塔里木大火成岩省小海子正长岩体的成因过程:对大陆板内地壳生长的指示

梁杰豪 ,  曹俊 ,  万淑敏 ,  吴鹤 ,  郑佳琪 ,  秦如妍 ,  张钰杰

科学技术与工程 ›› 2026, Vol. 26 ›› Issue (15) :6280-6302

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科学技术与工程 ›› 2026, Vol. 26 ›› Issue (15) :6280-6302 DOI: 10.12404/j.issn.1671-1815.2505092
天文学、地球科学

塔里木大火成岩省小海子正长岩体的成因过程:对大陆板内地壳生长的指示

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Petrogenetic Processes of Xiaohaizi Syenite Complex in the Tarim Large Igneous Province, NW China: Implications for Crustal Growth in Continental Interior

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摘要

塔里木大火成岩省作为一个不常见的过渡型大火成岩省,发育了众多具有A型花岗岩特征的碱性中性-长英质侵入岩且与赋含钒钛磁铁矿的镁铁-超镁铁质岩体相伴生。但关于这些碱性中性-长英质侵入岩的成因及其对地壳生长的意义仍存在很大争议。通过岩石学、矿物学、锆石U-Pb年代学、元素地球化学和Sr-Nd-Mg同位素研究,揭示小海子正长岩体的成因过程及其记录的大陆内部地壳生长过程。结果表明,小海子正长岩体岩石类型主要为铁橄榄石正长岩、角闪正长岩、石英正长岩和正长斑岩,形成时代为(283.3±2.1) Ma;全岩样品具有较高的铁指数[FeOT/(FeOT+MgO)=0.76~0.98]、富碱(Na2O+K2O=8.99%~12.2%),低MgO(0.05%~2.37%)、MnO(0.04%~0.17%)和P2O5(0.03%~0.61%),富集大离子亲石元素(Rb、Ba、Th、U)和高场强元素(Nb、Ta),高10 000×Ga/Al(2.83~5.10),属于弱过碱性-准铝质A型花岗岩类。晚期侵入的小海子正长岩类的(87Sr/86Sr)i和εNd(t)分别为0.703 27~0.704 23和-2.70~3.98,接近镁铁-超镁铁质岩体中橄榄辉石岩[(87Sr/86Sr)i=0.704 52~0.704 59, εNd(t)=1.12~2.33],暗示二者可能共同起源于地幔柱。橄榄石微量元素和Mg同位素进一步指示小海子正长岩的母岩浆为受硅酸盐熔体交代的地幔碳酸盐化榴辉岩部分熔融产生的碱性玄武质岩浆。碱性玄武质岩浆经历橄榄石、单斜辉石分离结晶形成橄榄辉石岩,残余熔体进一步通过碱性长石为主堆晶作用形成铁橄榄石正长岩、角闪正长岩和石英正长岩,正长斑岩。可见,地幔在大陆板内环境地壳生长过程中不仅限于作为热源而且可以提供主要物质来源。

Abstract

The Tarim large igneous province (TLIP), recognized as an atypical transitional LIP, contains numerous alkaline intermediate to felsic intrusions that exhibit affinities to A-type granites and are spatially and temporally associated with mafic-ultramafic intrusions hosting Fe-Ti-V oxide mineralization. The petrogenesis of these alkaline intermediate-felsic rocks and their implications for crustal growth remain, however, highly debated. An integrated approach incorporating petrography, mineral chemistry, zircon U-Pb geochronology, whole-rock major and trace element geochemistry, and Sr-Nd-Mg isotope systematics was applied to elucidate the petrogenetic history of the Xiaohaizi syenitic intrusion and its record of intracontinental crustal growth. The results show that the Xiaohaizi intrusion is composed mainly of fayalite syenite, amphibole syenite, quartz syenite, and syenite porphyry, emplaced at (283.3 ± 2.1) Ma. The whole-rock samples are characterized by high Fe-number [FeOT/(FeOT+MgO) = 0.76~0.98], total alkalis (Na2O+K2O = 8.99%~12.2%), and 10 000×Ga/Al ratios (2.83~5.10), together with low concentrations of MgO (0.05%~2.37%), MnO (0.04%~0.17%), and P2O5 (0.03%~0.61%). They are enriched in large-ion lithophile elements (LILEs; e.g., Rb, Ba, Th, U) and high-field-strength elements (HFSEs; e.g., Nb, Ta), and are classified as weakly peralkaline to metaluminous A-type granitoids. The late-stage syenites from Xiaohaizi yield initial (87Sr/86Sr)i ratios ranging from 0.703 27 to 0.704 23 and εNd(t) values from-2.70 to 3.98. These isotopic compositions overlap with those of the olivine pyroxenites from coeval mafic-ultramafic intrusions [(87Sr/86Sr)i = 0.704 52~0.704 59, εNd(t) =1.12 to 2.33], suggesting a common mantle plume source for both rock suites. Trace element compositions of olivine and Mg isotope data (δ26Mg) further indicate that the parental magma of the Xiaohaizi syenites is an alkali basaltic melt derived from partial melting of carbonated eclogite within the mantle, which had been previously modified by silicate melts. Fractional crystallization of olivine and clinopyroxene from this alkali basaltic magma produced the olivine pyroxenites. The residual melt subsequently experienced extensive cumulate processes dominated by alkali feldspar, giving rise to the fayalite syenite, amphibole syenite, quartz syenite, and syenite porphyry. These findings demonstrate that the mantle acts not only as a thermal engine but also as the primary material source for crustal growth in intracontinental settings.

Graphical abstract

关键词

A型花岗岩 / 正长岩 / 碳酸盐化榴辉岩 / 分离结晶作用 / 塔里木大火成岩省

Key words

A-type granite / syenite / carbonated eclogite / fractional crystallization / Tarim large igneous province

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梁杰豪, 曹俊, 万淑敏, 吴鹤, 郑佳琪, 秦如妍, 张钰杰. 塔里木大火成岩省小海子正长岩体的成因过程:对大陆板内地壳生长的指示[J]. 科学技术与工程, 2026, 26(15): 6280-6302 DOI:10.12404/j.issn.1671-1815.2505092
LIANG Jie-hao, CAO Jun, WAN Shu-min, WU He, ZHENG Jia-qi, QIN Ru-yan, ZHANG Yu-jie. Petrogenetic Processes of Xiaohaizi Syenite Complex in the Tarim Large Igneous Province, NW China: Implications for Crustal Growth in Continental Interior[J]. Science Technology and Engineering, 2026, 26(15): 6280-6302 DOI:10.12404/j.issn.1671-1815.2505092

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碱性岩浆虽然在地球上体积占比很小(小于1%[1-2]),但可以为原始岩浆分异过程提供重要的信息[3]。理解碱性岩浆的岩石学和地球化学特征,对于限定源区和地幔深处的原始熔体分离过程,以及阐明大陆地壳的分异和演化至关重要[4]。碱性岩浆有多种类型,正长岩是其中最典型的一类。一般认为,碱性杂岩体中的正长岩及伴生岩主要由交代地幔低程度部分熔融形成,可能与裂谷或地幔柱相关[5-6]。在岩浆侵位过程中,分离结晶和强烈的成分分层也是正长岩的普遍特征[7-9];同时下地壳中碱性镁铁质母岩浆的分离结晶和岩浆混合作用也可能对产生不同类型的正长岩起着重要作用,如科拉正长岩。因此,正长岩成因的复杂性可能源自地幔的交代和熔融过程,以及壳-幔相互作用与岩浆演化过程[3,10-12]。
二叠纪塔里木大火成岩省是中国继峨眉山大火成岩省之后发现的又一大火成岩省,其镁铁质岩石的分布面积约为265 000 km2,而长英质岩石的面积约为48 000 km2。基于其高比例的长英质岩石,Cheng等 [13]将塔里木大火成岩省归类为过渡型大火成岩省。长期以来,关于大火成岩省中常见的中性-长英质岩石是代表了相关玄武质岩石的结晶分异,还是来源于其他过程,存在广泛争议。实验岩石学表明,花岗质成分可以通过地壳岩石的部分熔融或幔源玄武质岩浆的分离结晶获得[14-15]。大火成岩省中性-长英质岩石复杂的成因模式对地壳的形成造成多解性[16]。需要指出的是,中性-长英质侵入岩(正长岩类、碱性花岗岩)主要分布在塔里木大火成岩省西北缘巴楚地区和皮羌地区,且多与赋含钒钛磁铁矿镁铁-超镁铁质岩体相伴生,组成了独特的“二元”岩石组合[17]。那么二者究竟具有什么样的成因联系以及能否作为钒钛磁铁矿的找矿标志同样亟需回答。因此,现以巴楚地区的小海子正长岩类为研究对象,旨在深入理解地球深部的物质属性以及“二元”岩石组合,也将对进一步探究塔里木大火成岩省深部动力学过程和理解大陆内部环境下地壳生长演化过程具有重要意义。

1 地质背景

位于中国新疆维吾尔自治区西南部的塔里木克拉通是中国三个主要克拉通之一,北邻天山造山带,南接昆仑造山带,东南部为阿尔金造山带。塔里木克拉通发育有典型的双层结构,由前寒武纪的变质结晶基底和显生宙沉积盖层两部分组成[18-19]。塔里木克拉通发育多期岩浆活动,其中早二叠纪岩浆岩在克拉通内部分布最为广泛,其岩性主要由大陆溢流玄武岩和流纹岩以及镁铁质-超镁铁质侵入岩体或岩墙群、A型花岗岩、碱性正长岩及少量的方解霞黄煌岩-霞石岩-霞石正长岩-碳酸岩为主的过碱性岩所组成[20-22]。塔里木二叠纪玄武岩和流纹岩的分布面积分别为2.65×105 km2和0.48×105 km2,规模与峨眉山大火成岩省相当,因此塔里木早二叠纪板内岩浆岩亦构成了又一个大火成岩省,即塔里木过渡型大火成岩省(图1)[13,20]。已有的研究证据表明,塔里木大火成岩省是地幔柱活动的产物,主要证据包括:①现深部地幔来源(约150 km)的含金刚石的富碳酸盐超镁铁质煌斑岩(方解霞黄煌岩[23]);②规模的地壳隆升(半径约为300 km的圆形区域,中心隆升高度达887 m[24]);③在与塔北二叠纪玄武岩同时代的高温苦橄质熔岩(估算的地幔潜能温度>1 300 ℃[25])。与塔里木地幔柱相关的岩浆活动至少分为三期:第一期约为300 Ma,以塔里木克拉通西北部巴楚瓦吉里塔格地区的富碳酸盐超镁铁质煌斑岩(方解霞黄煌岩[26])和碳酸岩为代表;第二期约为290 Ma,以广泛分布于塔里木内部的溢流玄武岩和流纹岩构成的双峰式火山岩为代表[13,20-21];第三期为280~270 Ma,以分布于塔里木克拉通西北缘的各类侵入岩(包括各类岩墙)为代表,主要包括碱性镁铁-超镁铁质侵入岩、岩墙群、正长岩、碱性花岗岩和过碱性岩类[22,27]。

2 小海子岩体地质特征

小海子岩体位于塔里木大火成岩省西北缘,新疆巴楚县东南约25 km处的小海子水库东侧,主要由橄榄辉长岩、橄榄辉石岩、正长岩和石英正长岩组成[28-29]。岩体呈等轴圆形,出露面积约12.6 km2,侵位于志留系-早二叠统地层中[图1(b)][30]。橄榄辉长岩和橄榄辉石岩大多被第四系沉积物覆盖,仅见零星露头。钻孔揭示镁铁-超镁铁质岩厚度超过750 m[30],铁矿石储量为3亿t(含16%~25%FeO,3%~4%TiO2,0.1%V2O5),从而与同处于塔里木大火成岩省西北缘的赋含大型钒钛磁铁矿的瓦吉里塔格(铁矿石储量为1.46亿t,含20%FeO,5.5%~8.5%TiO2,0.15%~0.20%V2O5)[31-32]和皮羌岩体共同构成了巴楚-阿图什地区钒钛磁铁矿矿集区[33]。正长岩杂岩体呈岩株状分布于岩体北部,出露较为完整。在岩体的北部、南部边缘橄榄辉石岩与正长岩接触,岩体东部出露堆晶的橄榄辉石岩体[图2(a)][34]。小海子正长岩体以角闪正长岩为主,同时局部发育少量铁橄榄石正长岩[图2(b)],两者之间为侵入接触关系[28]。年代学研究表明小海子碱性杂岩体的不同岩性端元近乎同时形成,其中橄榄辉长岩年龄为286.1~(283±3) Ma[29],橄榄辉石岩为279~278 Ma[27],正长岩体为286~277 Ma[28,35-36],辉绿岩为285~272 Ma[37]和石英正长斑岩为284~273 Ma[28,36]。

3 岩相学

铁橄榄石正长岩样品较为新鲜,呈灰色,发育中-粗粒结构[图2(c)]。矿物组合主要包括碱性长石(80%~90%)、角闪石(<10%)、单斜辉石(<5%)、铁橄榄石(≤3%)、石英(<5%)以及斜长石(<1%)。副矿物主要为磷灰石、铁钛氧化物以及锆石。就长石类而言,碱性长石以条纹长石为主,并伴随少量钠长石和微斜长石,晶体粒度范围在0.1~1.5 cm。角闪石作为最主要的暗色矿物,常在铁橄榄石和单斜辉石颗粒边缘发育形成反应边[图2(c)],内部可包含锆石、磷灰石和铁钛氧化物包裹体。辉石通常被角闪石包裹,部分细小辉石颗粒(约0.1 mm)则被碱性长石包裹。石英含量低(<1%),粒径为0.1~1.6 mm,通常充填于长石颗粒间隙或与钠长石直接接触。自形磷灰石多被角闪石包裹[图2(d)],极少形成集合体。少量斜长石呈他形,主要分布于碱性长石颗粒之间。

角闪正长岩样品呈浅灰白色,具中粗粒结构[图2(e)]。主要矿物组成为碱性长石(80%)、角闪石(8%)、黑云母(5%)、石英(5%)以及斜长石(1%~3%)。副矿物主要为铁钛氧化物、锆石以及磷灰石。就长石类而言,碱性长石以条纹长石和钠长石为主,暗色矿物集合体主要由黑云母和角闪石构成。呈自形至半自形的黑云母[图2(e)],粒径为0.25~4.5 mm,多与角闪石共生,其内部常含有针状磷灰石及铁钛氧化物包裹体。

浅肉红色石英正长岩整体呈中粗粒结构[图2(f)],主要由碱性长石构成(75%),此外还含有角闪石(7%)、黑云母(8%),并伴随一定量的石英(5%~10%)。少量磷灰石、铁钛氧化物和锆石也可出现。碱性长石以钠长石和条纹长石为主。暗色矿物集合体主要由黑云母和角闪石构成。石英含量为4%~6%,粒径介于0.2~2.5 mm,主要充填于碱性长石颗粒间隙或与角闪石、黑云母接触。

正长斑岩呈暗肉红色,典型的斑状结构[图2(g)]。岩石由斑晶和基质两大部分构成,其中斑晶约占50%,主要成分为斜长石(20%~25%)、碱性长石(15%~20%)以及石英(5%~8%)。斜长石粒径介于0.7~2.9 mm,周围可见环带构造及聚片双晶发育,颗粒形态多呈半自形板状或他形粒状。碱性长石粒径为0.7~2.8 mm,形态为他形板状或粒状。石英粒径0.6~2.6 mm,呈他形粒状。基质主要由碱性长石与石英微晶组成。

橄榄辉石岩呈黑色,中粗粒结构[图2 (h)]。矿物成分中,单斜辉石(35%~45%)与橄榄石(25%~35%)占优势,斜长石和铁钛氧化物的比例均介于5%~10%,同时伴随少量角闪石及黑云母(<5%)。在部分样品中,斜长石含量可超过单斜辉石。呈自形至半自形的单斜辉石和橄榄石粒径为0.5~5 mm,发育显著的堆晶结构。斜长石呈不规则形态充填于单斜辉石与橄榄石颗粒间隙,少量被粗粒单斜辉石包裹[图2(h)]。角闪石主要分布于橄榄石或单斜辉石边缘,而黑云母则常与分布于硅酸盐矿物粒间的铁钛氧化物共生。

4 分析方法

选取小海子岩体24件样品进行相关分析,其中铁橄榄石正长岩5件、角闪正长岩7件、石英正长岩3件和正长斑岩7件以及橄榄辉石岩2件。

本文研究的全岩主、微量元素分析工作在中国科学院地球化学研究所矿床地球化学国家重点实验室完成。主量元素采用ARL Perform X 4200型X射线荧光光谱仪(X-ray fluorescence spectrometer,XRF)测试,相关实验流程参考文献[38],分析精度优于1%。微量元素测试中,样品经酸溶消解处理后,利用PlasmaQuant MS Elite型电感耦合等离子体质谱仪(inductively coupled plasma mass spectrometry,ICP-MS)进行测定。实验过程选用国际标准物质GBPG-1、AGV-2及OU-6实施全过程质量监控,数据精度普遍优于5%。

矿物(除橄榄石外)主量元素分析及锆石U-Pb定年均在东华理工大学核资源与环境国家重点实验室开展。其中,U-Pb定年实验基于激光剥蚀电感耦合等离子体质谱(laser ablation inductively coupled plasma mass spectrometry,LA-ICP-MS)完成,使用仪器为NWR femto 257激光剥蚀系统和PE NexION 1000型等离子体质谱仪(ICP-MS)。普通Pb采用Anderson [39]提出的方法进行校正。矿物原位主量元素测试采用JEOL JXA-8100型电子探针,各元素含量校正标样均为天然矿物。原始数据经原子序数Z、吸收A、荧光F校正法校正,有效消除测试过程中的背景噪声与信号干扰,分析误差≤2%。

橄榄石成分及全岩Sr-Nd同位素在武汉上谱分析科技有限公司进行,使用仪器分别为Thermo Fisher Neptune Plus型多接收杯电感耦合等离子体质谱仪(multi-collector inductively coupled plasma mass spectrometry,MC-ICP-MS)和配备有GeolasPro激光剥蚀系统的Agilent 7700e ICP-MS。其中橄榄石微量元素测试详细的仪器参数和分析流程见文献[40]。数据处理基于多外标无内标校正法,全程采用玻璃标准物质组合(BHVO-2G、BCR-2G、BIR-1G及NIST SRM 610)实施质控校准。全岩Mg同位素分析利用Thermo-Finnigan Neptune plus MC-ICP-MS完成,实验方法参考文献[41]。根据分析结果,标样BHVO-2和JB-2的δ26Mg值分别为-0.26‰±0.03‰和-0.18‰±0.01‰,近似于国际同类实验室测试值(-0.24‰±0.05‰和-0.21‰±0.05‰)[42]。同时,空白样的Mg含量仅为0.76 ng,明显低于实验室平均值(10 ng)。

5 分析结果

5.1 锆石U-Pb定年

锆石U-Pb测年数据如表1所示。石英正长岩样品XHZ-14所获得的锆石,其粒径范围为60~200 μm,长宽比介于1∶1~2∶1,形态多呈自形或半自形,未见明显包裹体 (图3)。本次分析锆石在CL图像中普遍发育清晰的岩浆振荡或扇形环带,表明其为岩浆过程的产物。此外,这些锆石Th、U含量变化范围分别为(14.9~121)×10-6与(24.4~175)×10-6,其较高的Th/U(0.47~0.89)亦符合岩浆锆石的判别特征[43]。

经计算,11个锆石谐和年龄计算的加权平均206Pb/238U年龄为(283.3±2.1) Ma(2σ,均方加权偏差MSWD=1.3, 图3),这与前人报道的角闪正长岩、铁橄榄石正长岩、石英正长斑岩中锆石U-Pb年龄(表2),代表小海子正长岩体的结晶年龄。因此,结合野外接触关系和已有的高精度定年结果,小海子正长岩体和镁铁-超镁铁质岩体是同期岩浆的产物。

5.2 全岩主微量元素组成

小海子岩体的全岩主量及微量元素分析结果如表3与表4所示。所有样品在显微镜下均未观察到显著蚀变现象,且烧失量极低(LOI = 0.56%~1.59%),表明分析的样品未遭受明显的岩浆期后蚀变作用影响。因此,小海子岩体的主量元素与微量元素数据能有效代表其原始岩浆成分。

在全碱-二氧化硅(total alkali vs silica,TAS)图解中,铁橄榄石正长岩样品落在正长岩区域[图4(a)],具有碱性特征[图4(b)],SiO2=58.6%~61.4%,Al2O3=17.7%~18.4%,Fe2O3T=4.19%~6.27%,MgO=0.94%~1.83%,Mg#值为13.2~36.6;CaO=2.27%~4.41%,具有较高的Na2O(5.61%~6.53%)和K2O(2.80%~4.30%)含量,A/CNK=0.88~0.91,表现出钾玄质与准铝质的性质[图4(c)、图4(d)]。铁橄榄石正长岩具有较低的稀土总量∑REE=(245~431)×10-6。在全岩微量元素图解中(图5),铁橄榄石正长岩表现出轻稀土富集,重稀土相对平坦的右倾型式[(La/Yb)N=15.4~24.9],具有弱的Eu异常(Eu/Eu*=0.70~1.40)。富集Ba(645~1 002)×10-6、Nb(48.3~62.2)×10-6、Ta(4.67~5.36)×10-6、亏损Sr(575~827)×10-6、Th(4.98~19.2)×10-6和 U(2.08~2.82)×10-6。

角闪正长岩具有SiO2(56.2%~62.3%)、CaO(2.19%~4.41%)、Na2O(6.19%~6.64%)和K2O(2.80%~4.49%),在TAS图解中位于正长岩区域[图4(a)]; Al2O3含量为15.3%~18.0%,Fe2O 3T为3.84%~8.29%,MgO为0.67%~2.37%,TiO2为0.56%~1.65%,A/CNK=0.72~0.92,在地球化学分类图解中可见属于碱性[图4(b)、准铝质[图4(d)]岩石系列。稀土总量为(255~311)×10-6。在全岩微量元素图解中(图5),稀土元素配分模式表明,这些样品具有轻稀土富集的特征,重稀土分布较为平坦 [(Gd/Yb)N=2.60~2.77]。其稀土分异程度属中等水平 [(La/Yb)N=10.9~17.6],并呈现出明显的Eu正异常 (Eu/Eu*=0.90~1.60)。亏损Th(8.37~12.4)×10-6,U(1.88~3.13)×10-6、Zr(299~560)×10-6、Hf(9.43~17.6)×10-6元素,富集Rb(74.9~102)×10-6和Ba(746~1 202)×10-6元素;Nb/Ta为9.90~11.8,Zr/Hf为29.0~33.1,Th/U为3.61~6.28。

石英正长岩SiO2(67.4%~73.4%)含量较高,Fe2O 3T(3.61%~3.93%)和MgO(0.09%~0.35%)含量较低。Al2O3含量中等,为11.3%~15.2%,A/CNK =0.85~0.94[图4(d)]。该岩石类型具有低CaO(0.40%~0.71%)、高Na2O(4.81%~5.75%)和高K2O(4.18%~5.06%)的特征,Na2O/K2O范围为 1.14~1.17。相较于角闪正长岩,石英正长岩样品呈现更高的稀土元素总量[∑REE=(306.4~442.0)×10-6]。由球粒陨石标准化图解可见轻稀土元素富集,(La/Yb)N(11.4~16.1)和(Gd/Yb)N(2.81~3.06)均较高,并具有Eu正异常(Eu/Eu*=0.50~1.30)。石英正长岩具有较高的Rb/Sr(0.16~0.97),而Sr/Y(2.50~14.7)和Dy/Yb(2.68~2.70)则较低。

正长斑岩与石英正长岩表现出相似的特征,SiO2=59.8%~65.8%,Al2O3=14.5%~17.8%,Fe2O3T=2.08%~6.52%, MgO=0.05%~0.90%,CaO=0.81%~2.56%,具有较高的Na2O(4.20%~6.30%)和K2O(4.20%~6.10%)含量, A/CNK=0.90~0.97[图4(d)]。由球粒陨石标准化图[图5(a)]可见,正长斑岩表现出富集轻稀土、亏损重稀土的模式,(La/Yb)N介于13.2~23.6,具有明显的Eu正异常(Eu/Eu*=0.30~1.40)。在原始地幔标准化微量元素蛛网图解中[图5(b)],正长斑岩显示富集Nb(45.2~91.5)×10-6、Ta(2.91~7.09)×10-6、La(42.9~192)×10-6;亏损Th(7.91~25.2)×10-6、U(1.76~4.94)×10-6、Sr(63.0~687)×10-6、Zr(453~952)×10-6、Hf(14.1~25.7)×10-6元素的特点;Nb/Ta为11.7~17.7,Zr/Hf为31.2~40.7,Th/U为3.15~5.97。

橄榄辉石岩的SiO2=42.7%~43.5%,Al2O3=17.7%~19.6%,Fe2O3T=16.1%~ 16.6%,MgO=10.5%~19.9%,Mg#值为58.8~72.5。橄榄辉石岩具有最低的稀土总量∑REE为(74.98~134.44)×10-6,其稀土元素准化图解[图5(a)]表现为轻稀土和重稀土略亏损,中稀土富集的特征[(La/Yb)N=9.20~10.7,(Gd/Yb)N=3.18~3.48)],并且具有轻微的Eu正异(δEu=0.95~1.01)和Ce异常(δCe=1.02~ 1.03)。原始地幔标准化蛛网图中可见明显的Ba、Nb、Sr、Ti、Zr和Hf 的正异常[图5(b)],与辉绿岩墙相类似。

5.3 全岩Sr-Nd-Mg同位素

小海子岩体中铁橄榄石正长岩、角闪正长岩和橄榄辉石岩等的Sr-Nd-Mg同位素如图6、表5所示。铁橄榄石正长岩的初始锶同位素比值(87Sr/86Sr)i在0.703 27~0.703 48,钕同位素比值(143Nd/144Nd)i为0.512 458~0.512 462,对应εNd(t)为3.58~3.66;而角闪正长岩显示(87Sr/86Sr)i=0.704 23、(143Nd/144Nd)i=0.512 135及εNd(t)为负值(-2.70);相比之下,橄榄辉石岩同位素更显著富集,(87Sr/86Sr)i=0.704 52~0.704 59,(143Nd/144Nd)i=0.512 331~0.512 393,εNd(t)= 1.12~2.33。橄榄辉石岩的δ26Mg明显轻于地幔值(-0.25±0.07‰),范围为-0.54‰~-0.16‰[41]。与塔里木大火成岩省其他岩石相比,小海子橄榄辉石岩的δ26Mg与巴楚辉绿岩(δ26Mg=-0.31‰~-0.28‰)、碱玄岩(δ26Mg=-0.38‰~-0.30‰)、霞石岩(δ26Mg=-0.55%~-0.35‰)、霞石正长岩(δ26Mg=-0.62‰~-0.50‰)和方解霞黄煌岩(δ26Mg=-0.75‰~-0.36‰)变化范围一致,但重于(δ26Mg=-0.91‰~-0.85‰)响岩和碳酸岩(δ26Mg=-1.09‰~-0.65‰)[21,27,46]。

5.4 矿物化学

分别对小海子铁橄榄石正长岩、角闪正长岩和正长斑岩中的角闪石、黑云母和长石矿物进行了电子探针分析。角闪石表现出贫硅(SiO2=40.3%~49.8%),富铁(FeOT=14.2%~32.9%)的特征,Na2O=0.36%~2.82%,K2O=0.20%~1.10%。以23个氧原子为单位计算的晶体化学式中的阳离子,根据2012年国际矿物委员会角闪石命名方案[50],铁橄榄石正长岩、角闪正长岩及正长斑岩中的角闪石矿物皆归属于钙角闪石系列,Mg#值为46.2~62.9,TiO2含量为0.56%~1.62%,Al2O3为3.66%~6.45%,FeOT为19.0%~32.9%,MgO为8.55%~11.6%,CaO为9.52%~11.7%,Na2O为0.86%~2.24%和K2O为0.43%~1.09%。在角闪石分类图解中主要分布于镁角闪石至铁浅闪石区域[图7(a)、图7(b)]。相较铁橄榄石正长岩、角闪正长岩及正长斑岩,橄榄辉石岩内角闪石呈现显著差异:FeOT与K2O含量相对偏低,而TiO2、MgO、Al2O3、CaO及Na2O组分则略高。角闪石的Si/(Si+Ti+Al)均小于0.90,具有幔源成因特征[51]。正长斑岩中黑云母的SiO2=34.9%~37.6%,FeOT=25.5%~30.8%,MgO=5.80%~8.40%,K2O=8.80%~9.40%,成分变化不大,表现出富铁黑云母的特征[图7(c)]。角闪正长岩和铁橄榄石正长岩以斜长石和碱性长石为主[图7(d)],两类长石颗粒在成分上均较为均一,变化范围局限。斜长石成分为奥长石(An7.7~29.9Ab66.5~90.1Or2.1~5.8);碱性长石主要为歪长石,成分为(An4.0Ab63.9Or32.1)[52]。此外,对小海子橄榄辉石岩中橄榄石的微量元素进行了精确测定,测试结果如表6所示。这些橄榄石Fo[即Mg/(Mg+Fe)]=73.0%~80.0%,Ca=(1 683~2 060)×10-6,Ti=(120~178)×10-6,Mn=(1 820~2 277)×10-6,Ni=(1 573~1 945)×10-6,不同于典型的幔源橄榄石捕掳晶(Ca<700×10-6, Ti<70×10-6, Mn<1 045×10-6, 2 200×10-6≤Ni≤3 400×10-6) [53-54],反映出岩浆成因的特征。

6 讨论

6.1 小海子碱性正长岩体母岩浆特征

小海子铁橄榄石正长岩、角闪正长岩、石英正长岩和正长斑岩具有低的SiO2(56.8%~73.1%)和高Ba(228~1 269)×10-6、Sr含量(63.0~827)×10-6,暗示其不属于高分异花岗岩。因此,基于全岩成分的分类方法适用于小海子正长岩类。根据Frost等[55]的分类,小海子正长岩类具有铁质、准铝质和碱性特征,因此可以认为它们同样属于A型花岗岩(图8)[56]。此外,角闪正长岩、石英正长岩中黑云母成分也显示出A型花岗岩的特征[图9(a)、图9(b)]。根据微量元素和矿物学特征,A型花岗岩可以进一步分为来源于类似洋岛玄武岩(OIB)岩浆和地壳源区的两类[57-59]。

Eby[57]和Whalen等[59]的高场强微量元素分类图以及黑云母地球化学表明,小海子岩石属于A1亚类,即来源于类似于洋岛玄武岩的母岩浆,伴随很少或没有地壳物质的混染。小海子正长岩Sr-Nd同位素组成[(87Sr/86Sr)i=0.703 23~0.805 12,εNd(t)=-2.70~3.97];表5所示明显不同于以新元古代花岗岩[(87Sr/86Sr)i=0.711 5,εNd(t)=-21.25]和早中古生代花岗岩[(87Sr/86Sr)i=0.709 2,εNd(t)=-8.46]为代表的塔里木下、上地壳物质,因此推断小海子正长岩未受到明显的地壳物质混染[60-61]。此外,偏铝质的全岩成分和富Ca的暗色矿物(如角闪石、钙铁辉石等)的存在表明小海子正长岩与铁质、过碱性和碱性花岗岩类的演化不同,因为它们含有碱性的镁铁质硅酸盐矿物(即钠闪石-钠铁闪石、霓石)。各岩类均存在碱性长石、磁铁矿、榍石和黑云母等,该矿物组合指示母岩浆具有较高的Fe2O3和K2O含量,富碱、富水和贫硅特征[62]。尽管如此,仍然推断小海子碱性正长岩体的母岩浆成分可能与洋岛玄武岩相似,类似于巴楚辉绿岩墙。

6.2 源区属性

A型长英质岩石可能的源区包括:①交代岩石圈地幔[63-64];②残留的或变质基性下地壳[65-66];③地幔和地壳物质的混合;④亏损的软流圈上地幔[28,67]。部分熔融实验表明源区斜长石在低压下相对稳定;残留相中无斜长石而存在石榴子石+角闪石的组合需在压力≥1.0~1.2 GPa(约地壳40 km深度)或更高条件下才会发生[68-70]。由于长石在地壳熔融期间是稳定的,壳源A型花岗岩通常表现出低的Ba和Sr含量,以及明显的Eu负异常[71],但小海子正长岩体高Ba(228~1 269)×10-6和Sr(63.0~827)×10-6含量[图5(b)],以及Eu正异常(Eu/Eu*=0.30~1.60;图5(a),这与源区残留相为斜长石不相符。此外,小海子正长岩在手标本上未观察到明显的暗色包体,同时具有低的MgO(0.05%~2.37%)和Fe2O3T含量(2.08%~6.52%),不具有基性岩浆混合的特征。小海子正长岩中的角闪石颗粒具有较高的MgO(3.16%~12.7%)和TiO2(0.18%~2.06%)含量,成分上属于镁角闪石,更接近幔源岩浆中富镁的角闪石。虽然前人在小海子辉绿岩墙中识别出206Pb/238U年龄为2 480~717 Ma的继承锆石[72],但通过二端元混合模拟的结果表明小海子正长岩的形成受到了<10%的地壳熔体混合,因此小海子正长岩也不可能是壳源酸性岩浆与幔源基性岩浆混合后分异的产物。

小海子正长岩体各岩类相对富集大离子亲石元素,无Nb、Ta、Zr、Hf的负异常[图5(b)],稀土元素配分模式为右倾型[图5(a)],显示出与OIB相似的特征,指示初始岩浆源自地幔[73]。值得指出的是,小海子地区出露的正长岩是塔里木大火成岩省内唯一发现含有铁橄榄石的正长岩,暗示其可能与赋含超大型钒钛磁铁矿矿床的镁铁-超镁铁质侵入体有密切的成因关系[28-29]。邵辉等[74]提出无论是部分熔融还是分离结晶过程对Th/Hf和Ta/Hf的影响都较小,因此可以用来判断岩浆源区属性。相较于小海子橄榄辉石岩(Th/Hf=0.60~0.73, Ta/Hf=0.34~0.37;表1)和辉绿岩墙(Th/Hf=0.59~0.78, Ta/Hf=0.37~0.50)[33],小海子正长岩具有相近的Th/Hf(0.34~1.32,平均值为0.88)和Ta/Hf(0.12~0.51,平均值为0.31),说明其与小海子镁铁-超镁铁质侵入体有明显的亲源性。此外,正长岩的(87Sr/86Sr)i=0.703 23~0.805 12,εNd(t)=-2.70~3.97,与镁铁-超镁铁质侵入体中橄榄辉石岩单元的值接近[(87Sr/86Sr)i=0.704 52~0.704 59,εNd(t)=1.12~2.33],也表明了两者具有明显的亲源性。同样地,小海子铁橄榄石正长岩和正长斑岩的εHf(t)分别为4.8~7.1和5.7~9.5,δ18O则为4.11‰~4.67‰和4.20‰~4.77‰,类似于280 Ma的亏损地幔εHf(t)和δ18O值[75]。因此,小海子碱性正长岩体可能与镁铁-超镁铁质侵入体共同来自FOZO型地幔柱源区。

橄榄石是幔源原始岩浆中典型的初始结晶相,其微量元素(如Ni、Fe、Mn、Co和Zn等)可能记录了地幔的组分特征和岩浆过程,因此橄榄石被广泛作为超镁铁-镁铁质岩的成因指示矿物[76-79]。由于Ni在橄榄石和熔体之间的分配系数很高(Kdol/liq=12~45),从橄榄岩熔体中结晶的橄榄石Ni含量通常较低(如MORB),这与小海子橄榄辉石岩中橄榄石不同。次生辉石岩衍生的玄武质岩浆(例如Koolau)[80-81]也很难解释小海子橄榄辉石岩中橄榄石的成分,因为它们的Ni含量高于所研究的样品[图10(a)]。此外,高Fo(78.7~80.0)橄榄石明显偏离橄榄岩-辉石岩的混合趋势[图10(d)]。因此,无论是橄榄岩还是次生辉石岩混合源都不能完全匹配小海子橄榄辉石岩的橄榄石成分变化。综合以上分析,认为小海子橄榄辉石岩更可能源自榴辉岩地幔源区(图10)。然而,如果源区存在榴辉岩,那么其部分熔融的熔体虽然富铁但具有高硅的特征,橄榄石不能从这种熔体中结晶[82]。但是橄榄岩-榴辉岩混合源区来源的橄榄石能在维持稳定的Ni/(Mg/Fe)同时降低其Mn/Fe,这是因为榴辉岩中石榴子石能保留Mn[83]。小海子碱性正长岩具有较高的(La/Yb)N(2.20~3.10),较低的HREE、Sc和Y含量(表4),暗示其可能源自一个含石榴石的富集地幔源区。因此,有理由推测,小海子碱性正长岩体同源原始岩浆来自一个含榴辉岩组分的地幔柱的部分熔融。

橄榄石Ca-Ti图解中两种截然不同的趋势可有效识别地幔源区不同的交代介质类型,即代表由碳酸盐化硅酸盐熔体交代作用形成的Ca和Ti的共同富集和代表由富Fe、Ti硅酸盐熔体交代作用影响的高Ti但无Ca富集[76]。小海子橄榄辉石岩中橄榄石显示高的Ca和Ti含量(图11),表明源区受到了一定程度碳酸盐组分的交代影响。小海子橄榄辉石岩具有轻Mg同位素特征(δ26Mg=-0.54‰~-0.16‰),表现出源区有再循环碳酸盐化物质的参与。在小海子岩体邻近的瓦吉里塔格碱性杂岩体中曾被报道过~300 Ma火成碳酸岩脉,这可能暗示小海子碱性正长岩体的地幔源区在其产生之前可能遭受携带再循环碳酸盐的新元古代或早古生代俯冲板片交代改造[21]。在俯冲过程中,蚀变洋壳会经历高压相变为榴辉岩,并在碳酸盐脱碳过程中发生同位素交换,形成碳酸盐化榴辉岩。地幔柱上涌过程中捕获的碳酸盐化榴辉岩因其低的固相线温度优先发生部分熔融[82],形成的硅酸盐熔体与地幔橄榄岩反应形成了碱性正长岩的原富碱和贫硅的初始岩浆。

6.3 岩浆结晶条件

小海子碱性正长岩体中普遍存在早期结晶的岩浆型榍石和磁铁矿,说明初始岩浆体系就具有较高的氧逸度。在黑云母Fe/(Fe+Mg)-ΣAl图中[图9(b)],铁橄榄石正长岩和角闪正长岩的氧逸度介于-3.49~-1.17,而石英正长岩和正长斑岩的氧逸度介于-3.44~-2.77。由于黑云母为晚期结晶相,所以上述特征可能反映晚期结晶阶段,硅饱和熔体向硅过饱和熔体演化过程中氧逸度增高的趋势,并结晶出大量磁铁矿和榍石[83]。类似地,铁橄榄石正长岩中角闪石Fe2+/(Fe2++Mg)为0.46~0.74,高于角闪正长岩[Fe2+/(Fe2++Mg)=0.44~0.47],暗示铁橄榄石正长岩在相对低的氧逸度条件下形成。这种氧化还原条件的变化可能与岩浆结晶过程中Na和K不同的晶体化学行为所决定:K进入一种Fe2+占优势的矿物中,如铁云母,残余岩浆氧逸度升高,反之,Na和Fe3+替换将使岩浆氧逸度降低[87]。

综合锆石CL图像揭示的核-边结构特征及Zr饱和温度计(基于Zr含量与温度的正相关性),表明岩浆处于Zr饱和状态,且获得的Zr饱和温度有效约束了岩浆形成的上限温度。铁橄榄石正长岩和角闪正长岩的全岩Zr饱和温度(1 028~1 122 ℃,平均为1 093 ℃)略低于石英正长岩和正长斑岩(1 107~1 212 ℃,平均为1 113 ℃)。通过锆石Ti温度计对角闪正长岩的结晶温度进行计算,计算结果为689~879 ℃(αSiO2=1,αTiO2=0.6;计算方法见文献[88]),代表了岩浆结晶的最低温度。利用单斜辉石Al温度计[T=93.2W(Al2O3)+(742±40.0) ℃][89][W(Al2O3)为单斜辉石中Al2O3的质量分数],计算出铁橄榄石正长岩结晶温度范围为783~838 ℃,与锆石Ti温度计计算值相近。以上特征表明初始岩浆体系具有高温(679~1 212 ℃)的特征。

侵位深度是基于角闪石地质温压计计算得到。小海子正长岩中角闪石Mg#值的范围主要为1.43~3.14,适用于Hammarstrom等[90]提出的基于角闪石成分温压计。计算结果显示,铁橄榄石正长岩和角闪正长岩结晶压力范围为(0.52~1.80) kbar(1 kbar=100 MPa),平均压力1.19 kbar;石英正长岩和正长斑岩结晶压力范围为(0.74~2.60) kbar,平均压力 1.53 kbar。

6.4 分离结晶作用

如上所述,小海子正长岩为A1亚类,暗示它们是幔源镁铁质岩浆分异的产物[57-58]。在幔源岩浆演化过程中,分离结晶起着至关重要的作用。小海子正长岩具有较高且可变的SiO2(56.2%~73.4%)含量,低的MgO(0.05%~2.37%)、Cr(0.40~33.4)×10-6、Co(1.20~17.6)×10-6和Ni(0.20~32.7)×10-6含量,说明岩石是幔源岩浆经高度演化后的产物。随着La含量的增加,La/Sm没有发生明显的变化[图12(c)],同时Ce/Yb、εNd(t)分别随Ce和SiO2的增加均无明显变化[图12(a)、图12(b)],暗示分离结晶作用在岩浆演化中占据了主导作用。

由图13所示Harker图可知,随SiO2含量逐渐升高,K2O、Na2O则呈正相关增长趋势,而Al2O3、Fe2O3T、MgO及CaO/Al2O3则呈显著负相关。这种成分演化规律指示小海子正长岩体在岩浆结晶过程中发生单斜辉石、铁钛氧化物(磁铁矿/钛铁矿)及磷灰石的分离结晶。铁橄榄石正长岩和角闪正长岩的Zr、Hf、Th和Y随SiO2含量增加而减少,表明锆石和角闪石(或辉石)可能是早期的主要分离结晶相。Sr与Ba含量之间具有良好的正相关性[图12(d)],这也说明岩浆早期可能存在角闪石或辉石的分异。小海子正长岩极度亏损P和Ti,且TiO2随SiO2含量增加而减少,表明磷灰石和富Ti-矿物(如榍石、钛铁矿)也是重要的结晶分异相。实验岩石学表明,在磷灰石和榍石中Sm表现出比Ce和Lu更高的相容性[91-92],石英正长岩和正长斑岩相比于铁橄榄石正长岩和角闪正长岩具有更高的Ce含量[(78.0~524)×10-6]和Lu含量[(0.32~0.87)×10-6]、更低的Sm含量(5.70~22.7)×10-6,也可归因于磷灰石和榍石的分离结晶作用。MgO随SiO2含量升高而持续降低的趋势,进一步证实岩浆体系存在部分黑云母分离结晶。结合微量元素协变趋势:Sr与Ba呈显著正相关[图12(d)],而Rb与Ba呈负相关[图12(e)],共同揭示斜长石、碱性长石及黑云母的分离结晶过程对岩浆演化具有控制作用。典型情况下,斜长石分离结晶会导致熔体Sr和Eu亏损[93],钾长石分离则引发Ba亏损。然而,铁橄榄石正长岩与角闪正长岩样品显示出显著的Ba正异常、弱Eu正异常以及Sr负异常。这一特征组合表明,岩石形成过程中斜长石的分离结晶贡献程度弱于钾长石[94]。值得提出的是,Bachmann等[95]提出,在富水环境中斜长石延缓的结晶,或钛铁矿和角闪石的分离结晶(Eu的分配系数低于相邻的REE),将会导致熔体中Eu含量的增加。同时,考虑到铁橄榄石正长岩和角闪正长岩的Eu与Ba显示正相关关系[图12(f)],暗示小海子正长岩可能演化自一个富水环境,大量碱性长石的堆晶造成Ba、Eu的正异常。

小海子正长岩表现出富集Th、U、Zr、Hf等元素的特征而橄榄辉石岩显示出明显的亏损Th、U、Zr、Hf(图5),说明小海子正长岩可能代表了镁铁-超镁铁质侵入体堆晶后的残余熔体[96]。为了进一步验证小海子正长岩体来源于碱性玄武质岩浆分离结晶后的残余熔体,使用高镁辉绿岩墙样品(W13)[31]代表熔体模拟的起始岩浆成分,设置起始温度为1 300 ℃,结束温度为800 ℃,H2O=2.0%,压力为1 kbar。模拟结果表明,岩浆温度降至约945 ℃时,14%斜长石、46%单斜辉石、16%橄榄石和不足1%铁钛氧化物的矿物组合分离结晶时能产生与小海子正长岩杂岩相近的岩浆成分(图13)。在温度持续降至820 ℃时,36%斜长石、28%单斜辉石、6%黑云母、1%磷灰石和4%钛铁氧化物的矿物组合分离结晶时产生与小海子石英正长岩相近的岩浆成分。

6.5 对大陆板内地壳生长的指示

大火成岩省作为地球最大规模的火山活动,记录了巨量岩浆在短时限内的侵位与喷发过程[97]。长英质岩石在大火成岩省中通常相伴产出,比例通常<10%,部分长英质岩石单元可达9 000 km3[98]。但塔里木大火成岩省的长英质岩体出露面积达0.48×105 km2(占18%),与澳大利亚Woongarra及南非Bushveld同属过渡型大火成岩省[13,99]。因此,塔里木大火成岩省中大规模的长英质岩浆活动为理解大陆板内地壳生长提供了罕见的实例,也对理解大火成岩省地球化学特征和壳幔分异过程具有重要意义[100-101]。

大火成岩省内的长英质岩浆大多具有A型花岗岩特征,起源于高温环境。由于地幔柱的高温环境[102],使得上覆岩石圈或地壳中易熔或难熔的物质都有机会参与岩浆的演化过程之中,如岩石圈中富集组分、亏损地幔、基性下地壳等多端元组分[103]。这也就造成了大火成岩省内的中酸性岩浆具有多样性。A型(包括过碱性和铝质亚类)花岗岩的成因长期存在争议,其中关于地幔的作用是关键问题之一[54]。许多学者提出了不同的模型来解释A型花岗岩的地球化学组成,这些模型影响着我们对壳幔相互作用、大陆生长、陆壳成熟以及相关成矿作用的理解。其中,对于过碱性A型花岗岩,地幔被认为是重要的源区,不仅为花岗岩的形成提供了热量,也提供了物质来源[104]。然而,关于铝质A型花岗岩的成因与地壳源区和熔融条件的关系仍存在争议[105]。地幔对这些A型岩石形成的贡献被认为仅限于其作为热源的作用。但是,本文研究表明二叠纪小海子准铝质A型花岗岩是由幔源碱性岩浆结晶分异形成的,表明地幔是铝质A型花岗岩的主要来源。类似的结论同样在中亚造山带和华南地块的铝质A型花岗岩中提出[106]。如果这一结论正确的话,那么铝质A型花岗岩的侵位也可能指示了地幔物质对地壳的加入,即地壳生长。值得指出的是,塔里木大火成岩省中占主体的为“壳源”长英质岩石,结合出现含水矿物斑晶水硅铁石和角闪石,说明大量约290 Ma的长英质岩石是由于镁铁质岩浆导致富水地壳发生部分熔融的结果[13]。这种地壳生长方式的变化可能与岩浆供给速率的变化相关。约290 Ma,在地幔柱热传导作用下塔里木岩石圈地幔中的富集组分发生大规模熔融,大量来自富集岩石地幔的玄武质岩浆喷发,同时部分侵位到地壳通过对流加热引发富水地壳熔融[54],最终形成广泛分布于塔里木克拉通内部的溢流玄武岩和“壳源”流纹岩。此时岩浆供给速率较低仅支持形成浅部岩浆房[102]。随后280~270 Ma在塔里木厚的岩石圈阻挡下,地幔柱发生扁平化侧向流动到岩石圈薄弱带时,由于岩石圈较薄,因此地幔柱有可能发生减压熔融[25]。高的岩浆供给速率有利于地幔柱来源的岩浆在深部聚集和迁移[107],并逐渐演化为碱性玄武质岩浆和赋含钒钛磁铁矿矿床镁铁-超镁铁质堆晶岩。碱性玄武质岩浆的连续封闭体系分离结晶作用产生了“幔源”长英质岩石,例如小海子碱性正长岩体。

7 结论

(1)锆石U-Pb年代学研究表明,小海子角闪正长岩的形成时代为(283.3±2.1) Ma,与橄榄辉石岩在时空上紧密伴生。

(2)小海子碱性正长岩体主要由铁橄榄石正长岩、角闪正长岩、石英正长岩和正长斑岩构成,属于准铝质A型花岗岩系列。在微量元素地球化学特征上,该岩体显示出与洋岛玄武岩相似的化学组成,表现为大离子亲石元素、轻稀土元素及高场强元素的富集特征。Sr-Nd同位素组成变化范围局限[(87Sr/86Sr)i=0.703 27~0.704 23,εNd(t)=-2.70~3.98],具FOZO型地幔特征。地球化学数据和Sr-Nd同位素表明碱性正长岩和橄榄辉石岩为同源成因。

(3)在280~270 Ma,塔里木地幔柱来源的岩浆侵位到地壳深部岩浆房中,并在此演化为碱性玄武质岩浆和镁铁-超镁铁质堆晶岩。碱性玄武质岩浆的连续封闭体系分离结晶作用形成了小海子碱性正长岩体。

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基金资助

东华理工大学战略性矿产成矿理论与深部预测江西省重点实验室开放基金(SZKFJJ202601)

国家自然科学基金(42562008)

国家自然科学基金(42063005)

中国铀业有限公司-东华理工大学核资源与环境国家重点实验室联合创新基金(2023NRE-LH-09)

江西省自然科学基金面上项目(20232BAB203067)

2024年东华理工大学核地学部“揭榜挂帅”项目(2024HDX06)

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