Metallogenic features of diamondiferous kimberlites in Botswana and China:Enlightenment for exploration of the same type deposits
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摘要:
金刚石及其寄主岩石是人类认识地球深部物质组成和性质、壳幔和核幔物质循环重要研究对象。本文总结了中国不同金刚石类型的分布，着重对比了博茨瓦纳和中国含金刚石金伯利岩的地质特征，取得如下认识：（1）博茨瓦纳含矿原生岩石仅为金伯利岩，而中国含矿岩石成分复杂，金伯利岩主要出露在华北克拉通，展布于郯庐、华北中央和华北北缘金伯利岩带，具有工业价值的蒙阴和瓦房店矿床分布于郯庐金伯利岩带中；钾镁煌斑岩主要出露在华南克拉通，重点分布在江南和华南北缘钾镁煌斑岩带中；（2）钙钛矿原位U-Pb年龄和Sr、Nd同位素显示，86~97 Ma奥拉帕金伯利岩群和456~470 Ma蒙阴和瓦房店金伯利岩均具有低87Sr/86Sr（0.703~0.705）和中等εNd（t）（-0.09~+5）特征，指示金伯利岩浆源自弱亏损地幔或初始地幔源区；（3）博茨瓦纳金伯利岩体绝大多数以岩筒产出，而中国以脉状为主岩筒次之；博茨瓦纳岩筒绝大部分为火山口相，中国均为根部相，岩筒地表面积普遍小于前者；（4）奥拉帕A/K1和朱瓦能金伯利岩体是世界上为数不多的主要产出榴辉岩捕虏体和E型金刚石的岩筒之一，而同位于奥拉帕岩群的莱特拉卡内、丹姆沙和卡罗韦岩体与我国郯庐带的金伯利岩体类似，均主要产出地幔橄榄岩捕虏体以及P型和E型金刚石；（5）寻找含矿金伯利岩重点注意以下几点：克拉通内部和周缘深大断裂带是重要的控岩构造；镁铝榴石、镁钛铁矿、铬透辉石、铬尖晶石和铬金红石等是寻找含金刚石金伯利岩重要的指示矿物；航磁等地球物理测量需与土壤取样找矿方法相结合才能取得更好效果；（6）郯庐金伯利岩带、江南钾镁煌斑岩带和塔里木地块是中国重要含矿岩石的找矿靶区，冲积型金刚石成矿潜力巨大。
Abstract:Important implications for the interior workings, constituent, circulation between crust and mantle, convection between core and mantle of the Earth can be drawn by studying diamonds and their hosted rocks. Based on the geological comparison of metallogenic kimberlites from super-giant deposits in Botswana and Mengyin and Wafangdian deposits in China, the authors put forward some exploration suggestions and prospecting clues as follows:(1) Kimberlite is an unique diamondiferous rock in Botswana, whereas lamproite is a main hosted -rock in South China craton including two important lamproite zones along the Jiangnan orogenic belt and northern margin of South China craton. Kimberlite is dominantly distributed in the North China craton, which is composed of three kimberlitic zones along Tanlu fault, Trans-North China orogen and northern margin of North China. Two industrial value diamondiferous kimberlite deposits are distributed in the Tanlu zone. (2) In-situ U-Pb age and Sr, Nd isotopic data of perovskites show that 86-97 Ma Orapa kimberlites and 456-470 Ma Mengyin and Wafangdian kimberlites have low 87Sr/86Sr ratios of 0.703-0.705, medium εNd(t) values ranging from -0.09 to 5, indicating that primary kimberlitic magmas were likely derived from primitive mantle or convective lower mantle. (3) Primary kimberlites in Botswana dominantly occur as pipes, while in China they mainly occur as irregular fissures, expressed as dykes and lesser extent sills. Crater facies are pervasively observed in Orapa and Jwaneng kimberlite pipes in comparison with hypabyssal (or root zone) facies in Mengyin and Wafangdian pipe clusters. (4) Orapa A/K1 and Jwaneng mines are a few diamondiferous kimberlitic pipes yielding predominantly eclogitic xenoliths and E type diamond. In contrast, Letlhakane, Damtshaa and Karowe mines also occur in Orapa cluster, Mengyin and Wafangdian mines from the Tanlu kimberlite belt have mainly peridotite xenoliths as well as P type and E type diamonds. (5) Some exploration suggestions and prospecting clues of diamondiferous kimberlites are presented as follows:(A) Deep faults cutting through on-craton and off-craton subcontinental lithospheric mantle play a role in the emplacement of kimberlites; (B) Soil sampling for kimberlite indicator minerals such as picroilmenite and garnet, Cr-rich rutile, Cr-spinel and Cr-diopside is a primary exploration tool; (C) Geophysical surveys such as aeromagnetic mothed should be combined with soil sampling for better prospecting results. (6) Work in diamondiferous prospecting target areas in the Tanlu kimberlite zone, Jiangnan lamproite zone and Tarim block should be further strengthened. Illuvial type diamond deposits in China have great potential for mineralization.
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Keywords:
- kimberlite /
- diamond /
- prospecting indicator /
- Botswana /
- China
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1. 引言
三塘湖组(P1s)是广泛分布于新疆东准噶尔东北缘(三塘湖、克孜勒塔格、小青居羚山、库普及苏都库都克一带)的一套中酸性火山岩及其碎屑岩组合的陆相火山岩地层。下部为火山碎屑沉积岩与酸性喷出岩及中酸性火山碎屑岩不均匀互层；上部为中酸性喷出岩及火山碎屑岩夹火山碎屑-正常碎屑沉积岩，局部少量玄武岩；沉积夹层中产早二叠纪植物化石：Noeggerathiopsis cf. theodori Tschilova et Zalessky, Noeggerathiopsis cf. subangusta Zalessky(Sun, 1995)。
对这套陆相火山岩的研究最早始于1966年，1: 20万库普幅(L-46-XXV)将其划为中石炭世巴塔玛依内山组❶；1:20万奥什克山幅(L-46-XIX)将其自下而上划分为巴塔玛依内山组与苏都库都克组❷；1976年1:20万卡姆斯特幅(L-45-XXIV)亦将其划分为巴塔玛依内山组与苏都库都克组❸。随后，1979年1:20万克孜勒塔格幅(L-46-XXXV)❹与琼河坝幅(L-46-XXXVI)❺将其划分为上石炭统哈尔加乌组；1980年1:20万乌通苏依泉幅(L-46- XXVI)区调中将其划为中—上石炭统哈尔加乌组(C1-2h)❻；1:20万三塘湖幅(L-46-XXXIV)将这套地层在石头梅与条山地区分别划分为卡拉岗组(P1k)与哈尔加乌组❼；1985年新疆维吾尔自治区1: 200万地质图说明书将东、西准噶尔地区这套陆相火山岩自下而上统一定名为哈尔加乌组与卡拉岗组。但在1991年新疆维吾尔自治区地质矿产勘查开发局通过岩石地层清理则认为哈尔加乌组与卡拉岗组在三塘湖地区为同一层位，没有上下关系，时代为早二叠世；1995年孙巧缡在清理新疆岩石地层时建议将分布在新疆东准噶尔地区的这套陆相中酸性火山岩及其碎屑岩地层重新创名，由于三塘湖地区该套地层出露较好，建议用“三塘湖组”代表这套早二叠世地层；2000年新疆维吾尔自治区地质调查院认为这一建议较为切合实际，故沿用三塘湖一名代表这一套陆相火山岩❽。2015—2018年江西省地质矿产勘查开发局赣西北大队通过本次《新疆东准噶尔地区1:5万L46E019007、L46E019008、L46E020008三幅区域地质矿产调查项目》认为奥依托浪格地区原三塘湖组应划归为巴塔玛依内山组(C1-2bt)❾。
2. 地质背景及样品采集
新疆准噶尔盆地东北缘的三塘湖地区位于西伯利亚板块与哈萨克—准噶尔板块的结合部位，夹持在阿曼太—扎河坝与卡拉麦里巨型缝合带之间，因其特殊的大地构造位置而成为研究中亚造山带(CAOB)构造演化的热点区域之一(Li et al., 2012)。晚古生代是三塘湖地区经历洋陆转换的关键时期(Zhou et al., 2006)，大地构造背景争议的时间段集中在早石炭世至早二叠世，这一时期以海相沉积结束，发育典型的陆相火山岩为特征。争论的焦点主要可概括为以下两点：观点一(Zhao et al., 2008; Chen et al., 2009; Wu et al., 2009; Yang et al., 2010; Mao et al., 2010)认为三塘湖地区晚古生代陆相火山岩形成于碰撞造山期后陆内伸展背景；观点二(Long et al., 2006; Zhao et al., 2006; Zhao et al., 2006; Li et al., 2010)则认为三塘湖地区陆相火山岩形成于与俯冲作用相关的岛弧环境。新疆东准噶尔地区构造背景复杂，形成这种争议的关键性因素即在于北疆岩石地层划分的混乱性，在三塘湖地区建组的这套二叠纪中酸性陆相火山岩是否在整个三塘湖盆地具有普适性还有待商榷，其内是否包含了石炭纪陆相火山岩而面临解体需要进一步的工作证实。基础地质问题的解决对正确划分岩石地层单元、厘清陆相火山岩的时空演化序列、解释晚古生代的构造演化具有重要的地质意义。
研究区位于天山兴蒙造山系(一级)准噶尔弧盆系(二级)，跨北准噶尔晚古生代沟弧带与唐巴勒—卡拉麦里古生代复合沟弧带两个三级构造单元，包括洪古勒楞—阿尔曼太早古生代沟弧带、谢米斯台—库兰卡兹干古生代复合沟弧带、三塘湖晚古生代弧间盆地3个四级构造单元。奥依托浪格地区原三塘湖组陆相火山岩位于三塘湖晚古生代弧间盆地构造单元中，陆相火山岩共收集年龄样品3件，其中2件为锆石样品(RZ29-1、RZ48-1)，岩性为含橄榄石玄武岩，岩石呈深灰色，斑状-间粒间隐结构，块状构造。斑晶主要由斜长石(15%)组成，极少量橄榄石，斜长石粒度0.02~1 mm，呈自形板状，具强泥化，橄榄石呈自形柱状、粒状，具强暗化，并具蛇纹石化，从斑晶到基质粒度有过渡变化。基质主要由微板条状斜长石组成，斜长石杂乱分布，斜长石蚀变同斑晶，在斜长石之间分布微粒状辉石、玻璃质及少量磁铁矿，辉石较新鲜。磁铁矿呈微晶粒状嵌布在玻璃质中，玻璃质显光性，颜色较淡。在岩石中分布少量微细不规则杏仁体，杏仁体由沸石组成。1件为化石样品(D0811HS-1)，岩性为含炭质粉砂岩，层状片理发育，化石主要见于层面上。采样位置如图 1所示。
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图 1 研究区大地构造位置及地质图I−2—查尔斯克−乔下哈拉缝合带；I−3—准噶尔弧盆系；I−4—准噶尔地块−吐哈地块；I−3−1—北准噶尔晚古生代沟弧带；I−3−1b—洪古勒楞—阿尔曼太早古生代沟弧带；I−3−2b—谢米斯台—库兰卡兹干古生代复合沟弧带；I−3−2c—三塘湖晚古生代弧间盆地；I−3−2d—唐古巴勒—卡拉麦里古生代复合沟弧带；Qheol—风成堆积物；Qhch—化学沉积；Qhal—冲积堆积；Qhpl—洪积堆积；Qp3X—新疆群；J2t—头屯河组；J2x—西山窑组；J1s—三工河组；T2-3k—克拉玛依组；P3hl—黄梁沟组；C1-2bt—巴塔玛依内山组；C1j—姜巴斯套组；D3C1j—江孜尔库都克组；D3kx—卡希翁组；D3ka—克安库都克组；D2w—乌鲁苏巴斯套组Figure 1. Geotectonic location and geological map of the study areaI−2−Chaersike−Qiaoxiahala suture; I−3−Junggar arc basin; I−4−Junggar block−Tuha block; I−3−1−Late Paleozoic groove arc belt in North Junggar; I−3−1b−Hongguleleng−Aermantai early Paleozoic groove arc; I−3−2b−Xiemisitai−Kulankazigan Paleozoic composite groove arc; I−3−2c−Late Paleozoic inter-arc basin in Santanghu; I−3−2d−Tanggubale−Kalamaili Paleozoic composite groove arc; Qheol− Aeolian deposit; Qhch−Chemical deposit; Qhal−Alluvial deposit; Qhpl−Flood deposit; Qp3X−Xinjiang Group; J2t−Toutunhe Formation; J2x−Xishanyao Formation; J1s−Sangonghe Formation; T2−3k−Kelamayi Formation; P3hl−Huanglianggou Formation; C1−2bt−Batamayineishan Formation; C1j−Jiangbasitao Formation; D3C1j− Jiangzierkuduke Formation; D3kx−Kaxiweng Formation; D3ka−Keankuduke Formation; D2w−Wulusubasitao Formation3. 锆石U-Pb年代学特征
重砂样采集由新疆维吾尔自治区矿产实验研究所完成，锆石制靶与阴极发光分析在北京离子探针中心完成，将样品破碎至约100 μm，先用磁法和重液分选，然后在双目显微镜下手工挑选。将代表性的锆石颗粒黏在直径25 mm环氧树胶上，然后磨光至一半，抛光并镀金。锆石的阴极发光图像研究利用FEI PHILIPS XL30型扫描电镜，实验条件为15 kV，120μA.U，Th和Pb同位素组成分析在SHRIMPⅡ上进行。测定的206Pb/238U比值用标准锆石SL13(572 Ma)和澳大利亚的TEM(417 Ma)进行校正。每测定一次标准样品，测定3~4个锆石待测点。普通Pb校正采用204Pb直接测定法，加权平均年龄计算采用Isoplot软件，其置信度为20，置信水平95%，测试数据见表 1。
表 1 RZ29-1、RZ48-1锆石SHRIMP U−Pb年龄测试结果Table 1. RZ29-1 and RZ48-1 zircon SHRIMP U−Pb age test results
图 2是RZ29-1含橄榄石玄武岩锆石的阴极发光图，锆石大多呈短柱状，部分为不规则椭圆状，锆石发育发光强度不同的晶域，其中发光较弱的晶域锆石岩浆环带不可见，呈“墨棒状”，而发光较强的晶域则环带发育，以不规整椭圆状为多。对含橄榄石玄武岩进行了15个点位测试(表 1)，其中10个年龄分布在305~335 Ma，3个年龄在402~419 Ma，2个年龄异常为277.7 Ma与481 Ma；通过观察锆石形态与打孔位置，10个300 Ma左右的年龄均为环带不发育与发育较好的锆石；3个400 Ma年龄的锆石可能为捕获的较老的基底锆石，2个年龄异常值可见打点均未位于锆石的边部，包含了边部与核部两部分。剔除这5个锆石(1、5、9、10、12)不稳定值，剩余10个年龄较稳定的锆石具有线性的Th/U值，说明锆石是从成分相对均匀的岩浆中结晶出来的。因此测定的206Pb/238U年龄加权平均值可以代表陆相火山岩中锆石的结晶年龄，即火山岩的成岩年龄。图 3中是RZ48-1含橄榄石玄武岩部分锆石的阴极发光图，部分锆石岩浆环带不发育，对该样品打点8个，大多数年龄分布在300~362 Ma，通过观察锆石形态与打孔位置，7个330 Ma左右的年龄均为环带不发育与发育较好的锆石，这7个年龄较稳定的锆石具有线性的Th/U值。
在谐和图上，所有数据均位于谐和线附近，最终测定的锆石U-Pb加权平均年龄为(320.5±7.1) Ma，MSWD=3.2(图 4)，处于二分的上下石炭统界线附近，说明该火山岩形成于晚石炭世早期。RZ48-1测定的锆石U-Pb年龄为(335.6±6.5)Ma，MSWD= 1.9(图 5)，为早石炭世晚期。
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图 4 RZ29-1年龄直方图(a)与谐和图(b)Figure 4. RZ29-1 age histogram (a) and concordant diagram (b)![]()
图 5 RZ48-1年龄直方图(a)与谐和图(b)Figure 5. RZ48-1 age histogram (a) and concordant diagram (b)4. 三塘湖组解体讨论
4.1 三塘湖组的重新厘定与解体
在三塘湖地区，三塘湖组原为巴塔玛依内山组、苏都库都克组(或哈尔加乌组与卡拉岗组)的统称，代表三塘湖地区一套二叠系陆相中酸性火山岩系地层(Li et al., 2016)，通过地质剖面与1: 5万路线调查，基本查明奥依托浪格地区陆相火山岩为一套基性火山岩及碎屑岩组合，仅发育少量中酸性火山岩，与三塘湖组中酸性火山岩为主有较大差异(图 6)。
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图 6 奥依托浪格幅巴塔玛依内山组实测地质剖面缩略图1—砾岩；2—泥质粉砂岩；3—玄武岩；4—安山岩；5—英安岩；6—流纹质英安岩；7—珍珠岩；8—凝灰岩；9—闪长岩；10—粗面岩；11—火山角砾岩；12—碎石亚黏土Figure 6. Measured geological section map of the Batamayineishan Formation in Aoyituolangge geological map1-Conglomerate; 2-Argillaceous siltstone; 3-Basalt; 4-Andesite; 5-Dacite; 6-Dellenite; 7-Pearlite; 8-Tuff; 9-Diorite; 10-Trachyte; 11-Volcanic breccia; 12-Detritus subclay巴塔玛依内山组与其他石炭系不同，陆相火山岩广泛发育，是东准噶尔地区东北缘火山岩产出的主要层位。该组最早是由1:20万库普幅(L-46- XXV)区域地质矿产调查时建立，建组地点位于卡拉麦里蛇绿岩带的巴塔玛依内山南麓，主要表现为一套酸性、中基性陆相火山-湖相沉积体系。溢流相火山岩依岩性可分为玄武岩、安山岩、英安岩、流纹岩和珍珠岩等，具明显的多期次、间歇性喷发的特征(Zhang et al., 2014)。本文中测制巴塔玛依内山组地质剖面如图 6所示：地层厚度大于2248 m，总体呈现北倾的单斜构造，局部褶皱构造发育；岩性组合中以溢流相玄武岩为主，同时少量发育安山岩、玄武安山岩、粗面岩、英安岩、流纹英安岩和珍珠岩等；爆发相为各类型凝灰岩、火山角砾岩、玄武质角砾岩等；喷发间歇期可见泥质粉砂岩、细砂岩、岩屑砂岩、砾岩等沉积相系。通过剖面的岩相学研究，将本区巴塔玛依内山组依据正常沉积岩组分为3个喷发间歇期，火山作用岩组分为4个喷发旋回，以及13个喷发韵律❾，显示了本区巴塔玛依内山组同样具有多期次、间歇性喷发的特征，同区域上具有一致性。
准噶尔盆地陆东—五彩湾及北三台地区的钻孔资料显示，巴塔玛依内山组总体表现为上下两套火山岩中间夹一套碎屑岩，可分为三段：下段以溢流相中酸性火山岩与爆发相火山碎屑岩为主，上段以溢流相中基性火山岩夹爆发相火山碎屑岩为主，中段碎屑岩为火山喷发间歇期的正常沉积，局部地区夹煤层或煤线，含有丰富的植物和孢粉化石，植物化石为典型安加拉植物群，孢粉以高含量的单气囊的Noeggerathio psidozonotriletes为主要特征(Lü et al., 2013)。本文将巴塔玛依内山组分为上下两段，岩相演化序列清晰，段与段之间呈明显的岩相递变关系：下段(C1-2bt1)主要为爆发相(凝灰岩、火山角砾岩、集块岩)与喷发沉积相(砂岩、凝灰质砂岩)不均匀互层，其中东南角喷发沉积相极其发育，可见大型交错层理，成层性、褶皱形态清晰，细碎屑岩段见煤线发育，并有植物化石产出，但收集的样品经鉴定为蕨类植物的部分茎干，无时代意义；上段(C1-2bt2)主要为溢流相(基性玄武岩、少量中酸性安山岩、英安岩)夹爆发相(凝灰岩、火山角砾岩)，极少量沉积岩夹层中亦可见煤线与植物化石。本文所分上下段分别可与陆东—五彩湾及北三台地区的巴塔玛依内山组中上段(碎屑相-喷出相)相对应(图 7)。
巴塔玛依内山组上段中采集的植物化石(D0811HS-1)经南京古生物研究所鉴定，植物化石种类为次狭科达(匙叶)(近似种)Noeggerathiopsis cf. subangusta Zalessky，属安加拉区系植物，给出的时代为二叠纪，与库普幅(L-46-XXV)最早定名为中石炭统巴塔玛依内山组内所发现的早二叠世化石一致，充分说明这类植物化石的穿时性。有报道指出，新疆北部的安加拉区系植物最早出现在早石炭世晚期，繁盛于二叠纪(Dou et al., 1985)，这就解释了石炭纪地层中出现了二叠纪化石的合理性：即次狭科达(匙叶)也可以出现在石炭纪中晚期，为中晚石炭世与二叠纪早期的共同分子。
关于巴塔玛依内山组的年代学研究，从晚泥盆世晚期(364.0±13)Ma(Luo et al., 2012)到早二叠世晚期(275.0±6.8)Ma(Zhang et al., 2009)均有文章报道，时间跨度大，究其原因还是因为北疆这套陆相火山岩地层时代划分的混乱性。即使是石炭纪内部，巴塔玛依内山组同样存在早石炭世与晚石炭世的争议。通过本次巴塔玛依内山组年代学数据的统计学研究发现，绝大多数年龄数据分布在石炭纪内，仅1个数据与5个数据(其中4个数据属同一文章报道)分别位于晚泥盆世晚期与早二叠世晚期(未列表)，不具有代表性。石炭纪共收集年龄数据为18个，如表 2所示，其中早石炭世数据为6个，晚石炭世数据为12个，说明在区域上巴塔玛依内山组在晚石炭世比较发育。而本次工作分别对巴塔玛依内山组上下两段分别进行了SHRIMP锆石U-Pb定年，获得其下段年龄为(335.6±6.5)Ma、上段年龄为(320.5±7.1)Ma，说明巴塔玛依内山组下上段分别形成于早石炭世晚期与晚石炭世，具有穿时性，对解决巴塔玛依内山组下上石炭统之争具有重大的年代学意义。
表 2 巴塔玛依内山组年代学数据Table 2. Chronologic data of Batamayineishan Formation
前人研究表明北疆东准噶尔东北缘这套陆相火山由于上下关系不明很难进行解体，但本文认为这套陆相火山岩自西向东具有由早石炭世向早二叠世过渡演化的特征，可根据地质时代对石炭纪与二叠纪地质体进行区分，而本区的石炭纪陆相火山岩地层明显与区域上巴塔玛依内山组具有可对比性，故认为应将原三塘湖组解体为下—上石炭统巴塔玛依内山组与下二叠统(新)三塘湖组，三塘湖组仅代表二叠纪陆相火山岩。
4.2 石油地质意义
新疆北部东准噶尔东北缘这套陆相火山岩由于地层时代划分的混乱性，对其构造背景的争议主要体现在岛弧环境和板内拉张环境两方面，纵观东准噶尔晚古生代的演化历史，通常认为其为自西向东呈拉链式逐渐拼接的过程。在奥依托浪格地区，早石炭世早期仍存在卡拉麦里大洋向北俯冲作用下的残余洋盆沉积——姜巴斯套组(C1j)，姜巴斯套组上部产大量海生动物化石(图 8)，化石层厚近30 m，说明海洋生物活动范围逐渐变窄而汇聚至最终死亡，暗示残余洋盆受俯冲拼接作用而逐渐萎缩，直至早石炭世晚期奥依托浪格以西拼接最终完成(奥依托浪格以东三塘湖方向可能仍然存在俯冲作用)，开启陆相火山演化阶段。
笔者对奥依托浪格石炭纪火山岩进行了地球化学研究，研究显示巴塔玛依内山组火山熔岩以橄榄玄武岩为主，岩石类型显示自西向东呈钙碱-碱性变化趋势，姜巴斯套组火山岩则为拉斑玄武岩系，从岩系上可以看出两个方向上的演化：由南向北与俯冲作用方向一致的拉斑-钙碱序列，显示残余洋盆向岛弧演化；由西向东与链式拼合方向一致的钙碱-碱性序列，显示岛弧向陆内(弧后)拉张演化。微量与稀土元素显示石炭纪火山岩富集大离子亲石元素(LILE)与轻稀土元素(LREE)，亏损高场强元素(HFSE)与重稀土元素(HREE)，总体具有岛弧火山岩的特征；但从其岩石组合特征及其微量元素特征指标来看，又与传统的岛弧火山岩具有明显差异，兼具岛弧环境与板内拉张环境的地球化学性质❾。由此本文认为，新疆东准噶尔东北缘这套陆相火山岩地球化学性质的奇特之处，就在于其俯冲作用下的自西向东链式拼接过程，这套陆相火山岩自西向东由石炭纪向二叠纪演化，以奥依托浪格为例，在早石炭晚期，这套陆相火山岩开始演化之时，其西侧已经拼接完成，进入陆内伸展阶段，而其东侧则可能还在继续受到俯冲作用，为岛弧环境，故其地球化学特征同时显示岛弧环境与板内拉张，其构造部位应与弧后盆地相当。
近年来，东准噶尔陆东—五彩湾地区油气勘探发现石炭系巴塔玛依内山组火山岩有不同程度的油气显示，发现了五彩湾气田与卡拉麦里千亿立方米天然气大气田，使得东准噶尔地区巴塔玛依内组越来越受到重视。巴塔玛依内山组与上覆地层克拉玛依组(T2-3k)呈角度不整合关系，说明在石炭纪末期这套陆相火山岩经历过构造抬升，而火山岩的风化壳为油气的优质储层(Zhang et al., 2015)，同时本区存在至少3次火山间歇期，其间可见植物化石与煤线，其下段大套喷发沉积相说明其具有形成烃源岩的必要地质条件；另外构造上，巴塔玛依内山组整体呈背斜式，而下段喷发沉积相呈复式背向斜褶皱形态，为极好的油气藏储集体。同时火山机构发育，大量的环形、线性构造为油气的运移富集提供了空间。综上所述，奥依托浪格地区陆相火山岩虽然缺少类似东准噶尔陆东—五彩湾地区的下石炭统滴水泉组沉积地层作为烃源岩层的外部条件，但其自身内部具有形成“自生自储”油气藏的潜力，具有一定的石油地质意义。
5. 结论
(1)本文通过岩性、岩相组合对比与化石、SHRIMP锆石U-Pb年代学研究，认为奥依托浪格地区原三塘湖组(P1s)应重新厘定为巴塔玛依内山组(C1-2bt)。而原三塘湖组应根据时代解体为下—上石炭统巴塔玛依内山组与下二叠统(新)三塘湖组，三塘湖组仅代表二叠纪陆相火山岩。
(2)通过巴塔玛依内山组下上段火山岩SHRIMP锆石U-Pb年代学研究认为巴塔玛依内山组时代具有穿时性，为早石炭世到晚石炭世，对解决巴塔玛依内山组下上石炭统之争具有重大的年代学意义。
(3)北疆东准噶尔东北缘这套陆相火山岩不具备可分性的原因可能与东准噶尔构造带自西向东链式拼接而造成陆相火山岩自西向东由早石炭世向早二叠世连续演化有关。大地构造背景争议的两个焦点：陆内拉张伸展环境与俯冲带之上岛弧环境可能也与这种自西向东拼接方式有关，即该陆相火山岩同时受到东侧岛弧环境与西侧拉张环境的影响。该拼接模式对解释东准噶尔东北缘晚古生代构造演化争议具有重要的理论意义。
(4)本区石炭纪巴塔玛依内山组陆相火山岩构造发育：构造抬升、环形与线性构造、复式背向斜等。同时火山间歇期发育，为奥依托浪格地区巴塔玛依内山组形成“自生自储”油气藏提供了必要的地质条件，具有一定的石油地质意义。
致谢：本文得到江西省地质矿产勘查开发局赣西北大队邹国庆、孙国庆、左全狮高级工程师以及曹钟清、李旭辉教授级高工的指导与帮助；审稿专家对本文提出了宝贵的修改意见，在此一并表示感谢。
注释
❶新疆地质局区测大队. 1966.库普幅(L46-XXV)1:20万区域地质调查报告.
❷新疆地质局. 1966.奥什克山幅(L-46-XIX)1:20万地质图说明书.
❸新疆地质局区域地质调查大队. 1976.卡姆斯特幅(L-45- XXIV)1:20万区域地质调查报告.
❹新疆地质局区域地质调查大队. 1979.克孜勒塔格幅(L- 46-XXXV)1:20万区域地质调查报告.
❺新疆地质局区域地质调查大队. 1979.琼河坝幅(L-46- XXXVI)1:20万区域地质调查报告.
❻新疆地质局区域地质调查大队. 1980.乌通苏依泉幅(L- 46-XXVI)1:20万地质图说明书.
❼新疆地质局区域地质调查大队. 1980.三塘湖幅(L- 46-XXXIV)1:20万地质图说明书.
❽新疆地质调查院. 2000.纸房幅(L46C004002)1:25万区域地质调查报告.
❾江西省地质矿产勘查开发局赣西北大队. 2018.新疆东准噶尔地区1:5万L46E019007、L46E019008、L46E020008三幅区域地质调查报告.
致谢: 论文撰写过程中许志琴院士予以指导，牛晓露副研究员和冯光英副研究员给予华北克拉通和东北陆块构造演化方面的建议，中国地质大学(武汉)吴魏伟博士在金刚石成因方面给予帮助，李观龙和卢雨潇帮助查找材料，两位评审专家提出了宝贵的建议，在此一并表示诚挚地感谢。 -
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图 1 博茨瓦纳12个金伯利岩群在行政区图和构造地质简图中的分布（据Brook, 2017修改）
Figure 1. Administrative and geological maps of Botswana depicting locations of 12 kimberlite clusters
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图 2 奥拉帕金伯利岩群中金刚石矿的分布图(Kruger et al., 2017)
Figure 2. Positions of the diamondiferous mines in the Orapa kimberlite cluster
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图 3 奥拉帕A/K1金刚石矿的3D模型及其野外地质特征
a—A/K1的露头采坑；b—A/K1的3D模型显示由两个金伯利岩筒组成（缩写见正文）；c—北筒NPK−普遍可见花岗岩和玄武岩岩屑，岩屑粒径多小于1cm，橄榄石晶屑普遍蛇纹石化和方解石化；d—北筒MVK2−BBX，普遍可见棱角状玄武岩角砾；e—南筒黑色块状火山碎屑金伯利岩（SDVK），比重较大，含大量新鲜橄榄石和少量玄武岩捕虏体；f—南筒南部火山碎屑金伯利岩（SVK）上层，可见大量岩屑和橄榄石斑晶，偶见单斜辉石和钛铁矿
Figure 3. Field photos and a 3D view of the A/K1 kimberlite in which the lithologic units are shown in the text in details
a-Orapa A/K1 open pit containing North and South pipes; b-3D model of the A/K1 kimberlitic pipes; c-Northern Proclastic Kimberlite (NPK) in North pipe showing pervasively granite and basalt debris with size less than 1 cm. Olivine is commonly altered by serpentinization and calcitization; d-Massive Volcaniclastic Kimberlite (MVK)− Basalt breccia xenolith (BBX) in North pipe; e-Southern Dark Volcaniclastic Kimberlite (SDVK) including an amount of olivines in the South Pipe; f-Basalt breccia, olivine, rare clinopyroxene and ilmenite are commonly observed in the upper unit of the Southern Volcaniclastic kimberlite (SVK)
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图 4 丹姆沙B/K9矿点岩筒地质简图(据Buse et al., 2011修改)
Figure 4. Schematic geological map illustrating the features of the Damtshaa B/K9(modified from Buse et al., 2011)
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图 5 卡罗韦A/K6金刚石矿床岩筒模型和野外地质特征
a—卡罗韦A/K6南、中、北岩筒模型剖面图（南筒模拟深度约300 m(Chinn et al., 2010)）；b—AK6的3个金伯利岩矿筒中产出50~100克拉金刚石的分布图；c—AK6露头采坑；d—采坑的玄武质围岩；e—南筒的玻基斑状火山碎屑金伯利岩（VK）和块状初始岩浆金伯利岩（MPK）
Figure 5. Geological model and field photographs of diamondiferous kimberlite features in the Karowe mine
a-Geological section of A/K6 mine showing the features of north, central and south lobes; b-Distribution map of diamonds with 50 to 100 carats from north, central and south lobes; c-Open pin of the Karowe (A/K6); d-Country rock of basalt from south lobe; e-Fragmental kimberlite (FK) sample from the central lobe and magmatic/pyroclastic kimberlite (MPK) sample from the south lobe
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图 6 朱瓦能DK2矿区的4个金伯利岩管分布图及野外特征
a—DK2露头采坑；b—DK2采坑平面地质简图(de Wit et al, 2016)；c—南筒火山碎屑金伯利岩和玄武岩围岩露头
Figure 6. Jwaneng D/K2 pit composed of north, central, south and forth lobes (a); Schematic geological map showing the DK2 features (b); Photographs of the volcanoclastic kimberlite and wall rock basalt from the south lobe (c)
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图 7 中国金伯利岩和钾镁煌斑岩分布简图（板块边界和主断裂带据Zheng et al., 2013；许文良等, 2013）
1—山东蒙阴；2—辽宁瓦房店（旧称复县）；3—辽宁桓仁；4—辽宁葫芦岛；5—辽宁铁岭；6—吉林集安；7—吉林通化钾镁煌斑岩；8—河南鹤壁；9—河北涉县；10—山西大同饮牛沟钾镁煌斑岩；11—山西大同采凉山；12—山西应县；13—山西柳林；14—内蒙古四子王旗；15—湖北大洪山彭家垮金伯利岩；16—湖北大洪山王关−徐家冲钾镁煌斑岩；17—湖南宁乡；18—广西融水；19—广西都安；20—广西大化；21—贵州镇远；22—贵州施秉；23—贵州麻江；24—扬子陆块西缘钾质煌斑岩；25—浙江龙游；26—江西安远；27—新疆巴楚；28—新疆皮山
Figure 7. Schematic map of kimberlites and lamproites distribution in China
1-Mengyin, Shandong; 2-Wafangdian (formerly known as Fuxian), Liaoning; 3-Huanren, Liaoning; 4-Huludao, Liaoning; 5-Tieling, Liaoning; 6-Ji'an, Jilin; 7-Potassium-magnesium lamprophyre in Tonghua, Jilin; 8-Hebi, Henan; 9-Shexian, Hebei; 10-Yinniugou potassiummagnesium lamprophyre in Datong, Shanxi; 11-Cailiangshan, in Datong, Shanxi; 12-Yingxian, Shanxi; 13-Liulin, Shanxi; 14-Siziwang Banner, Inner Mongolia 15-Pengjia collapse kimberlite in Dahongshan, Hubei; 16-Wangguan-Xujiachong K-Mg lamprophyre in Dahongshan, Hubei; 17-Ningxiang, Hunan; 18-Guangxi meltwater; 19-Du'an, Guangxi; 20-Dahua, Guangxi; 21-Zhenyuan, Guizhou; 22-Shibing, Guizhou; 23-Majiang, Guizhou; 24-K-lamprophyre on the western margin of Yangtze block; 25-Longyou, Zhejiang; 26-Anyuan, Jiangxi; 27-Bachu, Xinjiang 28-Pishan, Xinjiang
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图 8 山东蒙阴金伯利岩地质简图（据宋瑞祥, 2013修改）
F1—蒙山断裂；F2—新泰—垛庄断裂；F3—铜冶店—蔡庄断裂；F4—上五井断裂；F5—鄌郚−葛沟断裂；F6—沂水−汤头断裂；F7—安丘—莒县断裂；F8—昌邑—大店断裂
Figure 8. Geological map of Mengyin kimberlites showing the locations of three mines of Changmazhuang, Xiyu and Poli and main faults(modified from Song, 2013)
F1−Mengshan fault; F2−Xintai-Duozhuang fault; F3−TongyedianCaizhuang fault; F4−Shangwujing fault; F5−Zanzenggou fault; F6−Yishui−Tangtou fault; F7−Anqiu−Juxian fault; F8−Changyi−Dadian fault
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图 9 辽宁省含金刚石金伯利岩和主要断裂构造分布图（据赵光慧等, 2011；宋瑞祥, 2013修改）
Figure 9. Distribution map of diamondiferous kimberlites and major faults in Liaoning Province (modified from Zhao et al., 2011; Song, 2013)
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图 10 辽宁瓦房店金伯利岩群构造地质简图（据(宋瑞祥, 2013；赵春强等, 2018)修改）
Figure 10. Sketch geological map of Wafangdian kimberlite cluster in Liaoning Province including five kimberlite zones (modified from Zhao et al., 2011; Song, 2013; Zhao et al., 2018)
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