(1 中国地质科学院矿产资源研究所 国土资源部成矿作用与资源评价重点实验室, 北京 100037; 2 中国地质大学地球科学 与资源学院, 地质过程与矿产资源国家重点 实验室, 北京100083; 3 江西省地质矿产勘查开发局902地质大队, 江西 新余33800 0)
第一作者简介刘成林, 男, 1963年生, 研究员, 主要从事沉积矿床研究工作。 Email : liuchengl@263.net
收稿日期:2016-08-16;
改回日期:2016-09-16
本文得到 国家重点基础研究发展计划“973”项目(编号:2011CB403007)和中国地质科学院基本科研 业务费项目(编号:YYWF201607)资助
me chanism of subterranean brines rich in potassium and lithium
in South China Bl ock
(1 MLR Key Laboratory of Metallogeny and Mineral Assessment,Institute of Miner al Resources, Chinese Academy of Geological Sciences, Beijing 100037, China; 2 State Key Laboratory of Geological Processes and Mineral Resources, School o f Earth Sciences and Resources, China University of Geosciences (Beijing), Bei jing 100083, China; 3 No.902 Geological Team , Geology and Mineral Ex ploration and Development Bureau, Xinyu 338000, Jiangxi, China)
图 1华南大地构造特征及盆地分布图(据马永生等,2009改编)
①—郯庐断裂; ②—房城-襄广断裂带; ③—江南中生代北界隐伏断裂; ④—绍兴-江 山-萍乡断裂带; ⑤—丽水-海丰断裂带
Fig. 4Tectonic features and basin distribution in South China (after Ma et al. , 2009)
①—Tanlu fault; ②—Fangcheng-Xiangguang fault zone; ③—Jiangnan Mesozoic n o rthern buried fault; ④—Shaoxing-Jiangshan-Pingxiang
fault zone; ⑤—Lish ui-Haifeng fault zone
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据孙涛(2006),早中生代(印支期)花岗岩主要分布于桂东南大容山—六万大山—旧州、 台马一带,以含堇青石为特点,同时更大范围地分布在赣南、粤北、闽西等地,以含白云母 、不含堇青石为特点,它们以强过铝质为主,占印支期花岗岩的72.7%;晚中 生代花岗岩在华南花岗岩中出露面积最大,燕山早期以粤、闽、湘、赣为主要分布区域,主 体呈NE向分布,在南岭地区呈EW向分布;与印支期花岗岩相比,燕山早期花岗岩准铝和弱过 铝质钙碱性岩性的比例增加,面积上强过铝花岗岩已不再占有优势;燕山晚期花岗岩的出露 面积超过50 300 km2,此时岩浆活动主要以准铝质和弱过铝质钙碱性为主。
强烈的燕山期构造岩浆活动是在华南板块转入板内机制的背景上发生的。据Chen等(2002) 研究,呈EW向展布的燕山早期花岗岩(即南岭花岗岩)属于典型的后造山花岗岩组合(钾长 花岗岩、二长花岗岩组合),且伴有双峰式火山岩与A型花岗岩,属于与伸展构造有 关的火成岩组合。这种EW向构造岩浆组合,属于与印支运动有联系的后造山花岗岩。燕山晚 期花岗岩(年龄低于140 Ma)广泛分布于东南沿海地区,且经常伴有同时代、同物质来源的 火山岩,构成所谓的花岗质火山侵入杂岩带(Li,2000)。这种花岗岩与火山岩相伴生的现 象,一直可以追索到江西赣江一线(周新民等,2000)。燕山晚期花岗岩和火山岩的形成, 与太平洋板块向欧亚板块的俯冲有直接关系(王德滋,2004)。
图 2华南地区花岗岩分布图(据孙涛,2006)
1—燕山期花岗岩; 2—印支期花岗岩; 3—海西期花岗岩; 4—加里东期花岗岩; 5—前 寒武纪花岗岩; 6—省界
Fig. 2The distribution of granites in South China (after Sun, 2006)
1—Yanshanian granite; 2—Indosinian granite; 3—Hercynian granite; 4—Caledo nian granite; 5—Precambrian granite; 6—Provincial boundariy
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表 1华南地区中生代—新生代盆地内及周缘玄武岩及花岗岩化学组成
Table 1Cchemical composition of basalt and granite in Mesozoic-Cenozoic basin and the periphery in South China
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白垩纪全球平均海平面处于较高水平,其比现今海洋平均海平面高约75~250 m(Haq,2014 ) 。同时,整个白垩纪时期全球海平面处于快速波动状态(Haq et al.,1987;1988;Miller et al.,2004;2008),并可能在土仑期达到最大,当时海平面可能比现今地球高240~25 0 m。晚白垩世海侵被认为是自奥陶纪以来最大规模的海侵事件(Hancock et al.,1979)。 这次海侵事件波及范围巨大,当时约23%的大陆都 受到了这次海侵的影响,而剩下的陆表面积仅仅占 地球表面积的18%(现今陆表面积占地球表面积的28%)(Matsumoto,1977)。这 一时期,整个北美约有35%~38%的陆地被海水淹没,而在欧亚大陆被海水淹没的面积达到了 41%~42%(Hallam,1977)。
马永生等(2009)编制了中国东部晚白垩世—古近纪岩相古地理图(图4),显示扬子地区 在该时期曾发生过海侵,但古环境的重建问题目前仍存在一定争论,争论的焦点集中在这一 时期中国东部是否发生过海侵。自20世纪70年代在江汉盆地、三水盆地、渤海湾盆地等古近 系陆续发现有孔虫(林景星,1979),从而提出中国东部晚白垩世—古近纪发生过海侵的观点 或推论。目前,中国东部晚白垩世-古近纪海侵事件的研究多集中于松辽盆地及其相邻盆地 (侯读杰等,1999;黄永建等,2015;Sha et al.,2008)、渤海湾盆地(袁文芳等,2005 ),而对以江汉盆地、洞庭盆地以及吉泰盆地等组成的裂谷盆地群的研究仍涉及较少。地 层中是否存在生活于海相环境中的生物化石是判别海侵的一个重要标志(侯佑堂等 ,1982)。
图 3白垩纪—古近纪气候变化记录(实线引自Zachos et al.,2001;虚线引自Keller,2 008)
Fig. 3Climate change record in Cretaceous-Paleogene (solid line sources after Zachos et al.,2001; dotted line sources
after Keller,2008)
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同时,袁文芳等(2005)报道了东营凹陷沙河街组四段发现的管状藻礁灰岩,其中产有与海 相密切相关的各类海相生物化石,为盆地这一时期的海侵事件提供了有利的证据。牟晓慧等 (2007)认为岐口凹陷沙河街组一段广泛发育的“纹层状钙质泥岩”和“油页岩”中有相当 部分是由泥岩和颗石灰岩互层构成,而颗石灰岩是由外海进入渤海湾盆地的颗石藻勃发堆积 形成,反映了海侵作用的存在。此外,何镜宇等(1982)、葛瑞全(2003;2004)、傅强等 (2007)、吴贤涛等(2004)通过对中国东部盆地白垩系—古近系中海绿石、方沸石以及磷 灰石的发现,认为这些盆地在晚白垩世—古近纪遭受了不同程度海侵的影响。Feng等(2009 )在松辽盆地上白垩统的油页岩研究中,发现其分子化石表现出Pr/Ph比值低(<0.9)、伽 马蜡烷含量高且变化较大、4-甲基甾烷丰富、甾烷中C27/C29和C28/C 29的比值大于泥岩、正烷烃碳同位素轻、高碳数烷烃中C43、C45和C 47异常丰富等特征,进而推断油页岩形成于还原环境,藻类丰富多样,可能与海侵作用 有关。
图 4中国东部晚白垩世—古近纪岩相古地理图(据马永生等,2009)
Fig. 4Late Cretaceous-Paleogene lithofacies paleogeographic map in eastern Ch ina (after Ma et al., 2009)
①—商丹加里东期板块结合带; ②—郯庐断裂; ③—房城-襄广断裂带; ④—绍兴-江 山-萍乡加里东期-晋宁期板块结合带;
⑤—四会-吴川断裂带; ⑥—丽水-海丰断裂 带
1—一级单元界线; 2—二级单元界线; 3—三级单元界线; 4—大断裂带; 5—裂陷盆地 ; 6—潜隆起区; 7—古隆起区; 8—陆缘浅海;
9—火山沉积盆地; 10—褶皱带
①—Shang dan Caledonian plate junction; ②—Tanlu fault; ③—Fangcheng-xiang guang fault zone; ④—Shaoxing-Jiangshan-Pingxiang
Caledonian-Jinningian p late junction; ⑤—Sihui-Wuchuan fault zone; ⑥—Lishui-Haifeng fault zone
1—Primary unit boundary; 2—Secondary unit boundary; 3—Three-level unit bo undary; 4—Large fault zone; 5—Rift basin;
6—Latent uplift zone; 7—Anci ent uplift zone; 8—Epicontinental seas; 9—Volcanic-sedimentary basin; 10 —Fold belt
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储集层特征江陵凹陷储卤层主要有3种类型,分别为砂岩孔隙型、泥岩裂隙型和 玄武岩孔 洞型。砂岩主要为石英砂岩,长石英砂岩和岩屑石英砂岩,砂岩一般为细-中砂状结构,碎 屑颗粒平均含量为78%,充填物平均含量22%。孔隙度11.4%,渗透率4.5×10-3 μm 2,属低孔低渗类型。泥岩裂隙主要是断裂带中的细小断裂及节理,储集性和连通性好, 但发育规模 不好控制。玄武岩中气孔含量与储层物性呈正比。火山岩气孔一般呈断续线状分布,气孔椭 圆形居多,长轴3~13 mm,短轴0.2~7.0 mm,气孔面积含量不均,密集处20%~30%不等 ,气孔一般不连通。
卤水化学组成江陵凹陷岗钾1井古新统卤水化学组成见表2,卤水皆为过饱和状态 ,矿化 度达到了334 g/L。C1-及Na+、C1-及Na+含量占据绝对多数,SO2-4含量极 低。w(KCl)为1.58%, 达到了工业品位的要求。
卤水微量元素种类多且含量高,主要为锂、锶、铷、溴、碘和硼等元素。沙市组卤水中 w(Br-)为200.23×10-6~230×10-6,高于上覆新沟嘴组地层水 w(Br-)平均值(94×10-6)的2.1~2.4倍;江陵凹陷各地层的地层水普 遍含碘,潜江组、新沟嘴组和沙市组地层平均w(I-)不均一,分别为几乎为零 、21×10-6和58×10-6。岗钾1井卤水锂w(Li+)为80×10-6 ;w(Sr2+)为230×10-6,w(Rb+)为60×10-6 ,w(Cs+)为25×10-6,w(Br+)为200.23×10-6, w(I-)为73×10-6,w(B)为900×10-6。
由表2可见,与四川三叠系海相地层深层卤水 相比,江陵凹陷古新统卤水与其有相同的地方, 埋藏深、温度较高、含盐度也高,并且卤水中的钾及 多种微量元素都达到了工业品位,它 们的成因可能有相似性。
岗钾1井卤水特征系数见表3,由该表可见,江
表 2江陵凹陷与四川盆地富钾卤水化学特征
Table 2Chemical composition of potassium-rich brines
in Jiangling depressio n and Qaidam Basin
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潜江组主要以碎屑岩、碳酸盐岩、蒸发岩及其过渡类的沉积建造为主。砂岩由于其渗流能力 好,是深层卤水最主要和有利用价值的赋存体。潜江组的 砂岩可划分为中砂岩、细砂岩、粉砂岩等几种岩性,从粉砂岩-细砂岩 -中砂岩储层物性由低到高。
表 3江陵凹陷古新世富钾卤水特征参数
Table 3Characteristic parameters of Paleocene potassium-rich
brines in Jian gling Depression
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潜江凹陷潜江组蒸发岩盐类矿物组合特征:钙芒硝、无水芒硝、无水钠镁矾、盐镁芒硝、钾 芒硝、石盐、钾石膏、杂卤石等(吴必豪等,1980),可以推断,原始湖水应为硫酸钠亚型 卤水,这与目前地层中占据主导的水化学类型较为吻。碳酸盐型卤水阴离子中 CO2-3和HCO-3占据主导,其当量浓度超过Ca、Mg之和,为典型的大气水的特 征。深部氯化钙型卤水具有富Ca、贫SO4、高矿化度及富含多种微量元素的特征,这一特 殊的水化学类型与深埋藏变质作用有关。
在吉泰盆地开展钾盐普查过程中发现有卤水矿点。据已实施的6个钻孔发现,盆内卤水矿床 走向北东,倾向南西,目前控制卤水延伸约2000 m。卤水赋存于白垩系周田组第三段的构造 破碎带中,卤水具承压性,最大水头高于孔口标高3 m;多孔抽水试验显示,涌水量稳定, 在孔深200~300 m段单井涌水量在220 m3/d以上,卤水中LiCl的含量为工业品位2倍,为 富锂卤水矿,同时还含有一定的钾、溴、碘、硼等 有益组分。在吉泰盆地四周发育有黄坳、吉水、遂川- 德兴三条深大断裂及数十条规模稍小的断 裂,这些具有较好的与深部及浅部沟通能力,深层卤 水受地层压力沿深大断裂向上运移,赋存于裂 隙、孔隙发育的断层带中。与江汉盆地卤水赋存特征类比,推测目前发现富锂卤水矿为次级 储卤区,主要储卤区可能在深部。
5深层卤水的起源与成因
表 4潜江凹陷潜江组典型卤水化学成分特征(据马黎春等,2015)
Table 4Chemical composition of typical brines in Qianjiang Formation of Qianji ang depression (after Ma et al.,2015)
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死海盆地位于约旦-以色列裂谷,裂谷南北长达1100 km, 宽5~20 km,是一个典型的剪张 性 裂谷,上新世至今的死海群,沉积了一套巨厚的碎屑岩-蒸发岩系。区内东北部 有 较大面积新近纪玄武岩等基性火山岩出露,裂谷盆地自北向南都广泛分布有盐泉(钱自强等 ,1994)。死海海水就是富钾卤水,死海卤水化学具有高钙、高溴特征,金含量是海水的 1000倍。死海盐类物质1/3来自约旦河,2/3来自高盐度泉水;3个泉水ρ(K+ ) 平均达15.9 9 g/L;计算氯化钾资源量40亿吨,调查资源量20亿吨(Bentor,1961;Zak et al.,1968 )。
20世纪60年代,在美国加利福尼亚州索尔顿海湖东南的科学钻探中,钻遇高温(270~370℃ )热卤,富含钾硼锂铷铯及重金属铁铅锌铜等元素(Thompson et al.,1988)(表5)。而 索尔顿卤水中主要重金属铜、锌、铁等则要高出一般盐湖卤水的数十甚至数百倍,索尔顿海 热卤水属于典型裂谷深部起源卤水。Helgeson(1968)认为,卤水是起源于科罗拉多河水的 沉积物同生水;而Craig(1969)根据氢、氧同位素研究,认为索尔顿海卤水起源于大气降 水,通过沉积物循环形成。
中国柴达木和四川盆地也产有富钾、锂、硼、铷、铯的卤水资源。柴达木盆地西部古近系和 新近系碎屑岩中赋存有大量富钾卤水(油田水),采样测试其 化学组成特征(表5),与柴达木盆地现代盐湖卤水 具有较大区别,其溴、碘、硼、锂和铯等微量元素要比盐湖卤水高数 倍至十倍以上,显然,地层深部卤水的
表 5索尔顿海与柴达木盆地深层卤水化学组成
(ρ(B)/10-6)
Table 5The chemical composition of deep brines in
Salton Sea and Qaidam Basi n (ρ(B)/10-6)
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盆地封存的卤水属于地层水(柯林斯,1974;Hanor,1994),区别于储存在盆地基底结晶 岩系中的卤水,如著名的加拿大地盾卤水(Frape et al.,1987)。大陆地区地下卤水中盐 分的主要来源包括:① 海侵的海水;② 海相沉积物风化释放的盐分;③ 大陆地表岩 石的 风化产物;④火山喷发物质和热水盐分(Mcarthur et al.,1989)。而水的主要来源包括 外源的大气降水和内源的盆地封存水体及地壳流体或幔源(Thompson,1992;Plank,1996 ;毛景文等,2001;2004a)。由此可知,沉积盆地中卤水的物质来源和演化包含 了一系列复杂作用(Cai et al.,2001)。
关于沉积盆地中卤水成因,国内外学者曾做了大量的研究:① 沉积盆地结晶基底中的卤 水(如B ottomley et al.,1994;1999;2003;Leybourne et al.,2007;Greene et al.,2008; Katz et al.,2011);② 地层水或盆地卤水(Sonnenfeld,1984;Matray et al.,1990 ;Fontes et al.,1993;黄思静等,1997;林耀庭等,1997;Cai et al.,1997;2001;K loppmann et al.,2001;Birkle et al.,2009;刘成林,2013);③ 表层水、现代盐湖 水、浅层地下水等水体(肖应凯等,1994;刘成林等,1999;王弭力等,1997;2001;韩凤 清,2001;Xiao et al.,2000;Winckler et al.,2001;Klein-BenDavid et al.,2004 ;樊启顺等,2007;谭红兵等,2007;2009)。沉积盆地中卤水的来源通常认为主要有2种 机制:其一,是表层水的蒸发作用产生的埋藏卤水或蒸发卤水(原生卤水);其二,是盐类 矿物的地下溶解和原生卤水的稀释(次生卤水)(Matray et al.,1990;Hardie,1991;H anor,1994;Kloppman et al.,2001;Birkle et al.,2009;刘成林等,2009;2013); 另外,深源卤水补给也是来源之一(曲懿华,1982;刘成林,2013)。
水-岩反应与深层卤水成因有密切联系。例如,加拿大地盾卤水,赋存于古老结晶岩的裂隙 内 ,有观点认为卤水是发生长期水-岩反应形成的(Fritz et al.,1982;1987;Frape et a l.,1 984),也有认为卤水是形成于蒸发浓缩的海水,向下渗透与岩石反应形成的(Bottomley e t al .,1999;2003)。在瑞典的Stripa地区,卤水赋存于花岗岩体的孔隙内,溶质来源于地下 水与围岩发生的水-岩反应(Nordstrom et al.,1989a;1989b)。在芬兰卤水位于海岸地 带,并且大约7000年以前就一直被海水所淹没,海水与其所赋存的结晶岩发生了水-岩反 应 (Lahermo et al.,1987)。在英格兰康沃尔地区,卤水赋存于花岗岩体内,溶质来源于地 下水与长石和黑云母发生的水-岩反应(Edmunds et al.,1984;1985)。在澳大利亚的Yi lgarn板块,含盐的地下水来源于海水,演化成多来源的成因,其中水-岩反应贡献了溶质 来 源(Mcarthur et al.,1989)。在欧洲西南部比利牛斯山逆冲带的东北,深部地下水与沉 积地层发生的高温水-岩反应导致了泉水的矿化(Khaska et al.,2015)。在东欧地台, 卤 水赋存与火成岩基底内,溶质来源于地下水与结晶岩的水-岩反应(Vovk,1987)。总之, 这些高盐度流体的成因一方面被解释为海相成因。另一方面,地下水向下渗透或一些深部高 温流体在上升冷却过程中均会发生水岩反应而形成卤水,这些都已被流体的化学成分和同位 素组成所证实。
从构造角度分析,华南中 生代—新生代盆地是由于构造格局的转折(挤压转变为拉张)导致 岩石圈发生大规模的减薄而形成的。在拉张的动力学背景下,壳幔相互作用及大规模的岩浆 活动,在裂谷盆地中发育大量的火成岩。例如美国的索尔顿盐湖、中东的死海盆地以及中国 西藏和青海的第四纪盐湖等,并在卤水中富集锂、硼、铷、铯等元素,而这些元素的来源与 盆地内的火山活动有密切的关系。可见,华南中 生代-新生代盆地卤水锂、硼、铷、铯元 素的富集与本地区玄武岩喷发和花岗岩侵入活动有关。
从古地理、古气候方面分析,白垩纪—古近纪时期,北半球欧亚大陆中部地区中亚、蒙古、 中国逐渐形成一个近东西向、狭长的干旱气候带。湖北江汉盆地及江西的吉泰盆地处于这一 干旱带内,在盆地内沉积了大套的蒸发岩并赋存富钾卤水。同时,古孢粉学及沉积学研究表 明,晚白垩世—古近纪时期,研究区整体处于干旱气候格局。白垩纪全球平均海平面处于较 高水平,整个白垩纪时期全球海平面处于快速波动状态,晚白垩世海侵被认为是自奥陶纪以 来最大规模的海侵事件。而中国东部晚白垩世—古近纪是否发生过海侵,一直是长期存在的 争论。前人在生物化石、古遗迹、矿物岩石学、生物标志化合物和地球化学指标方面均找到 了海侵的证据。江西吉泰盆地T7X钻孔岩芯石盐溴含量与江陵凹陷沙钾3井石盐溴含量相近( 平均91×10-6),与海水蒸发析出石盐溴含量(110×10-6~330×10-6 )相当,可以推断这些盆地的溴来源具有海水起源特征。
根据上述构造、物源与干旱气候特征,再现华南地区裂谷盆地的液态型钾锂资源富集成矿过 程(图5;图6)。其成矿过程可分解为“2个阶段”以及“3个成钾作用过程”。“2个阶段 ”包括:第一阶段,地表盐湖—太阳能作用阶段;第二阶段,埋藏-岩浆热能作用。 “3个成钾作用过程”包括:第一是蒸发沉积;第二是沉积淋滤;第三是变质-改造。
图 5裂谷盆地成钾模式图(刘成林,2013)
1—石盐; 2—钾盐; 3—砂砾岩; 4—粉砂; 5—玄武岩; 6—深循环卤水(起源于卤水 —矿物反应); 7—地层建造水被驱动上涌;
8—岩浆分异热液流体; 9—地表盐泉(来 自深循环水、建造水的上升排泄); 10—冲洪积物
Fig. 5Schematic diagram shows that how potash salts formed in rift basin (after Liu, 2013)
1—Halite; 2—Potash salt; 3—Sandy conglomerates; 4—Siltstones; 5—Basal ts; 6—Deep cycle brine (originating from
brine-minerals reaction); 7—Upwe lling formation water derived by magma; 8—Magmatic differentiation hydrotherma l fluids;
9—Surface salt springs (derived from discharge of the deep cycle w ater and formation water); 10—Alluvial deposits
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对于尚未蒸发浓缩演化至钾盐矿物析出的盐湖富钾卤水,在沉积晚期及埋藏时期,沉积环境 从地表太阳能驱动转为岩浆热能驱动。盐湖卤水转入同沉积期或更深部地层的盐类晶间及碎 屑孔隙-裂隙中;随着埋藏加深,物理化学条件变为还原条件。岩浆流体侵入,继续带来成 矿物质,岩浆热能加速卤水-矿物反应,卤水中硫酸根绝大部分被还原,同时镁离子进 入方解石或文石形成白云石,卤水化学类型转变为氯化钙型。随着地层压力增加,富钾卤水 转移至孔隙及裂隙发育的岩层中储藏(图6);如果断裂切穿储卤层,一部分热卤又可以盐 泉的形式补给盐湖,开始新的地球化学循环。裂谷发展后期,古盐湖开始淡化,出现巨厚的 石膏和碳酸盐岩及碎屑岩沉积,形成卤水盖层。
总之,华南陆块(地区)富、钾、锂、硼、铷、铯、 溴、碘卤水是多源补给、内生与外生地质作用耦合的
图 6裂谷盆地富钾卤水形成过程示意图(刘成林,2013)
Fig. 6Schematic diagram showing the formation process of potassium-rich brine s in the rift basin (after Liu, 2013)
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由于岩石圈发生大规模的减薄导致壳幔相互作用及大规模的岩浆活动,在裂谷盆地中发育大 量的火成岩。华南陆块分布大量玄武岩和花岗岩,为钾锂等有益元素的富集提供了物质补给 。中国东部晚白垩世—古近纪的海侵,可为盆地带来丰富的钾、溴、碘等物质。
在白垩纪—古近纪干旱的气候环境下,华南中 生代—新生代盆地广泛出现蒸发作用,形成大量 蒸发岩。同时,对于古盐湖中尚未蒸发浓缩演化至钾盐矿物析出的盐湖富钾卤水,在沉积晚 期及埋藏时期,转入同沉积期或更深部地层的碎屑孔隙-裂隙中,同时,在岩浆热能的驱动 与流体补给下,钾、锂、硼、铷、铯可能还继续得到补充富集。
华南陆块的液体钾锂矿床可能是内生与外生地质共同作用,或构造-火成岩-海侵-干旱气 候 耦合成矿的结果。由此,推测华南地区中生代-新生代盆地可能具有钾、锂、硼、铷、铯、 溴、碘复合成矿的条件,并构成华南卤水型液体钾锂(及硼、铷、铯、溴、碘)成矿区。
志谢参加此项工作还有中国地质科学院矿产资源研究所张华博士,沈立建博士 ,胡宇飞 硕士,陈永志研究员,野外采样得到锦辉集团公司和江西省地矿局902大队领导干部的大力 支持,在此一并志谢!
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