下水样品。本次研究采用精度为1 km×1 km(局部1 km×0.5 km)的近似网格法布设采样点。本次研究于2019年5、9月采集样品，共采集地下水样64件。采集的地下水样品，主要取自研究区井深不到50 m的浅井，水位埋深4~50 m，含水层为第四系砂层、细砂层、粉砂层。
地下水样品水化学分析了As、K+、Na+、Ca2+、Mg2+、Cl-、SO42-、HCO3-、F-、Br-、总碱度和总酸度。阳离子(Na+, K+, Ca2+, Mg2+)采用电感耦合等离子体发射光谱法(ICP-OES)测定，阴离子(HCO3-, SO42-, Cl-, F-, Br-)用离子色谱法测定，总碱度、总酸度采用酸滴定法测定，地下水As浓度测试采用荧光光谱仪(AFS-820，中国)，As检出限为0.05 μg/L，精密度＜1.0%。样品测试分析由中国地质调查局南京地质调查中心实验测试中心完成。研究区地下水化学分析结果见表 1。
表 1 淮河流域安徽太和县地下水化学测试分析（2019年6月、9月采样）Table 1. Chemical assay data of groundwater quality in Taihe County of Anhui Province in Huaihe River Basin (sampled in June and September 2019)
根据热力学原理，水岩反应中矿物的溶解与沉淀由各种矿物在地下水中的饱和指数(SI) 决定，利用SI可以识别水质和水化学演化过程(Zhu et al., 2011；Han et al., 2014；Taheri et al., 2017)。SI的数学表达式为:
其中IAP是离子活性积，Ks是矿物的平衡常数。SI＜0、SI = 0、SI＞0分别为矿物处于溶解、平衡、沉淀阶段的热力学判据，通常认为0.5＞SI＞-0.5为近饱和状态。
地下水化学分析以SPSS 19.0为平台对数据进行描述统计、相关分析、回归分析，以Phreeqc 3.40为平台选择确定矿物相，计算矿物饱和指数，专题图以Coreldraw X4、AquaChem 3.70为平台制作。
4. 结果与分析
4.1 地下水质量评价
根据地下水化学测试分析结果，依据国家地下水质量标准GB/T 14848-2017分类标准(MLR，2017)，地下水中As、Cu、Mo、Ba、Na+、Cl-、SO42-、HCO3-、CO32-、NO3-、NO2-、F-、COD、I、TDS、Mn、HBO2等的均值、标准差与质量分类见表 1。影响太和马集研究区松散岩类孔隙水水质的主要无机组分是砷、钡、钠、氯、氟、碘、锰、硝酸盐、硫酸盐、硼、溶解性总固体，其中砷、氟、锰、钠、硼是最主要影响因子，单项指标超过地下水质量Ⅲ类标准的样品比例均超过50%(表 1、表 2)。
表 2 安徽太和县地下水化学统计分析与评价Table 2. Statistics and evaluation of groundwater chemistry of Taihe Conty, Anhui Province in Huaihe River Basin
依据世界卫生组织推荐的饮用水质量标准(WHO, 2011)，影响研究区地下水水质的主要因素是As、F浓度。研究区浅层地下水砷浓度为(5.75±5.42) μg/L，呈现明显的空间变异性；超过世界卫生组织饮用水推荐准则值(10 μg/L)样品比例为23%，呈现高暴露风险。地下水氟浓度为(1.29±0.40) mg/L，超过推荐限值(1.5 mg/L)样品比例达31%。
4.2 地下水离子浓度与水化学类型
本次研究采集分析的地下水均为浅层孔隙水，含水岩组为全新统和上更新统含水岩组。根据水化学分析结果，研究区浅层地下水的总溶解固体(TDS)浓度为(719.29±310.20) mg/L，其中大部分样品为低盐度淡水(＜1000 mg/L)，26%在微咸水(1000~3000 mg/L)范围内。地下水的化学成分受主要离子(SO42-、Cl-、HCO3-、Na+、Ca2+、Mg2+)控制。阴离子成分以HCO3-为主，SO42-和Cl-次之，浓度分别为(617.93±220.25)、(83.73±73.09)、(54.03±58.81) mg/L。阳离子以Na+为优势离子，其次为Ca2+、Mg2+，浓度分别为(186.04±120.17)、(46.17±27.91)、(39.48±12.39) mg/L。
研究区测试样品总碱度(516±169) mg/L，总酸度(20.00±4.63) mg/L，地下水呈碱性。测试样品总碱度与HCO3-浓度极显著正相关，相关系数R=0.997(P≤0.01)，故水样中总碱度表现为HCO3-碱度，总碱度大小总体上反映了HCO3-含量的大小。高砷地下水总碱度主要分布在400~700 mg/L(图 2)，研究区碳酸盐岩矿物风化作用和离子交换反应升高了地下水的碱度。
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图 2 淮河流域安徽太和县高砷地下水总碱度图解Figure 2. Diagram of total alkalinity of high-arsenic groundwater in Taihe County of Anhui Province, Huaihe River Basin优势离子决定了地下水的类型，按piper三线图统计，研究区水化学类型以HCO3-Na为主，其次为HCO3-Na·Mg、HCO3-Na·Ca，HCO3-Na·Ca·Mg型。高砷地下水的水化学类型主要为HCO3-Na型(图 3)
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图 3 淮河平原安徽太和县地下水piper图Figure 3. Piper diagram of the groundwater in Taihe County of Anhui Province, Huaihe River Basin4.3 地下水演化过程
4.3.1 蒸发浓缩作用
Cl和Br也是地下水中普遍存在的溶质，由于Cl、Br在天然水中的保守行为和高溶解度，离子交换反应与矿物表面吸附等过程不能显著改变Cl和Br的浓度。岩盐(NaCl)矿物结构中不含较大的Br离子，其Cl/Br比值一般为104~105(摩尔比)，岩盐溶解随着氯离子浓度的增加将产生Cl/Br比值的快速增加；相比之下，地下水的蒸发过程可以改变地下水中Cl和Br的绝对浓度，但不会改变地下水岩盐饱和之前的Cl/Br比值。因此应用Cl、Br及Cl/Br比值可以识别区分地下水的溶解、蒸发等演化过程(Cartwright et al., 2006；Deng et al., 2009；Xie et al., 2012；Xing et al., 2013；Han et al., 2014；Taheri et al., 2017)。
研究区测试样品的Cl-浓度范围0.70~210 mg /L，均值(54.03±58.81) mg/L，Br-浓度范围为10.7~324 μg/L，均值(104±87.9) μg/L。Cl-浓度与Br-浓度显著正相关，相关系数0.75(P≤0.01)。样品的Cl-、Br-浓度较低，Cl/Br(mol)均值为1097±1044，比值变化范围51.0~4603。样品中大部分的Cl/Br比值超过600，显示显著的空间变异性；As超标地下水(＞10 μg/L)的Cl/Br比值范围544~3093，均值993。测试样品Cl/Br比值最高值超过4600，地下水Cl浓度不超过6 mmol /L，地下水溶解少量的岩盐是Cl/Br比值快速增大最可能的机制，较大的Cl/Br比值变化范围反映出各测试样品岩盐溶解量的不同。Cl/Br比与Cl浓度之间的关系(图 4)表明，蒸发作用、岩盐溶解作用是控制浅层地下水分布的主导过程，高砷地下水Cl/Br比值随Cl浓度的增加而相对不变，说明高砷地下水更大程度受到蒸发作用的影响。
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图 4 淮河流域安徽太和县地下水Cl/Br比值与Cl相关图Figure 4. Correlation between Cl/Br ratio and Cl of groundwater in Taihe County of Anhui Province, Huaihe River Basin4.3.2 岩石风化水解作用
Ca/Na、Mg/Na、HCO3/Na(mol)比值可以表示地下水矿化度的强弱，也可以得到地下水来源及水质演化的相关信息，在一定程度上为区域水文地球化学演化过程提供判断依据(Zhu et al., 2011; Liu et al., 2018)。从研究区地下水Mg /Na-Ca/Na、HCO3/Na-Ca/Na关系图(图 5)可知，随着Ca/Na比值的增大，地下水的Mg /Na、HCO3/Na比值逐渐增加。地下水主要阳离子浓度比值主要分布于蒸发盐矿物溶解与硅酸盐矿物风化作用之间，少部分分布于硅酸盐矿物风化作用与碳酸盐矿物溶解作用之间，表明研究区地下水受到蒸发盐溶解、硅酸盐风化、碳酸盐溶解等过程的共同影响。高砷地下水的离子比值主要分布于蒸发盐矿物溶解与硅酸盐矿物风化作用之间，显示高砷地下水更大程度受到蒸发盐溶解与硅酸盐矿物风化过程的影响。
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图 5 淮河流域安徽太和县高砷地下水Ca/Na-Mg/Na、HCO3/Na-Ca/Na图解Figure 5. Diagram of Ca/Na-Mg/Na and HCO3/Na-Ca/Na of groundwater in Taihe County of Anhui Province, Huaihe River Basin4.3.3 离子交换吸附作用
Na/Cl比值(mol)是表征地下水中Na+富集程度的一个水文地球化学参数，可以用来反映离子交换程度(Xing et al., 2013；Han et al., 2014；Yang et al., 2016；Taheri et al., 2017)。淮河流域属于干旱—半干旱地区，蒸发作用强烈，导致岩盐在沉积层累积，岩盐溶解是平原盆地区地下水中Na+和Cl-的主要来源之一。如果岩盐溶解为Na+与Cl-的主要来源，则Na/Cl(mol)-的比值应为1∶1，高于此比值的Na+则可能有其他来源。本次研究全区采集地下水样Na/Cl比值为9.63±57.4，绝大部分样品远大于1∶1，呈现显著的空间变异性，Na/Cl比值随Cl浓度的增加呈下降趋势；高砷地下水(10＞As≥5 μg/L)、污染地下水(As≥10 μg/L)的Na/Cl比值分别为43.1±85.1、15.7±16.0，全部位于岩盐溶解线上方(图 6)。由此推断，研究区地下水的Na+并不仅仅来源于岩盐溶解，地下水总体上可能经历强烈的阳离子交换作用，而且高砷地下水的离子交换作用更为显著。
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图 6 淮河流域安徽太和县高砷地下水Na-Cl图解Figure 6. Na-Cl diagram of groundwater in Taihe County of Anhui Province, Huaihe River Basin4.4 地下水离子来源与砷的活化
水岩相互作用控制着地下水中主要离子浓度及其赋存状态。本次研究利用PHREEQC 3.7计算矿物饱和指数，结果表明：近饱和矿物方解石(0.41)、文石(0.26)、菱镁矿(0.04) 的SI值接近0，处于准平衡状态；未饱和矿物岩盐(-6.52)、石膏(-1.99)、硬石膏(-2.23)、萤石(-1.02)的SI值小于-0.5，表明存在岩石溶解的趋势；白云石(0.70) 的SI大于0.5，存在化学沉淀的趋势(表 3)。地下水中Cl-、F-、SO42-部分源自岩盐、萤石及石膏、硬石膏矿物的溶解释出。
表 3 淮河流域安徽太和县地下水矿物饱和指数Table 3. Saturation indices of groundwater in Taihe County of Anhui Province, the Huaihe River Basin
在自然环境pH、Eh条件下，砷元素主要以无机氧化态As(Ⅴ)和还原态As(Ⅲ)元素价态存在。沉积物(土壤)中含砷矿物通常以砷酸盐、亚砷酸盐和硫化物等矿物相存在，在还原条件下，砷黄铁矿是砷的稳定宿主，其伴生砷与地下水砷分布高度相关(Hu et al., 2015; Taheri et al., 2017; Duan et al., 2017; Zhang et al., 2017; Shahid et al., 2018; Gillispie et al., 2019)。地下水动态、氧化还原电位(Eh)、酸碱度(pH)的变化影响沉积物砷的吸附-解析过程，进而影响水体砷的浓度，高pH、低Eh还原条件促进沉积物中砷的解吸和溶解进入地下水而在溶液中积累(高存荣等, 2010; 王杰等, 2015; Duan et al., 2017; Taheri et al., 2017; Zhang et al., 2017; Gillispie et al., 2019)。
地下水中的SO42-可能源自石膏溶解与硫化物氧化，全区地下水SO42-/Ca2+ (mol) 比值为0.76，地下水的SO42-不仅仅源于石膏矿物的溶解，还有硫化物的氧化。测试样品中的As和SO42-浓度之间正相关(相关系数R=0.584)。分析样品中As＜3 μg/L、3 μg/L≤As＜5 μg/L、5 μg/L≤As＜10 μg/L与As≥10 μg/L地下水的SO42-浓度均值分别为0.74、1.09、0.92与0.93 mmol/L，高砷地下水呈现相对高的硫酸盐浓度。
经X射线衍射物相分析，淮河流域浅层(0.2~1 m)沉积物主要矿物成分为石英、钾长石、方解石和黏土矿物，含量分别为47.1%、3.79%、8.27%和33.4%。部分样品中含有少量黄铁矿和菱铁矿，含量分别为2.5%和47.1%，未检测到赤铁矿，反映还原性地下水环境。据地下水化学数据与表层沉积物物相分析结果推测淮河流域沉积物中砷在还原条件下可能以含砷硫化物相存在，由于长期大量开采地下水，地下水流系统环境改变，破坏了含水层固液相动态交换的平衡，触发As从固相释放到地下水中。碳酸盐矿物的溶解通常会增加碱度(pH)值，在高pH条件下，含砷硫化物的氧化速率增加，地下水SO42-浓度增高，促进As向水体的释出。pH值的增大也促进As从金属氧化物(Fe、Mn)中解析从而增加水中As浓度(Duan et al., 2017; Taheri et al., 2017; Zhang et al., 2017; Gillispie et al., 2019)。因此推测含水层沉积物含砷矿物氧化溶解与还原活化是导致原生砷向地下水释出的主要过程。研究区地下水表现出的高矿化度和强烈蒸发作用可能与农业灌溉有较大关系，含水层中原生的矿物组分是造成高砷水的最主要原因。另外，高强度的深层地下水抽取灌溉也可能是导致的高砷水进入浅水含水层的原因之一。
5. 结论
高砷地下水的形成是多因素综合作用的结果，是一个复杂的水文地质过程。高砷地下水的形成是含砷矿物集聚、固相砷的溶解析出及富集砷的水文地质条件等在水岩相互作用过程中多因素综合作用的结果。本次研究选择流域内典型的高砷地下水小尺度流场为天然实验场，解析高砷地下水的形成演化过程，追溯砷的来源及其溶出释放机制。
(1) 研究区地下水砷含量为(5.75±5.42) μg/L，具有明显的空间变异性，超过世界卫生组织饮用水推荐准则值的测试样品比例为23%，呈现高暴露风险，饮用高砷地下水可能是威胁人类健康的主要途径。
(2) 根据水化学成分解析，研究区地下水经历蒸发作用、岩盐溶解、水岩相互作用等过程的共同影响。高砷地下水的化学类型主要为HCO3-Na型，高砷地下水更大程度受到蒸发作用、阳离子交换作用的影响。
(3) 研究区高砷地下水系原生成因，高砷地下水的As源自含水层沉积物原生砷的溶出释放。碱性环境下，含水层沉积物含砷矿物氧化溶解与还原活化可能是高砷地下水形成的主要机制。
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图 1 宣和岩体区域纲要图（a）及研究区地质简图（b）
1—第四系；3—晚白垩世崇安组；4—晚白垩世沙县组；5—早白垩世晚期构造层；6—早白垩世坂头组；7—晚侏罗世构造层；8—晚三叠世—中侏罗世构造层；9—中侏罗世漳平组；10—早侏罗世梨山组；11—晚二叠世—中三叠世构造层；12—晚二叠世翠屏山组；13—晚石炭世—中二叠世构造层；14—中二叠世童子岩组；15—中二叠世文笔山组；16—晚泥盆世—早石炭世构造层；17—早石炭世梨山组；18—晚泥盆世桃子坑组；19—晚泥盆世天瓦岽组；20—晚新元古代—早古生代构造层；21—末寒武世东坑口组；22—早—晚寒武世林田组；23—晚震旦世黄连组；24—南华—晚震旦世南岩组；25—中新元古代构造层；26—古元古代构造层；27—晚白垩世晶洞花碱长花岗岩；28—早白垩世正长花岗岩；29—早白垩世二长花岗岩；30—晚侏罗世正长花岗岩；31—晚侏罗世少斑中细粒正长花岗岩；32—晚侏罗世二长花岗岩；33—中三叠世正长花岗岩；34—中三叠世二长花岗岩；35—志留纪正长花岗岩；36—志留纪斑状细粒正长花岗岩；37—志留纪似斑状中粗粒正长花岗岩；38—志留纪似斑状中粒正长花岗岩；39—志留纪少斑中细粒正长花岗岩；40—志留纪含斑细粒正长花岗岩；41—志留纪二长花岗岩；42—断层产状；43—层理产状；44—地质界线；45—平行不整合界线；46—角度不整合界线；47—断层；48—推覆断层；49—滑脱断层；50—正断层；51—逆断层；52—脉动界线；53—涌动界线；54—测年样位置；55—研究区；56—剖面位置
Figure 1. Geological map of Xuanhe granite mass (a) and sketch geological map of the study area (b)
1- Quaternary; 2- Late Cretaceous tectonic layer; 3- Late Cretaceous Chongan Formation; 4- Late Cretaceous Shaxian Formation; 5- Early Cretaceous tectonic layer; 6-Early Cretaceous Bantou Formation; 7-Late Jurassic tectonic layer; 8-Late Triassic-Middle Jurassic tectonic layer; 9- Middle Jurassic tectonic layer; 10-Early Jurassic Nishan Formation; 11-Late Permian-Middle Triassic tectonic layer; 12-Late Permian Cuipingshan Formation; 13- Late Carboniferous- Middle Permian structural layer; 14- Middle Permian Tongziyan Formation; 15- Middle Permian Wenbishan Formation; 16- Late Devonian- Early Carboniferous tectonic layer; 17- Early Carboniferous Lishan Formation; 18- Late Devonian Taozikeng Formation; 19-late Devonian Tianwadong Formation; 20-Late Neoproterozoic-Early Palaeozoic tectonic layer; 21-Late Cambrian Dongkengkou Formation; 22-Early-Late Cambrian lingtian Formation; 23-Late Sinian Huanglian Formation; 24-Nanhua Period-Late Sinian Nanyan Formation; 25-Middle-Late Proterozoic tectonic layer; 26- Paleoproterozoic tectonic layer; 27-late Cretaceous miarolitic alkali feldspar syenite; 28-Early Cretaceous syenite; 29- Early Cretaceous monzogranite; 30- Late Jurassic syenite; 31- Late Jurassic oligophyric fine- grained syenite; 32- Late Jurassic Monzogranite; 33-Middle Triassic syenite; 34-Middle Triassic monzogranite; 35-Silurian syenite; 36-Silurian porphyritic fine-granied syenite; 37- Silurian like macular middle- coarse granied syenite; 38- Silurian like macular middle- granied syenite; 39- Silurian littel macular middle-fine grained syenite; 41-Silurian macular- bearing fine- granied syenite; 42-Fault attitude; 43-Bedding attitude; 44-Geological boundary; 45-Parallel unconformity boundary; 46 Angular unconformity boundary; 47- Fault; 48-Nappe fault; 49-Slip fault; 50- Normal fault; 51-Reverse fault; 52-Pulsation boundary; 53-Inrush boundary; 54-Dating sample position; 55- Study area; 56-Profile position
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图 2 长汀县下坑—连城县小坑志留纪宣和岩体剖面图（图 1b中A−A’剖面）
1—花岗斑岩脉；2—闪长岩脉；3—石英砂砾岩；4—砂砾岩；5—正断层；6—逆冲断层；其他图例见图 1
Figure 2. Geological section of Silurian Xuanhe granite mass in Xiakeng of Changding County -Xiaokeng of Liancheng County (A−A'profile in Fig. 1b)
1−Granite-porphyry dyke; 2−Diorite dyke; 3−Quartzose glutenite; 4−Glutenite; 5−Normal fault; 6−Thrust fault (other legends as for Fig. 1)
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图 3 宣和岩体野外露头及正交偏光显微照片
a、b—似斑状中粒正长花岗岩；c、d—似斑状中粗粒正长花岗岩；e—少斑中细粒正长花岗岩花岗岩；f—斑状细粒正长花岗岩
Figure 3. Microphotograph of Xuanhe granites mass (crossed nicols)
a, b−Oligophyric fine grained syenite; c, d−Porphyritoid medium grained syenite; e−Porphyritoid medium−coarse grained syenite; f−Porphyritic fine grained syenite
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图 4 宣和岩体锆石阴极发光图像及测点位置
Figure 4. CL images of Xuanhe granite mass and spot test position
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图 5 宣和岩体锆石U-Pb年龄谐和图和加权平均值
Figure 5. Zircon U-Pb concordia diagrams of Xuanhe granite mass
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图 6 宣和岩体TAS图解（a）、QAP图解（b）、K2O−SiO2图解（c）及A/NK−A/CNK判别图解（d）
（a底图据Middlemost，1994；b底图据TUGS，1979；c底图中实线据Peccerillo and Taylor, 1976.；虚线据Middlemost, 1985)
Figure 6. TAS diagram (a), QAP diagram (b), K2O−SiO2 diagram (c) and A/NK−A/CNK diagram (d) of Xuanhe granite mass
(a base map after Middlemost, 1994; b base map after TUGS, 1979; c base map solid line after Peccerillo R, Taylor, 1976; data of dashed line after Middlemost, 1985)
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图 7 宣和岩体稀土元素配分模式图（a）及微量元素蛛网图（b）
（球粒陨石标准化值和原始地幔标准化值据Sun and McDonough, 1989）
Figure 7. REE patterns and spidergrams of Xuanhe granite mass
(standardized value of chondrite and primitive mantle after Sun and McDonough, 1989)
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图 8 宣和岩体Sr同位素的岩石源区识别图（a）及εNd(t)−t及基底变质岩Nd同位素演化区域图（b）
Ⅰ—东山岛—莆田忠门变质岩演化域；Ⅱ—龙海深奥变质演化域；Ⅲ—麻源群演化域
Figure 8. The Sr isotope diagram and εNd(t) −t diagram of Xuanhe granite mass(b)
Ⅰ−Evolution field of metamorphic rock from Dongshan Island-Putian Zhongmen; Ⅱ−Evolution field of metamorphic rock from Longhai Shenao; Ⅲ−Evolution field of Mayuan Group
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图 9 宣和岩体A−C−F花岗岩类型判别图解
Figure 9. ACF discrimination diagram of granite type in Xuanhe granite mass
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图 10 宣和岩体构造环境判别图解
a—特曼−戈蒂里图解；b—R1−R2图解（据Batchelor and Bowdden, 1985)；c—Nb−Y图解；d—Ta−Yb图解a图：A—非造山带火山岩，B—造山带火山岩，C—A、B区所派生的碱性、偏碱性火山岩；b图：①—地幔斜长花岗岩；②—破坏性活动板块边缘(板块碰撞前)花岗岩；③—板块碰撞后隆起期花岗岩；④—晚造山期花岗岩；⑤—非造山区A型花岗岩；⑥—同碰撞(S型)花岗岩；⑦—造山期后A型花岗岩；c图、d图：WPG—板内花岗岩；ORG—洋中脊花岗岩；VAG—火山岩弧花岗岩；SYN−COLG—同碰撞花岗岩
Figure 10. The discrimination diagram for tectonic setting of Xuanhe granite mass
a−Rittmann−Gottiry diagram; b−R1−R2 diagram (after Batchelor and Bowdden, 1985); c−Nb−Y diagram; d−Ta−Yb diagram Diagram a: A−Anorogenic volcanic rocks, B−Orogenic volcanic rocks, C− Alkaline and peralkaline rocks derived from series A and B; Diagram b: ①−Mantle plagiogranite; ②−Destructive plate boundary granite (pre-plate collision); ③−Post-plate collision uplift granite; ④−Late orogenic granite; ⑤−Anorogenic A−type granite; ⑥−S−type granite; ⑦−Post-orogenic granite; Diagram c and d: WPG−Intraplate granite; ORG−Mid-ocean ridge granite; VAG−Volcanic rocks-arc granite; SYN−COLG—Syn-collisional granite
表 3 宣和岩体稀土元素、微量元素含量（10-6）及特征值表
Table 3 Trace elements (10-6) and rare elements (10-6) compositions of Xuanhe granite mass
下载: 导出CSV
表 4 志留纪侵入岩Rb−Sr、Sm−Nd同位素组成分析
Table 4 Rb−Sr and Sm−Nd isotope data of Silurian intrusive rock
下载: 导出CSV
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