沂沭断裂带构造演化与金矿成矿作用研究
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摘要
论文针对沂沭断裂带的研究现状和金矿勘查取得的成果,应用大陆动力学研究方法与成矿理论,采用野外调查与资料研究相结合、重点金矿区解剖与重要样品测试相结合的方法,从解析构造研究的基础入手,对沂沭断裂带的控矿规律进行了探讨,对成矿物质来源和成矿作用提出了新的认识。
沂沭断裂带是由四条主干断裂组成的具“二堑夹一垒”构造样式的组合型断裂。航磁△T异常图显示为一系列北北东-北东向线状和串珠状异常带,在布格重力异常图上表现为北北东走向的重力梯度带。带内结晶基底的构造线方向与带两侧基底岩系具完全不同的构造特征,并控制着地层的展布和岩浆岩的发育程度。
通过详细的构造剖面研究,沂沭断裂带活动方式于不同时期不同区段表现出明显的多样性,造成兼具韧性与脆性、挤压与引张、左旋与右旋等性质复杂的构造变形特征。结合地球物理探测资料,沂沭断裂带既具有深大断裂的切幔特征,又表现为浅层次的铲式断裂,在经历了漫长而多期的构造运动后,使之构造形态变得极为复杂。
沂沭断裂带形成始于新元古代,当时具有古沂沭裂谷的性质,晋宁运动使古沂沭裂谷闭合,形成鲁东、鲁西统一的古陆。断裂带两侧地壳产生差异运动,鲁东地区长期隆起,以剥蚀为主,仅局部有些海相沉积。海西-印支期运动之后,原东西向构造线改变为北东向、北北东向的构造型式。中生代时期,中国东部开始了由中亚-特提斯构造域向滨太平洋构造域转化阶段,中生代是我国滨太平洋构造体系强烈活动阶段,致使中国东部发生地幔置换作用与中生代岩石圈减薄。同时华北板块与扬子板块夹持下的秦-祁-昆洋盆消亡碰撞造山,使沂沭断裂带发生强烈的构造活化并发生大规模的左行平移,以及其后的推覆、右行平移及张裂作用。在这一大的构造背景下,沂沭断裂对该地区的构造格局、沉积作用、岩浆活动以及矿产的形成与分布等产生了重要影响。由于太平洋板块不断俯冲,沂沭断裂带处在大陆活动边缘裂谷中。上地幔深熔岩浆不断由该带涌出,为成矿送来矿源和热源。而在它的东侧由于板块热作用,地壳物质重熔形成大量的多期次的花岗质岩石,成为胶东金矿成矿的重要母体。’沂沭断裂带在古近纪时以左行平移为主伴有张裂,后期演化成裂谷；新近纪为左行平移,伴有强烈的火山活动。第四纪则表现为差异性升降运动。
沂沭断裂带强烈活动的大陆动力学环境起源于中亚—特提斯构造域向滨太平洋构造域转化、太平洋板块的俯冲。在三大板块即华北板块与扬子板块碰撞造山、太平洋板块向NWW俯冲的大背景下,导致了沂沭断裂带的活化并发生左行平移,其最大平移距离超过300Km。新生代则以拉张、挤压(兼扭动)交替进行为特征,形成具裂谷特征的构造格架。
沂沭断裂带内金矿按成因可分为岩浆期后热液破碎带蚀变岩型、岩浆期后热液裂隙充填石英脉型、接触交代矽卡岩型、潜火山热液爆发角砾岩型和沉积型五种类型。蚀变岩型金矿主要分布于沂水-汤头断裂带内,矿(化)体多赋存于糜棱岩化花岗岩、花岗质碎裂岩和绿泥片岩中,矿与非矿界线不清,矿体的圈定由样品分析结果确定,矿体形态多受断裂构造及韧性剪切带控制。石英脉型金矿产于基底岩系或中生代岩体内的断裂裂隙中,矿体与围岩界线清晰,矿体为含金黄铁矿化石英脉。接触交代型金矿床成矿的母岩为中生代燕山期多阶段侵入的复杂岩体,为中偏基性或中偏酸性-酸性偏碱性组分的岩浆岩,成矿围岩主要为寒武-奥陶纪灰岩,矿体产在燕山期岩浆岩与碳酸盐岩的接触带内,矿体形态复杂多变,主要为似层状和透镜状,其次有扁豆状、囊状等。潜火山热液型金矿床分布于胶莱盆地与沂沭断裂带的交汇处,矿体主要产于青山群次火山岩、火山岩中,少量产于侵入岩中,矿化围岩为石英闪长玢岩-花岗闪长斑岩、闪长岩、闪长玢岩、安山凝灰质角砾岩、安山岩等,矿体产出于隐爆角砾岩筒中,与次火山杂岩体关系密切,次火山杂岩体是重要的导矿、容矿地质体。铜、铅锌矿主要为中低温热液裂隙充填型,多分布于区域性深大断裂旁侧次级断裂构造中,形成于燕山晚期；蓝宝石矿产于沂沭断裂带内,多位于新近纪玄武质岩浆喷发中心部位。从成矿时序上,不同成因的矿床产出的构造部位、地质环境及成矿时间不同,总体上由老到新表现为金、铜、铅锌和蓝宝石的成矿序列。
不同时期的构造-岩浆作用形成了不同的矿床类型,燕山期是区内重要的金矿成矿期,它形成了山东独具特色的金矿类型和成矿系列。按照成矿作用特征,可划分为3个矿床成矿系列组合和15个矿床成矿系列。
沂沭断裂带内金矿床主要产于沂水-汤头断裂主裂面下盘的糜棱岩化碎裂岩和花岗质碎裂岩中。主要地质体中以泰山岩群与燕山期花岗岩金含量为高,其标准离差和变异系数较大,是区内金矿主要的成矿母岩,尤其是燕山期岩浆活动,是导致区内金矿成矿的重要因素。黄铁矿化、硅化、绢英岩化与金矿关系密切。载金矿物主要为黄铁矿和脉石英,其中早期黄铁矿为金矿物的主载矿物。金有自然金、银金矿两种,以角粒状为主,次长角粒状、树枝状、枝叉状及线状等,.金矿物的成色平均为816。
通过对蚀变岩型和石英脉型金矿中方解石、石英包裹体的研究表明：包裹体有单一液相包裹体、气液两相包裹体和富气相包裹体3种类型。其冰点温度变化于-2～-8.6℃之间,盐度在3.39wt%～12.39wt%之间,即中等盐度的岩浆流体(或深源流体)和低盐度的深循环的大气水流体；方解石中流体的盐度相对较低,推测为岩浆流体与大气水混合的结果。包裹体均一温度变化范围较宽,在107℃～550℃之间,可分为125℃～160℃、177℃～230℃和260℃～330℃三个温度峰值集中区,分别反映了早期以中温石英为代表的早期成矿阶段(260℃～330℃),以中低温石英和方解石为代表的中期成矿阶段(177℃～260℃)和以低温方解石为代表的晚期成矿阶段(125℃～160℃)。
对区内典型金矿床硫、氢、氧、碳和铅等稳定同位素的研究资料表明：黄铁矿的δ34S值的变化为+2.7～+4.4‰,δ180H20值为-1.78～4.07‰,δD(SMOW)值为-74～77‰,δ13C平均值为-4.18～-5.1‰,铅同位素具有正常铅的特点,说明区内金矿的成矿物质来源于地下深处,成矿流体以岩浆水为主,大气降水为辅。
蚀变矿物石英和长石的稀土元素特征具有一些相似的特点,二者均为向右倾斜的平滑曲线,属轻稀土元素富集型。但二者的差别也是明显的,长石中稀土元素的总量高,轻稀土元素富集更为明显,且表现为Eu的负异常；石英的稀土总量低,轻稀土元素富集不够明显,且表现为Eu的正异常。
对南小尧金矿矿石中的锆石进行U-Pb同位素年龄测定,上交点2438±13Ma基本代表了岩体的形成年龄,下交点116±20Ma可能代表了区域成矿的大致时限。对龙泉站金矿、南小尧金矿和牛家小河金矿石中的钾长石矿物进行K-Ar法测定,其年龄值分别为141.92±2.06 Ma、94.29±1.38 Ma、95.92±1.40 Ma,本区金矿的形成应在早白垩世中-晚期。沂南铜井地区测定的20件全岩及单矿物K-Ar测年数据,年龄值在110-126Ma间,另外有一组Rb-Sr等时线测年数据为113.4Ma。这些资料反映了金矿成矿时代应为白垩纪。
通过对区内金矿成矿规律进行了概略总结,认为基底富含金质的矿源岩、晋宁期强烈的韧性剪切作用、燕山期大规模的火山-岩浆热事件是导致区内金矿成矿的因素。根据地质基础资料和对成矿物质来源的研究,建立了区内金矿的成矿模式。
Pointing to present condition of research and achievements gained in gold exploration, by using continental dynamics research method and mineralization theory, combining field survey with information study, combing important gold mines anatomy with test samples, and on the basis of analyzing structure, ore controlling rule of Yishu fault belt is studied in this paper. New recognition of ore-forming materials and ore mineralization are put forward as well.
Yishu fault belt is composed of four main faults with the type of "two faulted troughs with one horst".△T aeromagnetic anomalies appear as a series of linear type anomaly belts with the trend of north-north-east to north-east and beaded anomaly belt. They showed as gravity gradient belts with the trend of north-north-east in Bouguer gravity anomaly map. The structural line directions of the crystalline basement have different characteristics with those on both sides of the basement rocks, and controlled the strata distribution and the development level of magmatic rocks.
Through detailed study on profiles of the structures, it is showed that activity styles of Yishu fault belt in different sections in different stages have obvious diversity. It caused complicated metamorphic characteristics of structures, such as toughness and brittle, squeeze and stretch, left rotating and right rotating. Combining with geophysical detection information, it is regarded that Yishu fault belt both has the cutting mantle characteristics of the deep fault, and spade fracture performance in shallow part. After experiencing long and multi-phase tectonic movements, its structures have become very complicated.
Yishu fault belt was formed in Neoproterozoic period with the property of ancient Yishu rift. The ancient Yishu rift was closed due to Jinning movement and formed unified ancient land in Ludong (eastern Shandong province) and Luxi (western Shandong province) areas. Crusts on both sides of the fault occurred differences in movements. Ludong area uplift in long time, and erosion was its major movement and deposition only occurred in partial areas. After the Hercynian and Indo-China movement, the former structure line changed from north-east trend to north-north-east trend. In Mesozoic period, eastern China started the change from central Asia and Tethys tectonic domain to the Pacific tectonic domain stage. The Mesozoic and Cenozoic periods were strong movement stages. They would cause the mantle replacement in eastern China and the lithosphere thinning in Mesozoic and Cenozoic period. At the same time, the Qin-Qi-Kunyang basin clamping between the north China plate and the Yangtze plate occurred collision and orogenic movement. It would cause strong activation of the Yishu fault belt and a large-scale shift to the left, the subsequent napping, translating to the right side and splitting. Under this structural background, structural pattern, sedimentation, magmatic activities and the form and distribution of minerals were effected by Yishu fault belt obviously. Due to subduction of the Pacific plate, Yishu fault belt located in marginal rift of continental movement. Magmatic lava in the upper part of the mantle pulped out from this area and provided sources and heat for mineralization. Due to thermal function of the plate in east part, a large number of multi-phase granite rock were formed after crust material remelting, which became important parent of gold mineralization in Jiaodong area. Yishu fault belt were translated to left accompanying with splitting in Paleogene, and evoluted to rift in later period. The movement in Neogene would translate at the left side with strong magmatic movement, while the movement in Quaternary showed differences in movements for the campaign.
The continental dynamics environment with strong activities in Yishu fault belt originated from the transformation of central Asia-Tethys tectonic domain to the foreshore Pacific tectonic domain, and the Pacific plate subduction. Under the background of north China plate and the Yangtze plate collision orogenic activity, and the subduction of Pacific plate to the NWW trend, the activation of Yishu fault belt and its translation to the left occurred. The largest translation distance was over 300km. The Cenozoic had the characteristics of extension and squeeze in turn, and the structural framework with rift characteristics was formed.
Gold deposits in Yishu fault belt can be divided into 5 types according to its origins; they are post-magmatic hydrothermal alteration with broken rock type, post-magmatic hydrothermal fracture filling quartz vein, contact skarn type, and the outbreak of crypto-volcanic hydrothermal breccia sedimentary rock type. Altered rock type gold deposits were mainly distributed in Yishui-Tangtao fault belt, and mineralization mainly occurs in mylonite granite, granite rock fragmental and green schist. The boundary between ore and non-ore was not very clear. The definition of ore bodies was determined by sample analysis result, and the ore body shapes were controlled by faults and ductile shear belts. Quartz vein type gold deposits occurred in basement rocks or Mesozoic rocks in the fault fissures. Ore bodies were gold-bearing pyritiferous quartz vein which had clear boundaries with country rocks. Parent rock of contact type gold deposit was the intruded complex in multi-stage Mesozoic Yanshan period. Its components were partial basis or partial acid to basis magmatic rocks. It was majorly composed of stratoid or phacoidal type, accompanying with lenticular and sackform type. Crypto-volcanic hydrothermal gold deposit located in the intersection part of Jiaolai basin and Yishu fault belt. Ore bodies mainly occurred in crypto-volcanic rocks and volcanic rocks of Qingshan group, while a small amount occurred in intrusive rocks. The mineralization rocks were quartz diorite porphyry-granite porphyry, diorite, diorite porphyry, Anshan tuffaceous breccia and andesite, etc. Ore bodies occurred in crypto-explosive breccia pipes which have close relation with volcanic complex. The crypto-volcanic complex was important ore leading and ore bearing geological bodies. Copper and lead-zinc deposits were mainly low-medium thermal fracture filling type, and were mainly distributed in sub-faults in both sides of regional deep faults. They were formed in late Yanshan period. Sapphire deposit occurred in Yishu fault belt. They were mainly occurred in central part of volcanic eruption of Neogene basalt. According to mineralization time, deposits caused by different origins occurred in different structural sections, different geological environment and different ore-forming times. The whole mineralization sequence was gold, copper, lead-zinc and sapphire from old to new.
Different types of deposits were formed by different tectonic and magmatic function in different stages. Yanshan period is an important gold mineralization period. It formed a unique gold mineralization and ore-forming series in Shandong province. According to the mineralization characteristics, it can be divided into three deposit forming series combinations and 15 deposit series.
Gold deposits in Yishu fault belt mainly occurred in mylonitic fragmental and granite rocks in lower part of main fracture in Yishui-Tangtao fault belt. Gold content in granite of major geological ore bodies is higher in Taishan group and Yanshan group. Its standard deviation and variation coefficient is large. They are major parent gold mineralization rocks, particularly the magmatic activities in Yanshan period are important factors for gold mineralization in this area. Pyritization, silication and beresite have close relation with gold deposit. Gold was composed of natural gold and silver gold. Gold ores were mainly showed as brecciform, accompanying with sub-brecciform, branched and line types, and the average component of gold mineral is 816.
Through study on calcite inclusions and quartz inclusions in altered rock type and quartz vein type gold deposits, it is showed that inclusions have three types, such as single liquid phase inclusion, gas-liquid phase inclusion and gas-rich inclusion. Its freezing temperature varies between-2℃～-8.6℃, the salinity is between 3.39 wt%～12.39wt%, that is medium degree salinity (or deep source fluid) and low degree salinity deep water circulation of the atmosphere fluid; salinity in calcite fluid is relatively low, which is estimated as the result mixing magmatic fluids and atmospheric water. Uniform temperature of inclusions has a wide variation range between 107℃～550℃, and can be divided into 3 peak temperatures as 125℃～160℃,177℃～230℃and 260℃～330℃. They respectively reflect the early mineralization stage which regarded quartz as the representative (260℃～330℃), medium mineralization stage which regarded low-temperature quartz and calcite as the representatives (177℃～260℃), and late mineralization stage which regarded low-temperature calcite as the representative (125℃～160℃).
As showed by stable isotope data of sulfur, hydrogen, oxygen, carbon and lead in typical gold deposits in this region,δ34 S value of pyrite varies between+2.7～+4.4‰,δ18O H2O value varies between-1.78～4.07‰,δD (SMOW) value varies between-74～-77‰, and the average value ofδ13 C is-4.18～-5.1‰. Isotope of lead has the characteristics of normal lead, which showed that gold-forming minerals are from deep part of underground. Ore-forming fluids are majorly composed of magma water accompanying with air precipitation.
Rare earth elements of altered quartz and feldspar have some similar characteristics. They both are smooth curves with right tilt, and belong to light rare earth element concentration type. However, the difference between the two is obvious, the total content of rare earth element in feldspar is the highest, and light rare earth element concentration is even more evident with negative performance of the Eu anomaly; total content of rare earth element in quartz is low, and light rare earth element concentration is not evident, and the performance of the Eu is abnormal.
U-Pb isotopic dating of zircon in Nanxiaoyao gold deposit is determined. The age of 2438±13Ma can represent the forming age of basic rocks, and 116±20Ma may represent a general time limit of regional mineralization. K-feldspar minerals in Longquanzhan gold deposit, Nanxiaoyao gold deposit and Niujiaxiaohe gold deposit are determined by using K-Ar method. Their ages are 141.92±2.06 Ma,94.29±1.38 Ma and 95.92±1.40 Ma respectively. The gold deposits in this area were formed in early and late Cretaceous period.20 whole-rock and single ore in Tongjing area of Yinan county are determined by using K-Ar dating method, the age is between 110～126 Ma. The age of other groups determined by Rb-Sr isochronal dating is 113.4 Ma. These data reflect that gold mineralization age should be in the Cretaceous period.
Through primary summary on gold mineralization rule in this area, it is regarded that the ore-rich source rocks, strong ductile shear function in Jinning group, and large scale of volcano-magma thermal incident are factors for causing gold mineralization in this region. According to geological data and study on ore-forming minerals, gold ore-forming model is set up in this area.
沂沭断裂带是由四条主干断裂组成的具“二堑夹一垒”构造样式的组合型断裂。航磁△T异常图显示为一系列北北东-北东向线状和串珠状异常带,在布格重力异常图上表现为北北东走向的重力梯度带。带内结晶基底的构造线方向与带两侧基底岩系具完全不同的构造特征,并控制着地层的展布和岩浆岩的发育程度。
通过详细的构造剖面研究,沂沭断裂带活动方式于不同时期不同区段表现出明显的多样性,造成兼具韧性与脆性、挤压与引张、左旋与右旋等性质复杂的构造变形特征。结合地球物理探测资料,沂沭断裂带既具有深大断裂的切幔特征,又表现为浅层次的铲式断裂,在经历了漫长而多期的构造运动后,使之构造形态变得极为复杂。
沂沭断裂带形成始于新元古代,当时具有古沂沭裂谷的性质,晋宁运动使古沂沭裂谷闭合,形成鲁东、鲁西统一的古陆。断裂带两侧地壳产生差异运动,鲁东地区长期隆起,以剥蚀为主,仅局部有些海相沉积。海西-印支期运动之后,原东西向构造线改变为北东向、北北东向的构造型式。中生代时期,中国东部开始了由中亚-特提斯构造域向滨太平洋构造域转化阶段,中生代是我国滨太平洋构造体系强烈活动阶段,致使中国东部发生地幔置换作用与中生代岩石圈减薄。同时华北板块与扬子板块夹持下的秦-祁-昆洋盆消亡碰撞造山,使沂沭断裂带发生强烈的构造活化并发生大规模的左行平移,以及其后的推覆、右行平移及张裂作用。在这一大的构造背景下,沂沭断裂对该地区的构造格局、沉积作用、岩浆活动以及矿产的形成与分布等产生了重要影响。由于太平洋板块不断俯冲,沂沭断裂带处在大陆活动边缘裂谷中。上地幔深熔岩浆不断由该带涌出,为成矿送来矿源和热源。而在它的东侧由于板块热作用,地壳物质重熔形成大量的多期次的花岗质岩石,成为胶东金矿成矿的重要母体。’沂沭断裂带在古近纪时以左行平移为主伴有张裂,后期演化成裂谷；新近纪为左行平移,伴有强烈的火山活动。第四纪则表现为差异性升降运动。
沂沭断裂带强烈活动的大陆动力学环境起源于中亚—特提斯构造域向滨太平洋构造域转化、太平洋板块的俯冲。在三大板块即华北板块与扬子板块碰撞造山、太平洋板块向NWW俯冲的大背景下,导致了沂沭断裂带的活化并发生左行平移,其最大平移距离超过300Km。新生代则以拉张、挤压(兼扭动)交替进行为特征,形成具裂谷特征的构造格架。
沂沭断裂带内金矿按成因可分为岩浆期后热液破碎带蚀变岩型、岩浆期后热液裂隙充填石英脉型、接触交代矽卡岩型、潜火山热液爆发角砾岩型和沉积型五种类型。蚀变岩型金矿主要分布于沂水-汤头断裂带内,矿(化)体多赋存于糜棱岩化花岗岩、花岗质碎裂岩和绿泥片岩中,矿与非矿界线不清,矿体的圈定由样品分析结果确定,矿体形态多受断裂构造及韧性剪切带控制。石英脉型金矿产于基底岩系或中生代岩体内的断裂裂隙中,矿体与围岩界线清晰,矿体为含金黄铁矿化石英脉。接触交代型金矿床成矿的母岩为中生代燕山期多阶段侵入的复杂岩体,为中偏基性或中偏酸性-酸性偏碱性组分的岩浆岩,成矿围岩主要为寒武-奥陶纪灰岩,矿体产在燕山期岩浆岩与碳酸盐岩的接触带内,矿体形态复杂多变,主要为似层状和透镜状,其次有扁豆状、囊状等。潜火山热液型金矿床分布于胶莱盆地与沂沭断裂带的交汇处,矿体主要产于青山群次火山岩、火山岩中,少量产于侵入岩中,矿化围岩为石英闪长玢岩-花岗闪长斑岩、闪长岩、闪长玢岩、安山凝灰质角砾岩、安山岩等,矿体产出于隐爆角砾岩筒中,与次火山杂岩体关系密切,次火山杂岩体是重要的导矿、容矿地质体。铜、铅锌矿主要为中低温热液裂隙充填型,多分布于区域性深大断裂旁侧次级断裂构造中,形成于燕山晚期；蓝宝石矿产于沂沭断裂带内,多位于新近纪玄武质岩浆喷发中心部位。从成矿时序上,不同成因的矿床产出的构造部位、地质环境及成矿时间不同,总体上由老到新表现为金、铜、铅锌和蓝宝石的成矿序列。
不同时期的构造-岩浆作用形成了不同的矿床类型,燕山期是区内重要的金矿成矿期,它形成了山东独具特色的金矿类型和成矿系列。按照成矿作用特征,可划分为3个矿床成矿系列组合和15个矿床成矿系列。
沂沭断裂带内金矿床主要产于沂水-汤头断裂主裂面下盘的糜棱岩化碎裂岩和花岗质碎裂岩中。主要地质体中以泰山岩群与燕山期花岗岩金含量为高,其标准离差和变异系数较大,是区内金矿主要的成矿母岩,尤其是燕山期岩浆活动,是导致区内金矿成矿的重要因素。黄铁矿化、硅化、绢英岩化与金矿关系密切。载金矿物主要为黄铁矿和脉石英,其中早期黄铁矿为金矿物的主载矿物。金有自然金、银金矿两种,以角粒状为主,次长角粒状、树枝状、枝叉状及线状等,.金矿物的成色平均为816。
通过对蚀变岩型和石英脉型金矿中方解石、石英包裹体的研究表明：包裹体有单一液相包裹体、气液两相包裹体和富气相包裹体3种类型。其冰点温度变化于-2～-8.6℃之间,盐度在3.39wt%～12.39wt%之间,即中等盐度的岩浆流体(或深源流体)和低盐度的深循环的大气水流体；方解石中流体的盐度相对较低,推测为岩浆流体与大气水混合的结果。包裹体均一温度变化范围较宽,在107℃～550℃之间,可分为125℃～160℃、177℃～230℃和260℃～330℃三个温度峰值集中区,分别反映了早期以中温石英为代表的早期成矿阶段(260℃～330℃),以中低温石英和方解石为代表的中期成矿阶段(177℃～260℃)和以低温方解石为代表的晚期成矿阶段(125℃～160℃)。
对区内典型金矿床硫、氢、氧、碳和铅等稳定同位素的研究资料表明：黄铁矿的δ34S值的变化为+2.7～+4.4‰,δ180H20值为-1.78～4.07‰,δD(SMOW)值为-74～77‰,δ13C平均值为-4.18～-5.1‰,铅同位素具有正常铅的特点,说明区内金矿的成矿物质来源于地下深处,成矿流体以岩浆水为主,大气降水为辅。
蚀变矿物石英和长石的稀土元素特征具有一些相似的特点,二者均为向右倾斜的平滑曲线,属轻稀土元素富集型。但二者的差别也是明显的,长石中稀土元素的总量高,轻稀土元素富集更为明显,且表现为Eu的负异常；石英的稀土总量低,轻稀土元素富集不够明显,且表现为Eu的正异常。
对南小尧金矿矿石中的锆石进行U-Pb同位素年龄测定,上交点2438±13Ma基本代表了岩体的形成年龄,下交点116±20Ma可能代表了区域成矿的大致时限。对龙泉站金矿、南小尧金矿和牛家小河金矿石中的钾长石矿物进行K-Ar法测定,其年龄值分别为141.92±2.06 Ma、94.29±1.38 Ma、95.92±1.40 Ma,本区金矿的形成应在早白垩世中-晚期。沂南铜井地区测定的20件全岩及单矿物K-Ar测年数据,年龄值在110-126Ma间,另外有一组Rb-Sr等时线测年数据为113.4Ma。这些资料反映了金矿成矿时代应为白垩纪。
通过对区内金矿成矿规律进行了概略总结,认为基底富含金质的矿源岩、晋宁期强烈的韧性剪切作用、燕山期大规模的火山-岩浆热事件是导致区内金矿成矿的因素。根据地质基础资料和对成矿物质来源的研究,建立了区内金矿的成矿模式。
Pointing to present condition of research and achievements gained in gold exploration, by using continental dynamics research method and mineralization theory, combining field survey with information study, combing important gold mines anatomy with test samples, and on the basis of analyzing structure, ore controlling rule of Yishu fault belt is studied in this paper. New recognition of ore-forming materials and ore mineralization are put forward as well.
Yishu fault belt is composed of four main faults with the type of "two faulted troughs with one horst".△T aeromagnetic anomalies appear as a series of linear type anomaly belts with the trend of north-north-east to north-east and beaded anomaly belt. They showed as gravity gradient belts with the trend of north-north-east in Bouguer gravity anomaly map. The structural line directions of the crystalline basement have different characteristics with those on both sides of the basement rocks, and controlled the strata distribution and the development level of magmatic rocks.
Through detailed study on profiles of the structures, it is showed that activity styles of Yishu fault belt in different sections in different stages have obvious diversity. It caused complicated metamorphic characteristics of structures, such as toughness and brittle, squeeze and stretch, left rotating and right rotating. Combining with geophysical detection information, it is regarded that Yishu fault belt both has the cutting mantle characteristics of the deep fault, and spade fracture performance in shallow part. After experiencing long and multi-phase tectonic movements, its structures have become very complicated.
Yishu fault belt was formed in Neoproterozoic period with the property of ancient Yishu rift. The ancient Yishu rift was closed due to Jinning movement and formed unified ancient land in Ludong (eastern Shandong province) and Luxi (western Shandong province) areas. Crusts on both sides of the fault occurred differences in movements. Ludong area uplift in long time, and erosion was its major movement and deposition only occurred in partial areas. After the Hercynian and Indo-China movement, the former structure line changed from north-east trend to north-north-east trend. In Mesozoic period, eastern China started the change from central Asia and Tethys tectonic domain to the Pacific tectonic domain stage. The Mesozoic and Cenozoic periods were strong movement stages. They would cause the mantle replacement in eastern China and the lithosphere thinning in Mesozoic and Cenozoic period. At the same time, the Qin-Qi-Kunyang basin clamping between the north China plate and the Yangtze plate occurred collision and orogenic movement. It would cause strong activation of the Yishu fault belt and a large-scale shift to the left, the subsequent napping, translating to the right side and splitting. Under this structural background, structural pattern, sedimentation, magmatic activities and the form and distribution of minerals were effected by Yishu fault belt obviously. Due to subduction of the Pacific plate, Yishu fault belt located in marginal rift of continental movement. Magmatic lava in the upper part of the mantle pulped out from this area and provided sources and heat for mineralization. Due to thermal function of the plate in east part, a large number of multi-phase granite rock were formed after crust material remelting, which became important parent of gold mineralization in Jiaodong area. Yishu fault belt were translated to left accompanying with splitting in Paleogene, and evoluted to rift in later period. The movement in Neogene would translate at the left side with strong magmatic movement, while the movement in Quaternary showed differences in movements for the campaign.
The continental dynamics environment with strong activities in Yishu fault belt originated from the transformation of central Asia-Tethys tectonic domain to the foreshore Pacific tectonic domain, and the Pacific plate subduction. Under the background of north China plate and the Yangtze plate collision orogenic activity, and the subduction of Pacific plate to the NWW trend, the activation of Yishu fault belt and its translation to the left occurred. The largest translation distance was over 300km. The Cenozoic had the characteristics of extension and squeeze in turn, and the structural framework with rift characteristics was formed.
Gold deposits in Yishu fault belt can be divided into 5 types according to its origins; they are post-magmatic hydrothermal alteration with broken rock type, post-magmatic hydrothermal fracture filling quartz vein, contact skarn type, and the outbreak of crypto-volcanic hydrothermal breccia sedimentary rock type. Altered rock type gold deposits were mainly distributed in Yishui-Tangtao fault belt, and mineralization mainly occurs in mylonite granite, granite rock fragmental and green schist. The boundary between ore and non-ore was not very clear. The definition of ore bodies was determined by sample analysis result, and the ore body shapes were controlled by faults and ductile shear belts. Quartz vein type gold deposits occurred in basement rocks or Mesozoic rocks in the fault fissures. Ore bodies were gold-bearing pyritiferous quartz vein which had clear boundaries with country rocks. Parent rock of contact type gold deposit was the intruded complex in multi-stage Mesozoic Yanshan period. Its components were partial basis or partial acid to basis magmatic rocks. It was majorly composed of stratoid or phacoidal type, accompanying with lenticular and sackform type. Crypto-volcanic hydrothermal gold deposit located in the intersection part of Jiaolai basin and Yishu fault belt. Ore bodies mainly occurred in crypto-volcanic rocks and volcanic rocks of Qingshan group, while a small amount occurred in intrusive rocks. The mineralization rocks were quartz diorite porphyry-granite porphyry, diorite, diorite porphyry, Anshan tuffaceous breccia and andesite, etc. Ore bodies occurred in crypto-explosive breccia pipes which have close relation with volcanic complex. The crypto-volcanic complex was important ore leading and ore bearing geological bodies. Copper and lead-zinc deposits were mainly low-medium thermal fracture filling type, and were mainly distributed in sub-faults in both sides of regional deep faults. They were formed in late Yanshan period. Sapphire deposit occurred in Yishu fault belt. They were mainly occurred in central part of volcanic eruption of Neogene basalt. According to mineralization time, deposits caused by different origins occurred in different structural sections, different geological environment and different ore-forming times. The whole mineralization sequence was gold, copper, lead-zinc and sapphire from old to new.
Different types of deposits were formed by different tectonic and magmatic function in different stages. Yanshan period is an important gold mineralization period. It formed a unique gold mineralization and ore-forming series in Shandong province. According to the mineralization characteristics, it can be divided into three deposit forming series combinations and 15 deposit series.
Gold deposits in Yishu fault belt mainly occurred in mylonitic fragmental and granite rocks in lower part of main fracture in Yishui-Tangtao fault belt. Gold content in granite of major geological ore bodies is higher in Taishan group and Yanshan group. Its standard deviation and variation coefficient is large. They are major parent gold mineralization rocks, particularly the magmatic activities in Yanshan period are important factors for gold mineralization in this area. Pyritization, silication and beresite have close relation with gold deposit. Gold was composed of natural gold and silver gold. Gold ores were mainly showed as brecciform, accompanying with sub-brecciform, branched and line types, and the average component of gold mineral is 816.
Through study on calcite inclusions and quartz inclusions in altered rock type and quartz vein type gold deposits, it is showed that inclusions have three types, such as single liquid phase inclusion, gas-liquid phase inclusion and gas-rich inclusion. Its freezing temperature varies between-2℃～-8.6℃, the salinity is between 3.39 wt%～12.39wt%, that is medium degree salinity (or deep source fluid) and low degree salinity deep water circulation of the atmosphere fluid; salinity in calcite fluid is relatively low, which is estimated as the result mixing magmatic fluids and atmospheric water. Uniform temperature of inclusions has a wide variation range between 107℃～550℃, and can be divided into 3 peak temperatures as 125℃～160℃,177℃～230℃and 260℃～330℃. They respectively reflect the early mineralization stage which regarded quartz as the representative (260℃～330℃), medium mineralization stage which regarded low-temperature quartz and calcite as the representatives (177℃～260℃), and late mineralization stage which regarded low-temperature calcite as the representative (125℃～160℃).
As showed by stable isotope data of sulfur, hydrogen, oxygen, carbon and lead in typical gold deposits in this region,δ34 S value of pyrite varies between+2.7～+4.4‰,δ18O H2O value varies between-1.78～4.07‰,δD (SMOW) value varies between-74～-77‰, and the average value ofδ13 C is-4.18～-5.1‰. Isotope of lead has the characteristics of normal lead, which showed that gold-forming minerals are from deep part of underground. Ore-forming fluids are majorly composed of magma water accompanying with air precipitation.
Rare earth elements of altered quartz and feldspar have some similar characteristics. They both are smooth curves with right tilt, and belong to light rare earth element concentration type. However, the difference between the two is obvious, the total content of rare earth element in feldspar is the highest, and light rare earth element concentration is even more evident with negative performance of the Eu anomaly; total content of rare earth element in quartz is low, and light rare earth element concentration is not evident, and the performance of the Eu is abnormal.
U-Pb isotopic dating of zircon in Nanxiaoyao gold deposit is determined. The age of 2438±13Ma can represent the forming age of basic rocks, and 116±20Ma may represent a general time limit of regional mineralization. K-feldspar minerals in Longquanzhan gold deposit, Nanxiaoyao gold deposit and Niujiaxiaohe gold deposit are determined by using K-Ar method. Their ages are 141.92±2.06 Ma,94.29±1.38 Ma and 95.92±1.40 Ma respectively. The gold deposits in this area were formed in early and late Cretaceous period.20 whole-rock and single ore in Tongjing area of Yinan county are determined by using K-Ar dating method, the age is between 110～126 Ma. The age of other groups determined by Rb-Sr isochronal dating is 113.4 Ma. These data reflect that gold mineralization age should be in the Cretaceous period.
Through primary summary on gold mineralization rule in this area, it is regarded that the ore-rich source rocks, strong ductile shear function in Jinning group, and large scale of volcano-magma thermal incident are factors for causing gold mineralization in this region. According to geological data and study on ore-forming minerals, gold ore-forming model is set up in this area.
引文
①山东省地质调查院.山东省沂南县龙泉站地区金矿普查报告.2004年.
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①临沂地区地质勘探队.山东省沂水县南小尧金矿区详查地质报告.1990年7月.
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