常福龙金矿床为受剪切带控制的低温热液脉型金矿床.由于矿化的三维连续性较差,传统手工圈连矿体难以准确刻画矿化的真实分布.隐式地质建模具有速度快、可重复性强、以数学为依据、人为干扰少等特点,尤其适合处理样品数据稠密且表面形态复杂的问题.通过引入径向基函数(RBF),对常福龙金矿床开展了三维隐式地质建模与品位估值,旨在探讨如何更好地解决复杂不连续矿体的圈定和估值问题.研究表明,在适当的约束条件下,隐式建模可以给出合理的地质模型.RBF估值与地质统计学方法的估值准确度相当,而前者呈现出的矿化结构更为清晰.研究工作对于促进隐式地质建模技术在中国资源量估算领域的应用有着一定的启示意义.

逆冲推覆构造间接控制了矿床的空间展布,其下盘发育的底板韧性剪切带、脆性逆断层及其叠加的晚期正断层构成了一套成矿构造组合.逆断层和正断层之间所夹即为矿体.断层侧列扩展造成矿体侧列分布,断层作用往北西方向逐渐减弱,造成矿体向北西倾伏至尖灭.热液成矿期可分为4个阶段,第一阶段脉状硅化,成矿作用较弱;第二阶段面状硅化-黄铁矿化,矿化强度和矿化规模均较弱,成矿贡献较小;第三阶段弥散状或脉状硅化-黄铁矿化,矿化强度和矿化规模均较强,形成工业矿体;第四阶段团块状和细脉状碳酸盐化,金成矿作用较弱.

陕西旬阳地区地处南秦岭-大别构造带中部,属旬阳-白河成矿带.在旬阳-白河成矿带内志留系地层中发现了东西长约100 km,南北宽10~50 km的铅锌矿富集区.旬阳地区的铅锌矿可以划分为南沙沟、任家沟、泗人沟、黄石板等主要矿带,均是赋存于下志留统梅子垭组和中志留统双河镇组两个赋矿层位中.通过综合分析前人对该区域研究的成果与资料,初步对旬阳地区志留系铅锌矿成矿规律与成矿模式进行了探讨,认为区内铅锌矿属于热液沉积-改造成因类型.成矿物质来源于基底岩石与地层深部,铅锌矿受志留系地层与同生断裂控制.成矿模式为海水下渗被加热形成热水-含矿热液沿同生断裂上涌沉积富集-后期热液及构造叠加改造富集成矿.

云山石墨矿床赋存于兴东群大盘道组二段一套富含石墨的片岩、变粒岩、浅粒岩等变质岩系中,矿体主要受地层控制,呈层状.区域变质作用表现为高角闪岩相变质之后又经历低角闪岩相的退变质作用过程.区域变质作用使分散状的碳质向石墨转变,形成石墨矿床,并形成伴生矿种矽线石、绿泥石.矽线石、绿泥石在不同层位具有分段富集特征,上述表明岩石成分差异和区域变质作用对矿床形成起着重要作用.分段富集为分采分选提供了依据,以提升石墨矿床综合利用价值.

燕山-太行山中生代收缩构造变形主要表现为基底卷入的逆冲构造、基底为核的大型纵弯褶皱构造,以及韧性逆冲推覆构造.构造形迹展布方向主要有近WE,NWW和NE-NNE向.在总体构造线呈NNE向展布的太行山构造带和辽西燕山东段,均发现有近WE向和NWW向收缩构造变形.收缩变形发生在二叠纪晚期、三叠纪、侏罗纪及早白垩世.它们的发生已经使克拉通遭受破坏.燕山中部近NS向构造剖面复原表明,在135 Ma之前的构造变形缩短率约为38%,华北东部晚古生代和早中生代岩相古地理研究显示,收缩变形前的地壳厚度约为35 km.如果将上述地质历史时期韧性剪切收缩变形反映的变形深度(20～25 km)作为卷入收缩变形的地壳厚度,并假定水平缩短变形量由垂向地壳加厚所调节,则在南北向缩短变形之后地壳厚度可达47～50 km,已经接近拆沉构造模型下地壳榴辉岩化所需的地壳厚度.同时,加厚地壳均衡抬升产生的重力势能差,与地壳加厚期间持续不断的岩浆活动导致的岩石圈强度弱化,为在区域构造应力状态不发生改变的情形下产生中浅部地壳的伸展垮塌创造了充分条件.因此,燕山-太行山中生代收缩构造变形,一方面直接导致了克拉通岩石圈浅层稳定状况的破坏,另一方面为在深部可能发生的拆沉作用和在浅部产生强烈伸展变形创造了有利条件.拆沉作用和伸展变形可能同是早期收缩变形导致地壳强烈加厚的结果.伸展变形既可以与拆沉作用相伴发生,也可以单独出现,不宜将浅层伸展变形作为深部拆沉作用曾经发生的直接证据.

Mesozoic contraction deformation in the Yanshan and Taihang mountains is characterized by basement-involved thrust tectonics, basement-cored buckling anticlines and ductile thrust and nappe tectonics. Most of these deformations are orientated west-east, west-northwest and northeast to north-northeast. The contraction deformations began in the Permian, continued through the Triassic and Jurassic and terminated in the Early Cretaceous, and constitute an important part of the destruction of the North China Craton. It is estimated, from balanced cross-section reconstructions, that the north-south shortening of the central part of the Yanshan belt before 135 Ma was around 38%. The initial crust thickness, pre-dating the major contraction deformation in late Paleozoic and early Mesozoic, was estimated to be around 35 km based on paleogeographic characteristics. Assuming that the inferred depth of ductile thrusting deformation, 20–25 km, was the crust thickness involved in the contraction deformation, and also assuming that the N-S contraction deformation was accommodated by vertical crust thickening, the thickness of the crust after the contraction deformation was expected to be around 47–50 km. This was the approximate crust thickness required for the eclogitization of the lower crust for delamination. The gravity potential accumulated by the isostatic uplift of the thickened crust, together with the decrease in crustal strength caused by the coeval magmatisms associated with the contraction deformation, led to the subsequent extensional collapse of the middle and upper crust although the regional stress regime associated with the plate interactions remained constant. It is inferred that the Mesozoic contraction deformations in the Yanshan and Taihang mountains were not only a significant tectonic process contributing to the destruction of the craton in middle and upper crust but also stimulated delamination at a deep level and the extension of the shallow crust. In other words, both the suspected delamination of the lower crust and upper mantle and the well constrained extension deformations of the shallow crust in the eastern North China Craton during the late Mesozoic are a consequence of crust thickening due to previous contractions. Extensional deformations could be expected to occur independently in the shallow crust, and are not necessarily associated with or responding to delamination at a deep level.

Sanyihao polymetallic deposit is located at the composite part of Tianshan-Yinshan Zonal Metallogenic belt and Iner Mongolia-Xinganling Metallogenic belt.According to the geochemical characteristics that the Mo、Pb、Zn、Ag、Cu and Au these six kinds of elements have great posibility to be enrichment and mineralization,and this area can be delineated out of 10 element content anomaly zones,theⅠ-Ⅵ zones are polymetallic ore-forming belts,the Ⅶ-Ⅹ zones are single mineral ore-forming belts.This deposit can be divided into A,B,C,D four strata belts from west to east.According to the geological and geochemical characteristics of the four strata belts,summed up the work of prospecting for the next step.