Detrital zircon U-Pb dating of Nanhua meta-tuffite in South Jiangxi and constraint on the time limit of the rift basin
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摘要:
江西省宁都某地新元古代浅变质岩风化壳中赋存离子吸附型稀土矿，文章对某矿区内原定青白口纪库里组的2件变质沉凝灰岩样品进行了碎屑锆石LA-ICP-MS U-Pb年代学研究，获得了88组和110组谐和年龄。2件样品的碎屑锆石年龄区间相似，主要分布在：810~780 Ma，峰值年龄为798 Ma（n=55）；748~727 Ma，峰值年龄为737 Ma（n=127）；691~667 Ma，峰值年龄为680 Ma（n=6），此外还有少量的年龄分布在2.85~1.08 Ga。认为，变质沉凝灰岩样品的沉积时代可能为南华纪，地层应归属为上施组；物源可能来自江南造山带东段（赣东北—皖南—浙西）青白口纪晚期—南华纪的火山-沉积岩；赣南区域上同时期的巨厚海相火山-碎屑沉积可能形成于华南古大陆裂解之后的裂谷盆地，赣南次级裂谷盆地的沉积时限为810~727 Ma。
Abstract:Ion-adsorption type REE deposits is hosted in regolith of Neoproterozoic epimetamorphic rocks in South Jiangxi, China. LA-ICP-MS U-Pb dating of detrital zircons from two metamorphic tuff samples of the originally identified Kuli Formation of Qingbaikou System in a mine area yielded the harmonic ages of 88 groups and 110 groups respectively. They are predominantly Neoproterozoic and have ages ranging from 810 to 667 Ma with three age peaks at ca 798 Ma (n=55), 737 Ma (n=127) and 680 Ma (n=6). There are also a few Meso-to Paleoproterozoic zircon grains with ages scattering from 2.85 Ga to 1.08 Ga. The dating results probably suggest that the sedimentary age of the tuffite may be Nanhua Period. It is speculated that the provenance may be volcanic-sedimentary rocks of late Qingbaikou Period to Nanhua Period in the eastern part of Jiangnan orogenic belt (northeast Jiangxi-southern Anhui-western Zhejiang). The super thick marine volcanic-clastic sediments of the same period in southern Jiangxi might be formed in the rift basin after the breakup of the ancient continent of South China, and the sedimentary time of the secondary rift basin in southern Jiangxi is about 810-727 Ma.
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1. 引言
华南新元古代构造-岩浆演化一直存在较大争议。江西地处华南腹地，新元古代地层及岩浆岩出露较好，是研究华南新元古代构造演化的重要地区。赣南广泛出露新元古代浅变质岩系，其原岩为一套海相火山-碎屑沉积，厚度达千米，近年在其风化壳中发现了离子吸附型稀土矿(赵芝等，2017)。目前，对浅变质岩系的研究程度很低，因缺乏精确的同位素年代学依据其沉积时代归属不一致：1︰20万宁化幅地质报告中将其归属为震旦纪(福建省冶金工业局，1972➊)，而1:5万长胜幅中归属为青白口纪(南方工业学校，1997➋)。对浅变质岩系沉积的构造环境认识也存在分歧：一种观点认为其沉积于裂谷盆地(舒良树，2012；Wang et al., 2013；杨明桂等，2015；邓奇等，2016)；另一种观点认为其沉积于弧-盆体系(周博文等，2018)。为了限定江西宁都某离子吸附型稀土矿区内变质沉凝灰岩的沉积时限、探讨其物质来源和沉积盆地的构造性质，本文对矿区内的2件变质沉凝灰岩样品进行了碎屑锆石LA-ICP-MS U-Pb年代学研究。
2. 地质概况及样品特征
赣中南地区(F2萍乡—广丰断裂带以南)零星分布中元古代结晶基底(寻乌岩组片岩、变粒岩和片麻岩)(图 1)，其上为青白口系—下古生界强烈褶皱的基底，其中青白口系—南华系为浅变质的火山-碎屑沉积，震旦系、寒武系和奥陶系为笔石相碎屑岩系，以韵律状泥砂质岩层为特征(舒良树，2012)。沉积盖层由未变质的上泥盆统、石炭系、二叠系、下三叠统等浅海相碳酸盐岩和泥砂岩以及上三叠统、侏罗系、白垩系和古近系陆相碎屑-火山岩组成，新近系仅零星分布(舒良树等，2006)。
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图 1 江西省中—新元古代地层分布略图(据刘亚光，1997修改)1—寻乌岩群(1.8~1.7 Ga, 刘邦秀等，2001)；2—铁沙街组(1.13~1.17 Ma，高林志等，2013；张恒等，2015b)；3—田里片岩(1.5~1.04 Ga，Li et al., 2007)；4—万年群和珍珠山群(860~849 Ma，Le et al., 2010; 刘树文等，2012)；5—张村群(860 Ma，高林志等，2014)；7—庐山垄群(840~831 Ma，高林志等，2012a)；8—星子群(825~834 Ma，Shu et al., 2008；关俊朋等，2010)；9—双桥山群(840~823 Ma，高林志等, 2008, 2010, 2011, 2012b；董树文，2010)；10—周潭岩群(834~809 Ma，王孝磊等，2013)；11—登山群(≤830 Ma，陈小勇等，2015)；12—赣南青白口—南华系(800~737 Ma，郭娜欣，2015；周博文等，2018)；13—赣北青白口—南华系(803~751 Ma，高林志等，2012b；Wang et al., 2013；王剑等，2013)；14—震旦系；F1 —宜丰—景德镇断裂带；F2 —萍乡—广丰断裂带；F3 —婺源—丰城断裂带；F4—德兴—东乡断裂带；F5 —葛源—樟村断裂带；F6—宜黄—定南断裂带Figure 1. Distribution of the Meso-Neoproterozoic strata in Jiangxi Province (modified from Liu Yaguang, 1997)1-Xunwu rock Group (1.8~1.7 Ga, Liu Bangxiu et al., 2001); 2-Tieshajie Formation (1.13~1.17 Ma, Gao Linzhi et al., 2013, Zhang Heng et al., 2015b); 3-Tianli schist (1.5~1.04 Ga, Li et al., 2007); 4-Wannian and Zhenzhushan Group (860~849 Ma, Le et al., 2010; Liu Shuwen et al., 2012); 5-Zhangcun Group (860 Ma, Gao Gao Linzhi et al., 2014); 6-Wengjialing Formation (841Ma, Zhang Heng et al., 2015a); 7-Lushanlong Group (840~ 831Ma, Gao Linzhi et al., 2012a); 8-Xingzi Group (825~834 Ma, Shu et al., 2008; Guan Junpeng et al., 2010); 9-Shuangqiaoshan Group (840~823 Ma, Gao Linzhi et al., 2008, 2010, 2011, 2012b; Dong Shuwen et al., 2010); 10-Zhoutan rock group (834~809 Ma, Wang Xiaoleng et al., 2013); 11-Dengshan Group (≤830 Ma, ChenXiaoyong et al., 2015); 12-Qingbaikou to Nanhua strata in southern Jiangxi (800~737 Ma, Guo Naxin, 2015; Zhou Bowen et al., 2018); 13- Qingbaikou to Nanhua strata in northern Jiangxi (803~751 Ma, Gao Linzhi et al., 2012; Wang et al., 2013; Wang Jian et al., 2013); 14- Sinian strata; F1- Yifeng- Jingdezhen fault zone; F2- Pingxiang - Guangfeng fault zone; F3- Wuyuan - Fengcheng fault zone; F4-Dexing -Dongxiang fault zone; F5-Geyuan - Zhangcun fault zone; F6-Yihuang - Dingnan fault zone宁都县位于赣南东部、宜黄—定南断裂带以东(图 1)，出露青白口系—寒武系褶皱基底，缺失奥陶系—泥盆系，零星分布石炭系和侏罗系，白垩系出露较广，印支期和燕山期岩浆活动较为发育(图 2)。某地青白口系浅变质岩风化壳中发育离子吸附型稀土矿，矿区出露的地层主要为神山组和库里组，其中神山组呈东西向带状分布，与库里组呈平行不整合接触，岩石类型以千枚岩为主，少量片岩。库里组呈东西向带状展布，与上覆中生代地层呈角度不整合，岩石主要为变沉凝灰岩类和变质砂岩(赵芝等，2018)。
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图 2 江西省宁都地区地质图(据福建省冶金工业局，1972和南方工业学校，1997修编)1—青白口系未分组；2—青白口系神山组；3—青白口系库里组；4—南华系上施组；5—南华系沙坝黄组；6—南华系洪山组；7—震旦系坝里组；8—寒武系；9—石炭系；10—侏罗系；11—白垩系；12—早古生代花岗岩；13—侏罗纪花岗岩；14—侏罗纪闪长岩；15—断层；16—角度不整合；17—整合/假整合；18—样品Figure 2. Geological map of Ningdu County, Jiangxi Province (modified from Fujian Metallurgical Industry Bureau, 1972; Southern Industrial School, 1997)1- Qingbaikou System; 2- Shenshan Formation; 3- Kuli Formation; 4- Shangshi Formation; 5- Shabahuang Formation; 6- Hongshan Formation; 7- Bali Formation; 8- Cambrian System; 9- Carboniferous System; 10- Jurassic System; 11- Cretaceous System; 12- Early Paleozoic granite; 13-Jurassic granite; 14-Jurassic diorite; 15-Fault; 16-Angular unconformity; 17-Conformity/disconformity; 18-Sampling site样品采自宁都某地的离子吸附型稀土矿区，2件样品均为原定的青白口纪库里组第一段，ND-b5的采集层位更靠库里组二段，ND-b34的采集层位更靠神山组二段(图 3)。ND-b5(图 4a、c、e)：呈土黄色，变余碎屑结构，变余层理构造，弱风化。显微镜下见少量的石英晶屑和岩屑(＜5%)，岩屑绢云母化仅残留轮廓；基质多为变质新生的绢云母和经重结晶作用形成的细小的长英质矿物。ND-b34(图 4b、d、f)，呈土黄色，变余碎屑结构，变余层理构造，弱风化，粒度较ND-b5稍粗一些。显微镜下可见长石和石英晶屑(~20%)，呈棱角状，边部裂隙发育；基质为变质新生的绢云母和黑云母，以及重结晶作用形成的细小的长英质矿物。
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图 3 用于碎屑锆石U-Pb测年的变质沉凝灰岩样品的采集层位示意图(据南方工业学校，1997绘编)Figure 3. Sampling locations of meta-tuffite rocks for the detrital zircon U-Pb dating (modified from Southern Industrial School, 1997)![]()
图 4 江西省宁都地区变质沉凝灰岩的野外及显微镜下特征Kfs—钾长石；Qtz—石英Figure 4. Field and microscopic photographs of the meta-tuffites in Ningdu County of Jiangxi ProvinceKfs-Potash feldspar; Qtz-Quartz3. 测试方法
碎屑锆石由北京中兴美科科技有限公司挑选和制靶，锆石靶子上黏贴的锆石颗粒在200~300颗之间。锆石的阴极发光图像由中国地质科学院矿产资源研究所电子探针实验室技术人员拍摄。笔者在显微镜下观察了锆石的透射和反射光特征并采集了相关图像。在此基础上开展了锆石U-Pb测试，测试工作在中国地质科学院矿产资源研究所LA-MC-ICP-MS实验室完成，所用仪器为Finnigan Neptune型MC-ICP-MS及New Wave UP213激光剥蚀系统。实验中激光剥蚀斑束直径为40 μm，频率为10 Hz，能量密度为2.5 J/cm2，以He为载气，采样方式为单点剥蚀。锆石逐一测试，仅排除了裂隙和包体发育的锆石，每10个测试点前后各插入一组标样，以确保标样和测试锆石的仪器条件一致。标样顺序为SRM 610(人造硅酸盐玻璃标样)、GJ-1std(锆石标样)、GJ-1std和Plesovice(锆石标样)，详细的实验测试过程参见文献(侯可军等，2009)。数据处理采用ICPMS Data Cal程序处理，年龄谐和图用Isoplot3.0程序完成，测试数据误差为1σ。对于年轻锆石(< 1000 Ma)采用206Pb/238年龄，对于较老的锆石(>1000 Ma)采用207Pb/206Pb年龄。谐和图中所有年龄数据都有显示，加权平均年龄只选择了谐和度≥95%的年龄，谐和图中灰色背景的数据没有参与加权平均年龄的计算，测试结果见表 1。
表 1 江西省宁都变质沉凝灰岩的LA-ICPMS碎屑锆石U-Pb年龄测试结果Table 1. LA-ICPMS detrital zircon U-Pb dating results of the meta-tuffites in Ningdu County of Jiangxi Province
4. 测试结果
样品ND-b5中的锆石多呈自形的长柱状，粒度多在50~200 μm，大部分锆石表面脏、被熔蚀，也常见锆石内部含包裹体。阴极发光(CL)图像上锆石边部均有亮色边，且发育程度不同(图 5a)。根据CL图像特征可分为两类锆石：第一类锆石发育典型的岩浆震荡环带结构，发光亮度均一；第二类锆石也发育典型的岩浆震荡环带结构，但是环带往往遭受不同程度的破坏，呈现不一样的亮度，这类锆石的年龄往往不谐和。对108颗锆石进行了测年，大部分为第一类锆石，少部分为第二类锆石。其中，88颗锆石的206Pb/238U年龄谐和度≥95%，年龄分布在840~667 Ma，集中在3个年龄区间：809~780 Ma，加权平均年龄为797 Ma(n=35)；746~728 Ma，加权平均年龄为737 Ma(n=46)；685~667 Ma(n=4)(图 6a)。18颗锆石的206Pb/238U年龄谐和度＜95%，未参与加权平均年龄的计算。1颗锆石的206Pb/238U年龄为277 Ma，谐和度为99%，呈长柱状、晶形完好且环带结构发育，推测为外来混入锆石，本文不予考虑。1颗锆石的207Pb/206Pb年龄为2876 Ma，谐和度为97%，呈浑圆状，环带结构发育，可能经历了较长距离的搬运，推测为物源区的古老锆石。
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图 5 江西省宁都地区变质沉凝灰岩中碎屑锆石阴极发光图像及年龄Figure 5. Detrital zircon cathodoluminescence images and U-Pb ages of the meta-tuffites in Ningdu County of Jiangxi Province![]()
图 6 江西省宁都地区变质沉凝灰岩中的碎屑锆石U-Pb年龄谐和图(a, c)及相对频率图(b, d)Figure 6. Detrital zircon U-Pb concordia diagram (a, c) and relative frequency plot (b, d) of the meta-tuffites in Ningdu County of Jiangxi Province样品ND-b34中的锆石多呈自形晶，长柱状，粒度为100~250 μm，多为无色，少部分呈淡红色，大部分锆石表面干净，少部分锆石内部含包裹体。CL图像显示个别锆石边部发育亮边，大部分锆石发育典型的岩浆震荡环带结构，亮度均一，也有的锆石环带遭受不同程度的破坏，内部具熔蚀结构(图 5b)。对120颗锆石进行了测年，测试的锆石内部无包体、表面较干净。110颗锆石的年龄谐和度≥95%，206Pb/238U年龄主要在810~685 Ma(图 6c)，可划分为两个年龄区间：810~785 Ma，加权平均年龄为798 Ma(n=20)；748~727 Ma，加权平均年龄为737 Ma(n=81)。2颗年龄最小的锆石，其年龄分别为691 Ma和686 Ma，与样品ND-b5中最小锆石年龄区间吻合。4颗锆石的207Pb/206Pb年龄为1970 Ma、1887 Ma、1789 Ma和1139 Ma均有磨圆，推测为物源区的古老锆石。10颗锆石的年龄谐和度＜95%，未参与加权平均年龄的计算。
5. 讨论
5.1 碎屑锆石的年龄意义
赣南青白口纪—南华纪浅变质岩系出露于新余市、永丰县及宁都县等地(图 1)，自下而上划分为神山组、库里组和上施组。已有的LA-ICP-MS锆石U-Pb年代学资料显示：于都地区库里组变质沉凝灰岩的年龄为(789.6±2.9) Ma(n=105，MSWD=0.52)(郭娜欣，2015)，永丰地区上施组凝灰质黏土岩的年龄为(774.1±8.8) Ma(n=38，MSWD=1.6)、(774.3±8.5) Ma(n=26，MSWD=1.02)和(756 ±7.5) Ma(n=30，MSWD=0.58)(周博文等，2018)。本文对宁都某地原定库里组中的变质沉凝灰岩的碎屑锆石LA-ICP-MS U-Pb年代学研究表明，两件样品具有相似的年龄峰值。188颗锆石年龄集中在810~667 Ma，最年轻的一组锆石年龄峰值约为680 Ma(n=6，占3%)，次年轻的年龄峰值约为737 Ma(n=127，占67.5%)，从统计学的角度考虑后者的年龄更可靠。沉凝灰岩是由火山碎屑物质落入水盆地中与正常沉积物混杂组成，经化学沉积物和黏土杂基胶结与压实作用成岩的火山作用同期产物。因此，沉凝灰岩中最年轻的一组锆石年龄可以代表区域内最晚期的一次火山事件。研究样品中次年轻的一组锆石均呈自形晶，未显示长距离搬运的特征，可能来自距离较近的火山灰，推测矿区内的变质沉凝灰岩成岩于南华纪，地层归属为上施组，而非库里组。由于岩石组合相似，区域上库里组和上施组的地层归属较为混乱。同时，样品中含较多青白口纪晚期的锆石(~798 Ma的峰值年龄，占29%)，与于都地区库里组变质沉凝灰岩的年龄一致，推测赣南地区青白口纪—南华纪火山-碎屑沉积建造的形成时限在810~727 Ma。
5.2 碎屑锆石的来源
变质沉凝灰岩的碎屑锆石有两个主要的年龄区间：810~780 Ma和748~727 Ma，暗示2件样品具有相似的物质源区。锆石磨圆程度差，说明沉积物源区较近。赣南周潭群分布于弋阳、余江及金溪等地(图 1)，为一套高绿片岩相—低角闪岩相变质岩，主要由灰黑色斜长片麻岩、斜长变粒岩夹绿泥石阳起石片岩、斜长角闪岩组成，原岩为一套海相富铝质泥砂质建造(吴新华等，2001)，厚度大于1200 m，未见底。王孝磊等(2013)对其进行了碎屑锆石U-Pb定年，3件样品最年轻的年龄峰值分别为843 Ma、830 Ma和809 Ma，且有大量1800~1500 Ma和2500~2300 Ma的老锆石。本文样品中缺失843 Ma和830 Ma的峰值年龄，暗示赣南浅变质岩系和周潭群的物质源区存在较大差异。研究显示，赣东北—皖南—浙西北一带普遍存在810~780 Ma和748~727 Ma的火山岩。如，赣东北青白口纪晚期—南华纪自下而上由桃源组(上墅组)、罗村组和听门组组成(张恒等，2015a)(图 7)。其中，桃源组为陆相凝灰岩、流纹岩、玄武岩、火山碎屑岩及火山角砾岩，流纹岩的锆石U-Pb年龄为803 Ma(王剑等，2013)。罗村组以砾岩、泥岩及粉砂质泥岩为主。听门组以砾岩、杂砂岩夹粉砂岩、粉砂质泥岩、页岩为主。皖南地区同期火山-沉积岩由历口群和休宁组组成，沉积厚度约1600 m(图 7)(邓奇等，2019)。历口群下部邓家组由石英砂岩、粉砂岩和板岩组成，上部铺岭组为火山岩，其中流纹岩和凝灰岩的锆石年龄介于765~751 Ma(Wang et al., 2012)。浙西地区同期火山-沉积岩由虹赤村组/上墅组(二者为同期异相)和休宁组组成(图 7)(邓奇等，2019)，沉积厚度超过4300 m。虹赤村组以岩屑砂岩为主夹少量火山岩，火山岩的锆石U-Pb年龄为797 Ma(Li et al., 2003)。上墅组为双峰式火山岩组合，锆石U-Pb年龄在802~773 Ma(Li et al., 2008；Zheng et al., 2008；Wang et al., 2012)。休宁组主要为凝灰质砂岩、凝灰质粉砂岩、凝灰岩及凝灰质、硅质泥岩相互交替，底部为紫红色砾岩和砂砾岩，其中凝灰岩的锆石U-Pb年龄为785 Ma和727 Ma(邓奇等，2019)。江南造山带中800~790 Ma和760~750 Ma的岩浆活动存在明显差别，早期基性岩主要为岩石圈地幔来源，晚期为岩石圈地幔和软流圈地幔双重来源，代表两期不同构造背景下的岩浆事件(邓奇等，2016)。由此推测，本文变质沉凝灰岩样品中810~780 Ma的锆石来自赣东北—皖南—浙北一带同期火山岩-沉积岩，748~727 Ma的锆石主要来自同期的火山灰。
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图 7 江西及其周边青白口纪—南华纪地层对比1—海相火山-碎屑沉积；2—海相沉积；3—陆相火山岩；4—沉积岩；5—地层缺失；6—角度不整合；7—平行不整合Figure 7. Stratigraphic correlation of Qingbaikou System with Nanhua system in Jiangxi and its adjacent regions1-Volcano-clastic marine sediments; 2-Marine sediments; 3-Terrestrial volcanic rocks; 4-Sedimentary rock; 5-Stratigraphic break; 6-Angular unconformity; 7-Parallel unconformity5.3 赣南青白口纪晚期—南华纪沉积盆地的性质
赣南青白口纪—南华纪(810~727 Ma)出露一套巨厚的海相火山-碎屑沉积建造，其中神山组以黑色炭质或含炭千枚岩、含炭粉砂质千枚岩或板岩为主，夹少许千枚岩和变余细砂岩，新余地区厚度大于1050 m，未见底，其上被库里组平行不整合覆盖。库里组以千枚岩、凝灰质千枚岩和千枚状沉凝灰岩为主，新余地区厚2425 m，永丰地区主要为浅灰白色变沉凝灰岩夹多层中酸性熔岩，偶夹炭质绢云千枚岩，厚1186 m，被上施组整合覆盖。上施组为一套变质凝灰质砂岩、变质沉凝灰岩及凝灰质板岩互层，区域上岩性较稳定，宜春地区厚983 m，宁都地区厚544 m，整合于库里组之上。宜春—永丰一带下伏于古家组，宁都一带下伏于沙坝黄组(刘亚光，1997)。神山组黑色岩系及含黄铁矿构造与饥饿盆地的主要沉积相似，这种黑色岩系在湘桂次级裂谷盆地中广泛分布(王剑等，2001)，库里组和上施组为海相火山岩相组合，可能是盆地堆积、充填的产物。江南造山带发育的800~750 Ma的岩浆岩形成于陆内裂谷盆地(徐先兵等，2015；邓奇等，2016)。从沉积序列和岩浆特征推测赣南青白口纪—南华纪火山-碎屑沉积形成于次级裂谷盆地。从赣南至赣北，南华纪沉积物由单向物源为主，即同期火山喷发物为主，改变为双向物源，即古老的陆源物质和早期—同期的火山物源(王孝磊等，2013；Wang et al., 2013；陈小勇等，2015)，反映了南华纪海、陆古地理单元差异的特征。区域上湘桂次级裂谷盆地于沉积时限在819~814Ma(周汉文等，2002；Wang et al., 2003)，赣东北江南次级裂谷盆地于803 Ma开始沉积(王剑等，2013)，浙北次级裂谷盆地约807 Ma开启(王剑，2000)。680 Ma之后，华南进入稳定的陆缘滨海—浅海斜坡相沉积环境(舒良树，2012)。
6. 结论
(1) 碎屑锆石LA-ICP-MS U-Pb测年结果表明，江西省宁都某离子吸附型稀土矿床中的2件变质沉凝灰岩样品具有相似的锆石年龄组成，主要分布在810~780 Ma、748~727 Ma和691~667 Ma三个年龄区间，峰值年龄分别为798 Ma(n=55)、737 Ma(n=127)和680 Ma(n=6)，其次含有少量2.85~1.08 Ga的古老锆石。最年轻的一组碎屑锆石可能为同期火山灰携带的岩浆锆石，可代表沉凝灰岩的形成时代，即南华纪，地层应归属于上施组，而非库里组。
(2) 赣南青白口纪晚期至南华纪巨厚的海相火山-沉积建造可能代表了华南古大陆解体之后的裂谷盆地沉积，宁都某地变质沉凝灰岩的碎屑锆石年龄约束了赣南次级裂谷盆地的沉积时限，即798~680 Ma。
注释
➊福建省冶金工业局. 1972.1:20万宁化幅区域矿产调查报告[R].
➋南方工业学校. 1997. 1:5万长胜幅地质图及说明说[R].
致谢: 感谢两位匿名审稿专家对本文提出的宝贵意见，提高了文章质量。感谢中国地质科学院矿产资源研究所白鸽研究员对第一作者在赣南稀土成矿理论研究中的指导。他是白云鄂博稀土-铌-铁矿及南方离子吸附型稀土矿研究的先锋，也是白云鄂博铌矿的发现者之一，为我国稀土事业做出了杰出贡献。不幸的是，白鸽研究员于2020年1月26日驾鹤西去，笔者谨以此文缅怀先生！ -
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图 1 江西省中—新元古代地层分布略图(据刘亚光，1997修改)
1—寻乌岩群(1.8~1.7 Ga, 刘邦秀等，2001)；2—铁沙街组(1.13~1.17 Ma，高林志等，2013；张恒等，2015b)；3—田里片岩(1.5~1.04 Ga，Li et al., 2007)；4—万年群和珍珠山群(860~849 Ma，Le et al., 2010; 刘树文等，2012)；5—张村群(860 Ma，高林志等，2014)；7—庐山垄群(840~831 Ma，高林志等，2012a)；8—星子群(825~834 Ma，Shu et al., 2008；关俊朋等，2010)；9—双桥山群(840~823 Ma，高林志等, 2008, 2010, 2011, 2012b；董树文，2010)；10—周潭岩群(834~809 Ma，王孝磊等，2013)；11—登山群(≤830 Ma，陈小勇等，2015)；12—赣南青白口—南华系(800~737 Ma，郭娜欣，2015；周博文等，2018)；13—赣北青白口—南华系(803~751 Ma，高林志等，2012b；Wang et al., 2013；王剑等，2013)；14—震旦系；F1 —宜丰—景德镇断裂带；F2 —萍乡—广丰断裂带；F3 —婺源—丰城断裂带；F4—德兴—东乡断裂带；F5 —葛源—樟村断裂带；F6—宜黄—定南断裂带
Figure 1. Distribution of the Meso-Neoproterozoic strata in Jiangxi Province (modified from Liu Yaguang, 1997)
1-Xunwu rock Group (1.8~1.7 Ga, Liu Bangxiu et al., 2001); 2-Tieshajie Formation (1.13~1.17 Ma, Gao Linzhi et al., 2013, Zhang Heng et al., 2015b); 3-Tianli schist (1.5~1.04 Ga, Li et al., 2007); 4-Wannian and Zhenzhushan Group (860~849 Ma, Le et al., 2010; Liu Shuwen et al., 2012); 5-Zhangcun Group (860 Ma, Gao Gao Linzhi et al., 2014); 6-Wengjialing Formation (841Ma, Zhang Heng et al., 2015a); 7-Lushanlong Group (840~ 831Ma, Gao Linzhi et al., 2012a); 8-Xingzi Group (825~834 Ma, Shu et al., 2008; Guan Junpeng et al., 2010); 9-Shuangqiaoshan Group (840~823 Ma, Gao Linzhi et al., 2008, 2010, 2011, 2012b; Dong Shuwen et al., 2010); 10-Zhoutan rock group (834~809 Ma, Wang Xiaoleng et al., 2013); 11-Dengshan Group (≤830 Ma, ChenXiaoyong et al., 2015); 12-Qingbaikou to Nanhua strata in southern Jiangxi (800~737 Ma, Guo Naxin, 2015; Zhou Bowen et al., 2018); 13- Qingbaikou to Nanhua strata in northern Jiangxi (803~751 Ma, Gao Linzhi et al., 2012; Wang et al., 2013; Wang Jian et al., 2013); 14- Sinian strata; F1- Yifeng- Jingdezhen fault zone; F2- Pingxiang - Guangfeng fault zone; F3- Wuyuan - Fengcheng fault zone; F4-Dexing -Dongxiang fault zone; F5-Geyuan - Zhangcun fault zone; F6-Yihuang - Dingnan fault zone
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图 2 江西省宁都地区地质图(据福建省冶金工业局，1972和南方工业学校，1997修编)
1—青白口系未分组；2—青白口系神山组；3—青白口系库里组；4—南华系上施组；5—南华系沙坝黄组；6—南华系洪山组；7—震旦系坝里组；8—寒武系；9—石炭系；10—侏罗系；11—白垩系；12—早古生代花岗岩；13—侏罗纪花岗岩；14—侏罗纪闪长岩；15—断层；16—角度不整合；17—整合/假整合；18—样品
Figure 2. Geological map of Ningdu County, Jiangxi Province (modified from Fujian Metallurgical Industry Bureau, 1972; Southern Industrial School, 1997)
1- Qingbaikou System; 2- Shenshan Formation; 3- Kuli Formation; 4- Shangshi Formation; 5- Shabahuang Formation; 6- Hongshan Formation; 7- Bali Formation; 8- Cambrian System; 9- Carboniferous System; 10- Jurassic System; 11- Cretaceous System; 12- Early Paleozoic granite; 13-Jurassic granite; 14-Jurassic diorite; 15-Fault; 16-Angular unconformity; 17-Conformity/disconformity; 18-Sampling site
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图 3 用于碎屑锆石U-Pb测年的变质沉凝灰岩样品的采集层位示意图(据南方工业学校，1997绘编)
Figure 3. Sampling locations of meta-tuffite rocks for the detrital zircon U-Pb dating (modified from Southern Industrial School, 1997)
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图 4 江西省宁都地区变质沉凝灰岩的野外及显微镜下特征
Kfs—钾长石；Qtz—石英
Figure 4. Field and microscopic photographs of the meta-tuffites in Ningdu County of Jiangxi Province
Kfs-Potash feldspar; Qtz-Quartz
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图 5 江西省宁都地区变质沉凝灰岩中碎屑锆石阴极发光图像及年龄
Figure 5. Detrital zircon cathodoluminescence images and U-Pb ages of the meta-tuffites in Ningdu County of Jiangxi Province
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图 6 江西省宁都地区变质沉凝灰岩中的碎屑锆石U-Pb年龄谐和图(a, c)及相对频率图(b, d)
Figure 6. Detrital zircon U-Pb concordia diagram (a, c) and relative frequency plot (b, d) of the meta-tuffites in Ningdu County of Jiangxi Province
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图 7 江西及其周边青白口纪—南华纪地层对比
1—海相火山-碎屑沉积；2—海相沉积；3—陆相火山岩；4—沉积岩；5—地层缺失；6—角度不整合；7—平行不整合
Figure 7. Stratigraphic correlation of Qingbaikou System with Nanhua system in Jiangxi and its adjacent regions
1-Volcano-clastic marine sediments; 2-Marine sediments; 3-Terrestrial volcanic rocks; 4-Sedimentary rock; 5-Stratigraphic break; 6-Angular unconformity; 7-Parallel unconformity
表 1 江西省宁都变质沉凝灰岩的LA-ICPMS碎屑锆石U-Pb年龄测试结果
Table 1 LA-ICPMS detrital zircon U-Pb dating results of the meta-tuffites in Ningdu County of Jiangxi Province
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