Confirmation of gneissic granite of Qingbaikou period and its constraint on the timing of the Rodinia supercontinent on the Altun orogenic belt
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摘要:
阿尔金造山带新元古代花岗岩的研究对探讨该地区Rodinia超大陆汇聚阶段构造演化过程具有重要意义。本文对在亚干布阳一带新厘定的青白口纪片麻状花岗岩开展了详细的岩石学、年代学和岩石地球化学研究。锆石LA-ICP-MS U-Pb年代学证据显示片麻状花岗岩结晶年龄分别为（883.0±3.3）Ma和（883.1±3.3）Ma，说明其侵位于青白口纪。地球化学结果显示，常量元素具有富硅、铝、钾和低钠、镁、钙和钛的特点，具钙碱性-高钾钙碱性、过铝质花岗岩特征。岩石轻稀土分馏较强而重稀土分馏较弱，具有明显的负Eu异常，总体呈右倾的“V”型稀土分配模式。岩石富集Rb、Th、LREE等大离子亲石元素，中等亏损Ba，强烈亏损Nb、Sr、P、Hf、Ti等高场强元素，总体特征显示了典型的壳源花岗岩的特征，其源于地壳变质砂岩部分熔融，形成于同碰撞晚期构造环境，属Rodinia超大陆汇聚阶段的产物。综合研究表明，阿尔金地区新元古代早期同碰撞型岩体的形成时代集中在871~945 Ma，限定了Rodinia超大陆汇聚时限，且在空间上构成了一条重要的岩浆岩带，是对Rodinia超大陆碰撞汇聚作用的响应。
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关键词:
- 片麻状花岗岩 /
- LA-ICP-MS锆石U-Pb定年 /
- 地球化学 /
- 构造环境 /
- Rodinia超大陆 /
- 地质调查工程 /
- 阿尔金
Abstract:The study of the Neoproterozoic granites in the Altun orogenic belt is significant for revealing the area of the Rodinia supercontinent convergent stage tectonic evolution. In this paper, a detailed study of petrology, chronology and geochemistry was carried out for a new division of Qingbaikou gneissic granite in Yaganbuyang area. The U-Pb dating of zircons from the gneissic granite using LA-ICP-MS yielded (883.0±3.3)Ma and (883.1±3.3)Ma, indicating that the gneissic granite was generated in Qingbaikou period. The geochemical analysis shows that major elements are characterized by high SiO2, Al2O3 and K2O values and low Na2O, MgO, CaO and TiO2 values, thus belonging to the calc-alkaline-high-K calc-alkaline series, and peraluminous.REE distribution patterns show negative anomaly of Eu, obvious fractionation of LREE and weak fractionation of HREE, with a clear V trough, which shows the features of crustal derived granite. The gneissic granite is rich in large ion lithophile elements of Rb, Th, LREE, slightly depleted in Ba and mightily depleted in high field strength elements of Nb, Sr, P, Hf, Ti. These characteristics are similar to features of the continental collision type granite. The source rock of the gneissic granite was formed by the partial melting metasandstone from the crust in the subduction-collisional environment about Rodinia supercontinent. Comprehensive study shows that these syn-collisional granites were generated between 871 Ma and 940 Ma, which constrained the timing of the Rodinia supercontinent in Early Neoproterozoic along the Altun orogenic belt. These rock bodies have the characteristics of zonal distribution in space and confirm the existence of syn-collisional granites belt about Rodinia supercontinent on the Altun orogenic belt.
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1. 引言
地下水中的化学成分可以示踪地下水的循环途径, 反映地下水流系统的特征；而地下水水化学类型是地下水化学成分的集中反映，也是地下水水文地球化学特征研究的重要内容之一(袁道先，1990；沈照理和王焰新，2002；王焰新等，2005)。水文地球化学结合同位素示踪的方法可更深入研究区域地下水的循环特征和水动力场特征(刘文波等，2010；李向全等，2011；郭晓东等，2014；袁建飞等，2016；孙厚云等，2018)。晋祠泉出露于太原西山悬瓮山下，由难老泉、圣母泉、善利泉组成，1954—1958年实测泉水平均流量为l.94 m3/s。与晋祠泉同处太原西山山前断裂带的平泉，1978年建立了特大型岩溶水自流井水源地，自流量最大达到1.56 m3/s。由于这些自流井的开采，使晋祠泉的流量急剧下降，1994年4月30日断流。为建设美丽山西，省政府将规划实施晋祠泉复流工程。因此研究晋祠泉的补给来源、晋祠—平泉水力联系成为一项重要课题。
2. 研究区概况
山西太原晋祠泉域位于太原盆地的北部，泉域面积2713 km2(梁永平等, 2019)。其碳酸盐岩含水层为下古生界寒武系和奥陶系，连续沉积厚度超过900 m。晋祠岩溶地下水主要接受西山碳酸盐岩裸露区及覆盖区的降水人渗补给、汾河及支流在碳酸盐岩段的渗漏补给(后期又加入水库渗漏补给)。晋祠泉域岩溶地下水排泄方式主要包括：晋祠泉、平泉、通过西山边山断裂带向盆地内松散层的潜流排泄以及人工开采井。晋祠泉位于北北东向晋祠断裂之南端，位于岩溶发育的排泄区，为西山岩溶地下水的天然集中排泄点，断裂西侧出露有奥陶系峰峰组石灰岩，断裂东侧为第四系松散层，岩溶地下水向东遇第四系松散层的阻挡而沿断裂上升溢出地表形成泉水(图 1)。晋祠泉群泉总流量在20世纪50年代平均为1.95 m3 /s，60年代为1.61 m3 /s，70年代为1.21 m3 /s，80年代为0.52m3/s(晋华等, 2005)。1960年以前基本上为天然动态。平泉则位于交城至清徐的北东东向断裂带之北端，晋祠泉的下游，是西山岩溶地下水的人工排泄点之一，泉水出露高程为784.31~86.87 m。2011年8月，清徐县平泉村“不老泉”和沙河底“水巷”两处泉水呈现复流迹象。2016—2018实测群泉总流量分别为0.067 m3/s、0.084 m3/s、0.114 m3/s。
3. 研究技术与方法
通过开展野外地质、水文地质补充调查，查明晋祠、平泉水文地质条件。于2016年5月在晋祠泉域边山断裂带取样24组。其中简分析9组，全分析15组(表 1)。2016年5月—2018年5月布置水质长观点两处，分别为晋祠泉口岩溶井、平泉村不老池泉水。pH、温度、电导率等指标直接通过WTW多功能水质监测仪现场测试获得；Ca、HCO3离子由德国默克测试盒现场滴定。化学分析在中国地质科学院岩溶地质研究所国土资源部重点实验室完成。2H/18O同位素(中国地质科学院岩溶地质研究所国土资源部重点实验室)测定精度分别为±2.0‰和±0.1‰；δ34S值在中国地质调查局武汉地质调查中心实验室完成测试，δ34S值采用IsoPrime质谱仪进行测定，δ34S值采用CDT(Canyon Diablo Meteorite)标准，测试精度优于±0.1‰。所有水样阴阳离子平衡相对误差小于5%，利用水化学模拟软件Phreeqc计算矿物饱和指数；利用Origin软件绘制离子比例系数图、同位素分析。
表 1 取样点基本信息Table 1. The information of sampling point
4. 晋祠—平泉水力联系分析
4.1 水位动态特征
地下水位动态变化，是反映含水层中地下水资源量变化的一个指征，地下水位的上升或下降，直接反映了地下水补给与消耗量的变化(陶虹等, 2013)。根据地下水水位动态监测资料分析，在1980年前，地下水水位的变化随降水量的大小而变化，呈稳定状态(图 2)；1980—1992年，晋祠泉地下水水位的变化呈稳定下降趋势，主要原因是有太原化学工业公司、开化沟、淸徐县平泉村和梁泉村等水源地大量开采岩溶地下水，导致地下水水位下降；1993—2005年，整个泉域地下水水位急剧下降，主要原因是岩溶水开采量急剧加大和降水量减少(图 3)；2005—2012年，泉域地下水水位呈上升趋势，主要原因是万家寨引黄工程，“关井压采”，部分工矿企业置换利用黄河水，中小煤矿整治与关停，汾河实施清水复流工程(二库修建)，使泉域内岩溶地下水水位有明显回升(图 2)。
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图 3 晋祠泉流量与岩溶水开采量变化趋势对比曲线(a)及晋祠泉—平泉流量关系线（b），资料来源山西省第一水文地质工程地质队；1—晋祠泉流量；2—晋祠泉域岩溶地下水开采量；3—平泉流量Figure 3. Comparison curve of Jinci spring discharge and karst water exploitation(a) and the discharge relation between Jinci spring versus Pingquan spring(b)1-Jinci spring flow; 2-Karst groundwater exploitation in Jinci spring area; 3- Pingquan spring flow4.2 水化学特征
岩溶水化学成分受区域内的地质条件、水动力条件和人类工程活动等因素的控制，并能够较好的保存这种影响“信息”。因此，水文地质工作者经常利用水文地球化学方法研究复杂的岩溶水系统(Smykatz-Kloss et al., 1990; Fairchild et al., 2006; Musgrove et al., 2010; Rui Ma et al., 2011;唐春雷等，2019)。依据工作所取得岩溶地下水，碎屑岩井水样分析结果，得出岩溶水pH值6.92~7.86，均值为7.35。钙离子95.3~417.0 mg/L，均值为226.9 mg/ L。硫酸根离子149~1219 mg/L，均值为633 mg/L。碎屑岩井水30.5~73.1 mg/L，均值为60.0 mg/L。硫酸根离子35~90 mg/L，均值为66 mg/L。岩溶水(泉)总体特征表现为阳离子高钙镁、低钾钠，阴离子低氯，高硫酸根。按照舒卡列夫分类法，研究区碳酸盐岩含水岩组地下水主要类型是Ca-SO4型与Ca-SO4·HCO3型。其中Ca-SO4·HCO3型主要分布在西山断裂带北部。Ca-SO4型主要分布在西山断裂带南部。碎屑岩井地下水主要类型是Ca · NaHCO3型。晋祠泉、平泉同为Ca-SO4型(表 2)。
表 2 晋祠泉域岩溶地下水水化学类型Table 2. Karst groundwater hydrochemical type of Jinci spring catchment
研究区岩溶地下水化学组分主要受方解石(文石)、白云石和石膏等矿物影响。SO42-+ HCO3-与Ca2++Mg2+关系图(图 4a)显示，岩溶地下水样品呈直线分布并偏离至1:1线以下，表明少量有煤矿排水，地表水的混入岩溶地下水中。Na++K+-Cl与Ca2++ Mg2+ - SO42-- HCO3-关系图(图 4b)显示，径流区部分点位于阳离子交换线附近，说明地下水水化学形成除方解石(文石)、白云石和石膏的溶解，还有阳离子交换作用。
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图 4 龙子祠岩溶地下水离子关系图a—(SO4+ HCO3)-(Ca2++Mg2+)图; b—(Na++K+-Cl-)-(Ca2++Mg2+-SO4-HCO3)图; c—SO42+ -TDS图; d—Sr2+ -Ca2+图; 1—晋祠泉；2—平泉；3—碎屑岩井；4—岩溶井Figure 4. Ion relation diagrams of karst groundwater in Longzicia-(SO4+ HCO3)versus(Ca2++Mg2+); b-(Na++K+-Cl-)versus(Ca2++Mg2+-SO4-HCO3); c-SO42+ versus TDS; (d-Sr2+ versus Ca2+; 1-Jinci spring; 2-Pingquan spring; 3-Clastic rock well; 4-Karst well在TDS是反映水质的综合指标。研究区TDS与硫酸根含量存在着极高的线性相关(图 4c)。区域岩溶地下水中SO42-主要来源有奥陶系碳酸盐岩含水层石膏溶解，煤矿酸性水和大气降水中的硫酸根(张海潇等, 2019)。说明含水层石膏溶解，煤矿酸性水补给，大气降水中的硫酸根是影响TDS的主要因素之一。
岩溶水循环过程中，Sr2+浓度随着径流途径和水岩交互作用的时间而增加，相比之下Ca2+浓度却受制于溶解平衡，因此，不同来源的水的Sr2+/Ca2+值不同，径流途径和水岩交互作用的时间越长，其值越大，反之越小(Keul et al., 2017; Yokota et al., 2018; Pracný et al., 2019)。如图 4(d)所示岩溶水径流区(晋祠泉J17，J24，J13，J19，J18，J21，J20)，排泄区(平泉，J04，J11，J10，J12，J01，J07)，热水井(J16，J15) Sr2+浓度随着径流途径增加。热水井(J16，J15)Sr2+浓度最高，其原因是水岩交互作用的时间较长。
4.3 同位素环境特征
δ34S-SO42-被广泛用于追踪水中硫酸盐的来源氢(Temovski et al., 2018; Xiao et al., 2018; Zhou et al., 2018; Sim et al., 2019)。氢氧同位素是研究地下水起源与演化的理想示踪剂，可利用地下水中的稳定氢氧同位素识别研究区地下水补给来源(Schiavo et al., 2009; Capaccioni et al., 2011; Pasvanoğlu, 2013; Zhang and Li, 2019)。晋祠泉—平泉段岩溶地下水的δ18O变化在-9.7‰~-8.5‰，δD变化在-70.1‰~-63.9‰，平均值分别为-9.3‰和-68.4‰。，该段岩溶水样点均散落于太原站大气降水线右下方(图 5a)，表明其主要补给来源为大气降雨。晋祠—平泉一带岩溶地下水氢氧同位素值较接近，说明这一带补给来源与补给途径相近。
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图 5 岩溶地下水δD-δ18O关系图(a)及岩溶地下水及其他类水δ34S-SO42系图(b)Figure 5. Diagram of δD versus δ18O(a) and diagram of S δ34S vs SO42-(b)地下水中硫酸盐主要有3种来源，即降水、蒸发岩溶解和硫化物或有机硫氧化。在水文地球化学研究中，常使用δ34S对水中硫酸盐的来源进行标定。大量研究表明，山西中奥陶统石膏的δ34S值为23.8‰ ~31.4‰，矿坑水中的δ34S值为- 13.6% ~ 7.98‰，新近系黄土中δ34S值为5.5‰~9.5‰，汾河及其支流与引黄水的中δ34S值7.9‰~10.66‰。从晋祠泉—平泉段岩溶水δ34S分布图(图 5b)，可以看出，岩溶地下水的δ34S值总体较大，接近于石膏的δ34S值范围，说明岩溶地下水中的SO42-主要来源于石膏溶解。
4.4 晋祠—平泉水化学水质监测分析
为了分析晋祠—平泉水力联系的水化学证据，在晋祠难老泉、不老池开展了逐月水化学含量动态监测(Ca2+、Mg2+、K++Na+、Cl-、SO42-、NO3-)。2016年5月至2018年5月共50组水样，如图 6所示晋祠泉与平泉各个离子变化趋势基本一致。说明晋祠与平泉存在紧密的水力联系。平泉Ca2+、Mg2+、SO42-、K++Na+含量显著高于晋祠泉，而Cl-、NO3-含量则低于晋祠泉。
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图 6 晋祠泉及平泉水主要水化学组分含量月均动态Figure 6. Monthly average dynamics of main hydrochemical components in Jinci Spring and Pingquan Spring4.5 径流途径水化学演化
反向地球化学反应路径模拟是定量研究水文地球化学演化的重要手段。反应路径模拟的理论基础是沿地下水同一水流路径，终点的水化学成分和同位素的质量等于起点的水化学成分和同位素的质量加上两点间由于水岩作用(如沉淀、溶解、阳离子交换等)、蒸发作用和不同水流的混合作用引起的化学组分和同位素的转移量，通过质量平衡反应模型和同位素质量传输模型，可推测地下水从起点到终点间的水文地球化学反应路径(Plummer et al., 1990; Petalas and Lambrakis, 2006; Han et al., 2011; Cánovas et al., 2016)。
4.5.1 饱和指数与可能矿物相的确定
饱和指数能反映常见的含有碳酸盐类、硫酸盐类和硅酸盐类等矿物与地下水之间所处的溶解平衡状态，这是反向水文地球化学模拟计算的基础。利用Phreeqc计算各矿物饱和指数(表 3)，由表 3可以看出：方解石、文石、白云石的饱和指数均大于0，说明它们在地下水中呈饱和状态，具有沉淀趋势；石膏、硬石膏和岩盐的饱和指数均小于0，说明它们在地下水中处于非饱和状态，具有继续溶解趋势。依据饱和指数分析结果，选择石膏、方解石、白云石、NaCl，作为水文地球化学模拟的“可能矿物相”。
表 3 岩溶地下水中矿物饱和指数Table 3. Mineral saturation index in karst groundwater
4.5.2 Phreeqc水化学模拟
应用Phreeqc软件确定了水中各种组分和矿物的饱和状态；通过物质平衡模型，来确定岩溶地下水系统径流路径上不同两点之间矿物沉淀或溶解的数量。晋祠—平泉径流路径发生的主要水岩作用为：石膏的溶解，方解石沉淀、岩盐稀释和二氧化碳气体溶解或逸出等。
5. 对晋祠泉复流的贡献
晋祠泉与平泉同属于一个晋祠泉岩溶地下水系统，都位于西山山前边山断裂带的排泄区。晋祠与平泉存在紧密的水力联系。说明晋祠泉与平泉存在一个比较强的导水通道。可以通过在晋祠泉下游导水通道上帷幕灌浆，提高晋祠泉水水位，使晋祠泉出流。此方案的优点：(1)晋祠泉水水质明显优于平泉。(2)降低下游带压煤矿开采突水的风险。(3)晋祠泉水出流以地表水渠形式管理调度，生态人文环境影响较小。
6. 结论
(1) 在1980年前，晋祠泉地下水水位的变化随降水量的大小而变化，呈稳定状态；1980—1992年，地下水水位的变化呈稳定下降趋势，主要原因是大量开采岩溶地下水；2005—2012年，地下水水位呈上升趋势，主要原因是万家寨引黄工程，关井压采，部分工矿企业置换，汾河实施清水复流工程(二库修建)，使泉域内岩溶地下水水位有明显回升。
(2) 研究区碳酸盐岩含水岩组地下水主要类型是Ca-SO4型、Ca-SO4·HCO3型。Ca-SO4·HCO3型主要分布在西山断裂带北部。Ca-SO4型主要分布在西山断裂带南部。碎屑岩井地下水主要类型是Ca·Na-HCO3型。晋祠泉、平泉同为Ca-SO4型。
(3) 晋祠泉的δ18O和δD值分别为- 9.39‰，- 68.5‰。平泉的δ18O和δD值分别为- 9.29‰，-71.0‰。其点均散落于太原站大气降水线右下方，表明晋祠泉与平泉的主要补给来源为大气降雨，氢氧同位素值较接近，说明晋祠泉与平泉补给来源与补给途径相近。研究区岩溶地下水的δ34S值总体较大，接近于石膏的δ34S值范围，说明岩溶地下水中的SO42-主要来源于石膏溶解。
(4) 晋祠与平泉存在紧密的水力联系，晋祠泉与平泉存在一个比较强的导水通道。可以通过帷幕灌浆，提高晋祠泉水水位，使晋祠泉出流。
致谢: 中国地质调查局西安地质调查中心校培喜教授级高级工程师和西北大学刘良、柳小明教授在论文写作过程中提供了建设性意见, 谨此表示感谢。 -
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图 1 阿尔金造山带大地构造位置图（a）及研究区地质简图（b）
TRB—塔里木盆地；QL—祁连山；QDB—柴达木盆地；WKL—西昆仑；EKL—东昆仑；HMLY—喜马拉雅山；INP—印度板块；Q—第四系；N2y—新近系油砂山组；J1-2dm—侏罗系大煤沟组；ЄOMm—奥陶纪茫崖蛇绿混杂岩；QbS—青白口系索尔库里群；Pt1A—古元古代阿尔金岩群；O—S玉苏普阿勒塔格岩体；O2-3—帕夏拉依档岩体；νQb—斜长角闪岩；γQb—片麻状花岗岩；γδQb—盖里克片麻岩；γδοQb—亚干布阳片麻岩；OΣH—超基性岩块体；β—玄武岩块体；v—辉长岩脉
Figure 1. Tectonic position map of Altun (a) and geological sketch map of the study area (b)
TRB-Traim Basin; QL-Qilian Mountains; QDB-Qaidam Basin; WKL-Western Kunlun Mountains; EKL-Eastern Kunlun Mountains; HMLYHimalaya Mountains; INP- Indian Plate; Q- Quaternary; N2y- Neogene Youshashan Formation; J1-2dm- Jurassic Dameigou Formation; ЄOMm - Ordovician Mengya ophiolite melange; QbS- Qingbaikou System Suorkuli Group; Pt1A- Palaeoproterozoic Altun rock group; O- S- Yusupualeke Tagh plutons; O2-3-Paxialayidang plutons; νQb-Amphibolite; γQb-gneissic granite; γδQb-Gailike plutons; γδοQb -Yaganbuyang syenogranite; OΣH-Ultrabasic rock block; β-Bsaltic Block; v-Gabbro dyke
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图 2 片麻状花岗岩野外宏观特征及显微镜下照片
a、b—片麻状黑云花岗岩宏观露头照片；c、d—片麻状黑云母花岗岩显微照片（c—PM004/6-1Bb，正交偏光；d—PM003/4-1Bb，正交偏光）；Pl—斜长石；Mi—微斜长石；Q—石英；Bit—黑云母；Mu—白云母；Hb—角闪石
Figure 2. The outcrop and microstructure photos of gneissic granite
A, b-The outcrop photos of gneissoid-biotitic granite; c-Micro-photos of gneissoid-biotitic granite (PM004/6-1Bb, crossed nicols-PM003/4-1Bb, crossed nicols); Pl-Plagioclase; Mi-Microline; Q-Quartz; Bit-Biotite; Mu-Muscovite; Hb-Hornblende
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图 3 片麻状花岗岩（PM003-4）中锆石的CL图像和U-Pb年龄值
Figure 3. Zircon CL image and U-Pb ages of gneissic granite (PM003/4)
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图 4 片麻状花岗岩（PM003-4）锆石U-Pb谐和图
Figure 4. LA-ICP-MS zircon U-Pb concordia diagram for gneissic granite (PM003/4)
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图 5 片麻状花岗岩（PM004-6）中锆石的CL图像和U-Pb年龄值
Figure 5. Zircon CL image and U-Pb ages of gneissic granite (PM004-6)
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图 6 片麻状花岗岩（PM004−6）锆石U−Pb谐和图
Figure 6. LA−ICP−MS zircon U−Pb concordia diagram for gneissic granite(PM004−6)
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图 11 片麻状花岗岩球粒陨石标准化稀土元素配分图（a）和原始地幔标准化微量元素蛛网图（b）
Figure 11. Chondrite-normalized REE patterns (a) and primitive mantle-normalized trace element patterns (b) of gneissic granite
after Sun and McDonough, 1989
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图 12 片麻状花岗岩Rb/Ba−Rb/Sr图解（底图据Sylvester, 1998）
Figure 12. Rb/Ba−Rb/Sr diagrams of gneissic granite (after Sylvester, 1998)
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图 13 片麻状花岗岩A/MF−C/MF成因图解（底图据Alther et al., 2000）
Figure 13. AFM−CFM diagrams of gneissic granite (after Alther et al., 2000)
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图 14 片麻状花岗岩微量元素构造环境判别图解
Figure 14. Diagrams of the tectonic setting of major elements for gneissic granite
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图 15 片麻状花岗岩Hf−Rb/30−Ta×3三角判别图解（底图据Harris et al., 1986
Figure 15. Hf-Rb/30-Ta×3 diagrams of gneissic granite (after Harris et al., 1986)
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图 16 阿尔金青白口纪早期构造演化模式图
Figure 16. Model for the tectonic evolution during the early Qingbaikou period of the Altun
表 1 片麻状花岗岩（样品PM003/4）锆石LA−ICP−MS U−Pb同位素分析结果表
Table 1 LA−ICP−MS zircon U−Pb isotopic analysis results of gneissic granite(sample PM003-4)
下载: 导出CSV
表 2 片麻状花岗岩(样品PM004−6)锆石LA−ICP−MS U−Pb同位素分析结果
Table 2 LA−ICP−MS Zircon U−Pb isotopic analyses of gneissic granite(sample PM004−6)
下载: 导出CSV
表 3 阿尔金造山带片麻状花岗岩主量元素（%）、微量元素（10-6）分析结果
Table 3 Major elements(%) and trace elements(10-6) from gneissic granite in the Altun orogenic belt
下载: 导出CSV
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