In terms of regional geological survey, the northern margin of North China Craton has completed1:200,000 geological, hydrological,1:500,000 aeromagnetic and1:kloc-0/0,000,000 gravity surveys, and some areas have completed1:500,000 geochemical surveys. In the second round of metallogenic prospect zoning in China, the North China Craton is divided into two secondary metallogenic belts, namely, the gold, silver, copper, lead, zinc, cobalt, nickel and boron metallogenic belt in the northern margin of the North China Craton (Ⅱ-3) and the gold, silver and copper polymetallic metallogenic belt in the North China Craton (Ⅱ-4). The metallogenic belt in the northern margin of North China Craton (Ⅱ-3) is further divided into three grade Ⅲ metallogenic belts, and the metallogenic belt in North China Craton (Ⅱ-4) is further divided into seven grade Ⅲ metallogenic belts (Chen Yuchuan,1999; Li Junjian et al., 2002a, b), summed up the temporal and spatial distribution of various metallic and nonmetallic deposits in this area and the comprehensive prospecting criteria. These works have created conditions for carrying out geological theoretical research and prospecting exploration of metal deposits.
In terms of ore prospecting, since 1950s, China geologists have successively carried out field geological surveys and scientific research at different scales in the northern margin of North China Craton, and successively discovered a series of minerals such as iron, gold, rare earth, graphite, boron, magnesite, non-ferrous metals and rare metals (Rui Zongyao et al., 1994). The representative iron polymetallic deposit is Baiyun Obo super-large iron-gold deposit. There are Zhulazaga and Changshanhao in Bayan Obo Rift Zone, such as Hadamengou, Saiwusu, Houshihua, Shibaqinghao, Halaqin and Moduqin in Wulashan-Daqi area, Honghuagou, Zuoshanzi and Jinchanggouliang in Chifeng area, and Jiapigou, Wulong and Paishanlou in Liaodong area in southern Jilin Province. Representative lead-zinc deposits include super-large SEDEX polymetallic massive sulfide deposits such as Dongshengmiao, Tanyaokou, Huogeqi and Jiashengpan in Langshan-Zhaertaishan area, and strata-bound hydrothermal reformed lead-zinc deposits such as Caijiayingzi, Niujuanzi, Beichagoumen, Bajiazi and Gaobanhe in Liao Yan area. Molybdenum polymetallic deposits such as Chaganhua and Chagandels in Wulate Houqi of Baoyintu uplift belt (Xi Zhong et al., 2010; Cai Minghai et al., 20 1 1), Xisha Gaide (Hou Wanrong et al., 20 10a, 20 10b), Dasuji Molybdenum Mine in Zhuozi County (Zhang Zeng et al., 2009) and Xiaodonggou on both sides of Xilamulun River. Liu et al, 20 10), the representative boron, magnesium and diamond deposits are Wengquangou superlarge ludwigite deposit in Liaoning, Dashiqiao superlarge magnesite deposit in Yingkou, Liaoning and Fuxian diamond deposit in Liaoning.
In the research of metallogenic theory, since the founding of New China, the scientific research work in this field has never stopped, and a series of scientific research works and papers have been published. Representative scientific research works related to mineralization in the northern margin of North China Craton include Geology and Mineralization of Early Precambrian in China (Zhang Qiusheng, 1984), Metamorphic Structural Evolution and Gold Mineralization of Archean Granite Belt in Daqingshan, Inner Mongolia (Gan Shengfei, 1992) and Structural Ore-controlling Analysis of Jinchanggouliang Gold Mine in Inner Mongolia (Wang Jianping et al.). ). 1992), the geology of nonferrous metal deposits in the northern margin of North China Block and its adjacent areas (Rui Zongyao et al., 1994), the geology and mineralization of Archean greenstone belt in North China Platform (Shen Baofeng et al., 1994), the geology of gold deposits in Chifeng area of Inner Mongolia (Wang Shilin et al., 65434) 1995), metallogenetic series and prospecting of metal deposits in the northern margin of North China block in Hadamengou pegmatite gold deposit geology, Inner Mongolia (Pei et al., 1998), etc., block structure and gold and iron minerals in the northern margin of North China block (1998), and mineral resources prospect evaluation of main metallogenic belts in China. 1999), regional mineralogy (Zhai Yusheng et al., 1999), China gold deposit and its metallogenic regularity (Chen Yuchuan et al., 2008) 2003), Precambrian mineralization in China (Shen Baofeng et al., 2006), metallogenic regularity and prospecting direction of main metallogenic belts in North China block (Li Junjian et al. Pei et al. (1998,2003) put forward the viewpoint that "time dimension" creates "space dimension" in evolutionary metallogeny, and combined with the analysis of metallogenic chronology, explored the division of four metallogenic levels and their coupling laws, which established a new idea and method for the regional metallogenic research in the northern margin of North China Craton. Mao Jingwen et al. (2005) thought that there were three large-scale metallogenesis in northern China in Mesozoic, which occurred in 200 ~ 160ma, 140 Ma and 120 Ma respectively. Chen Yanjing et al. (2009a, 2009b) divided the hydrothermal metallogenic system of the North China Plate into three series: magmatic hydrothermal, metamorphic hydrothermal and epithermal, and considered that the North China Craton and the eastern part of its continental margin orogenic belt had a strong mineralization in Yanshan period, and the metallogenic age gradually changed from west to east. Nie et al. (Nie, 1997a, 1997b) made an in-depth analysis of typical gold deposits in the northern margin of the North China Craton, and discussed and summarized the laws of magmatic activity, crustal evolution and gold mineralization. Mao Debao et al. (2002) divided the Pb-Zn-Ag deposit in the middle part of the northern margin of the North China Craton into three metallogenic belts and one concentrated area, and the genetic types were divided into sedimentary jet type, superimposed reformation type, epithermal type related to alkaline volcanic activity in Dahongyu period and hydrothermal type related to Mesozoic volcanic-porphyry activity. Dai Junzhi et al. (2006) considered that the eastern end of Yanliao molybdenum (copper) metallogenic belt in the northern margin of North China Craton is dominated by molybdenum ore, while the western end of Hebei Province is dominated by copper (molybdenum) ore. The deposit types are mainly porphyry type, porphyry-skarn type and skarn type, and the mineralization mainly occurs around 180 Ma and 140 Ma. Liu Jianming et al (Ceng Qingdong et al., 2009; Lichun Zhang et al., 2009; Wan et al, 2009; Zeng et al, 2010; Liu et al; Zhang Lianchang et al., 20 10) systematically studied and summarized the copper-molybdenum deposits along the Xilamulun River in northern Chifeng, and put forward the Xilamulun molybdenum (copper) metallogenic belt for the first time.
In the aspect of gold deposit geology research, predecessors summarized the geological characteristics, temporal and spatial distribution, types and genetic mechanism of gold deposits in the northern margin of North China plate from different angles (Wang,1989; Shen Baofeng et al., 1997a, b; 200 1a，b； Nie et al., 2002; Nie, 1997a,1997b; Miller et al.,1998; Zhang et al.,1999; Xiao et al.,1999,2000; Zhou et al., 2002; Hart et al., 2002; Li Junjian et al., 2002a, 2002b, 2006; Yang et al., 2003). Regarding the temporal and spatial distribution of gold deposits, Wang (1989) divided the North China Craton into 10 gold mineralization areas: Huadian, Qingyuan, Dandong-Yingkou, Chifeng-Chaoyang, Zunhua-Qinglong, Xuanhua-Chongli, Wutai, Zhongtiaoshan and so on. Mainly Zhou et al. (2002) divided the gold deposits in the northern margin of North China Craton into three concentrated areas: Daqingshan (Hadamengou) and Saiwusuyang et al. (2003) divided the gold deposits in North China Craton into three concentrated areas: (Daqingshan, Chifeng-Chaoyang, Jidong-Liaoxi, Jinan), Jiaoliao (Liaodong, Jiaodong, Luxi) and Hart et al. (2002) divided the gold deposits in the northern margin of North China Craton into three gold mineralization concentrated areas (including Zhangjiakou, Yanshan and Chifeng) and Changbai Mountain (Figure 1-2), and classified most gold deposits as orogenic gold deposits. It is considered that Jinchanggouliang gold deposit belongs to epithermal type, and Hadamengou gold deposit may be related to intrusive rocks. There are six periods: ~ ~250 Ma, ~ ~200 Ma, ~ ~ 180 Ma, ~ ~ 150 Ma, ~ ~ 129 Ma. Regarding the genetic type of gold belt, one view is that it is greenstone type gold deposit. Because most of the gold deposits in the northern margin of North China Craton occur in the Precambrian metamorphic crystalline basement greenstone belt and related magmatic rocks, some scholars classify these gold deposits as greenstone belt gold deposits (Luo Zhenkuan et al.,1994,2000; Shen Baofeng, 1994a, b,1996; Li Junjian et al., 2002a, b, 2006; Zhai Yusheng et al., 2002). Compared with the gold deposits in the greenstone belt in the world, the gold deposits in the northern margin of the North China Craton have many similar characteristics: (1) The gold mineralization is obviously regional, forming a mineralization intensive area; (2) There are greenstone belts in the mineralized area; (3) Gold mineralization has no obvious lithologic specificity, and the types of host rocks are diverse; (4) There is an obvious time difference between the mineralization time of gold deposits and the formation time of host rocks, and the mineralization is later than the formation time of host rocks; (5) Both ore deposits and ore bodies are controlled by structures, especially ductile shear zones; (6) Gold mineralization is accompanied by obvious wall rock alteration. However, due to the different geological environment, especially the superimposed transformation of late tectonic magmatic thermal events, the gold deposits in the northern margin of North China Craton have their own particularity: (1) Mineralization is often multi-stage and multi-stage, and gold mineralization in different periods is superimposed on each other, showing late mineralization; (2) The ore-forming fluid is multi-genetic, which is neither a typical metamorphic fluid nor a single magma or Tianshui fluid, but a multi-genetic mixed fluid; (3) The scale of the deposit is small and the metallogenic age is new (Shen Baofeng, 1994a, b, 1996). Shen Baofeng et al. (1996) divided greenstone gold deposits into two types: primary gold deposits in late syntectonic period and regenerated gold deposits after tectonic period. Primary gold deposits in the late syntectonic period are divided into stratabound gold deposits and vein gold deposits; The regenerated gold deposits after the tectonic period are mainly hydrothermal gold deposits related to metasomatic magmatism. Luo Zhenkuan et al. (1994) summarized the characteristics of gold deposits of greenstone type in North China craton: gold deposits are controlled by granite-greenstone terrane of craton; It is mainly distributed in the north-south margin and east of craton, controlled by tectonic magmatism induced by Phanerozoic plate movement, and mainly formed in Hercynian and Yanshan periods. Archean greenstone formation, Phanerozoic granitization and ductile-brittle shear tectonic belt are the three major factors controlling greenstone gold deposits. Nie (1990) summarized the genetic types of some greenstone gold deposits abroad. According to the combination of rock types in the greenstone belt, and considering the relationship between the metamorphic degree, tectonic environment, petrological characteristics and the spatial and temporal distribution of gold mineralization, the Archean greenstone belt can be divided into three types: (1) basalt type with relatively complete outcrop in the rockstrata; (2) The dominant type lacking the evolutionary characteristics of bimodal volcanic rocks; (3) The sedimentary strata are extremely developed, showing Dauar type. Sun Fengyue (1995) classified some representative views on the genesis of greenstone gold deposits into six types: (1) related to clastic sedimentary rocks; (2) Controlled by Komatiite; (3) related to porphyry; (4) controlled by TTG intruders; (5) It is related to felsic magmatism with high oxidation degree; (6) Controlled by lamprophyre activity. One view is that gold deposits are related to intrusive rocks. Some scholars believe that most of the gold deposits in the northern margin of North China Plate are distributed along Phanerozoic granites that intrude into Neoarchean-Proterozoic strata, and are related to granitoids in time and space, but they classify the gold deposits in the northern margin of North China Plate as gold deposits related to intrusive rocks (Sillitoe et al.,1998; Thompson et al.,1999; Lang et al., 2000; Liu Jiayuan, 1998). One view is orogenic gold deposits. Gold deposits in the northern margin of North China Craton are mainly distributed on the edge of Craton, close to the Central Asian orogenic belt, which is bound to be controlled and influenced by the northern orogenic movement. Some deposits also have the characteristics of orogenic gold belts, so they are classified as orogenic gold deposits (Miller et al.,1998; Groves et al.,1998; Hart et al., 2002; Zhou et al., 2002; Chen Yanjing et al., 2009a, b), some scholars believe that the gold deposits in the northern margin of North China are the product of multi-stage orogeny and have obvious multi-stage metallogenic characteristics. Regarding the genesis of gold deposits, Wang Yiwen (1992) thinks that the regional potential gold content is the primary prerequisite for the formation of gold mineralization concentration areas, and the formation of granite intrusions and ductile shear zones is the main driving force for gold activation in source beds (rocks). Luo Zhenkuan et al. (1994) think that the distribution area with multi-stages, complex composition and dense distribution of dikes is not only the center of magmatic activity, but also the center of tectonic activity, which is the necessary condition for gold mineralization, and the dense distribution of dikes can be used as a macro indicator for searching for greenstone gold deposits. Zhai Yusheng and others (2002) believe that the gold deposits in North China Craton were mainly formed in the activation stage of Craton, and its overall structural background can be summarized as the transition period from late compression collision to extensional structure. Gold mineralization is the product of the late evolution of tectonic granite magma. Chen Yanjing and others (1998) believe that gold deposits in North China Craton are mainly distributed in Yinshan-Yanshan-Liaoji Mesozoic intracontinental collision orogenic belt, Qinling and Jiaodong Mesozoic collision orogenic belt, Taihang Mountain and Tanlu fault magmatic belt. The metallogenic age is mainly Jurassic-Cretaceous, and the geodynamic background of mineralization is the compression-extension transition period of collision orogeny. Zhai et al. (200 1) believe that the gold concentration area in the middle part of the northern margin of North China block is controlled by the intersection area of regional tectonic framework, and the trinity structure of magmatic intrusion, basement uplift and metamorphic core complex (or basement fault uplift) under the background of extensional-compressional structure becomes the structural system that controls the gold concentration area as a whole. Regarding the classification of gold deposits, Wang et al. (1989) classified the gold deposits in North China Platform into sedimentary metamorphic type, metamorphic hydrothermal type, mixed hydrothermal type, magmatic hydrothermal type, volcanic hydrothermal type, multi-stage superposition type, associated type and placer gold type. Zhou et al. (2002) divided China gold deposits into orogenic gold deposits, skarn/porphyry copper-gold deposits, Carlin gold deposits, epithermal gold deposits and placer gold deposits. Nie et al. (2002) divided the gold deposits in Baotou-Baiyunebo area into: (1) gold deposits in Archean high-grade metamorphic rocks, such as Shibaqinghao, Laoyanghao and Houshihua; (2) Gold deposits occurring in Proterozoic shallow metamorphic sedimentary rocks, such as Saiwusu, Changshanhao and Gan Stahle Gai; (3) Gold deposits occurring in or related to Hercynian alkaline intrusive rocks, such as Hadamengou, Donghuofang and Luchang. Li Hongchen (200 1) divided the gold deposits in the northern margin of the North China Craton into nine types: Archaean ferrosilicon syngenetic gold deposits, Proterozoic anorthite syngenetic gold deposits, mylonite-type gold deposits, mylonite-belt chronological gold deposits, mylonite-belt alkaline gold deposits, mylonite-belt granite-type gold deposits, mylonite-belt volcanic-subvolcanic gold deposits, magmatic gold deposits and continental gold deposits. Li Zhongshan et al. (2004) divided the gold deposits in the northern margin of North China Craton into three categories and seven subcategories, namely, intrusive magmatic hydrothermal gold deposits (heavy magmatic hydrothermal subcategory and synmagmatic hydrothermal subcategory), volcanic-subvolcanic hydrothermal gold deposits (volcanic hydrothermal subcategory and subvolcanic hydrothermal subcategory) and sedimentary reformed gold deposits (metamorphic hydrothermal subcategory, metamorphic hydrothermal subcategory and epithermal infiltration hydrothermal subcategory). Wang Yiwen (1992) divided the gold deposits in the northern margin of North China Craton into Archean greenstone type gold deposits (Jiapigou, Paishanlou, Nanlongwangmiao, Jinchangyu, etc.). ), Proterozoic turbidite gold deposits (Baiyun, Sidaogou, Maoling, etc. ) and potash altered rock type gold deposits (Zhangjiakou, Wulashan, etc. ). Wang Youzhi (1992) divided the gold deposits in the northern margin of the North China Craton into chronological, chronological-altered, altered, porphyry and volcanic types.
In a word, the gold deposits produced by the North China Craton are mainly distributed along the edge of the Craton, including the northern edge gold belt, the eastern edge gold belt (Jinan-Liaodong, Jiaodong) and the southwestern edge gold belt (Qinling and Xiaoqinling), showing a "golden edge" (figure 1-3). The gold deposits in the northern margin of the North China Craton are characterized by "banded distribution, segmented enrichment, old ore-bearing country rocks and new metallogenic epoch", mainly distributed along the Yinshan-Yanshan marginal uplift belt near the east-west direction (Figure 1-2), and the ore-forming materials are often multi-source, and often have the characteristics of "old ore-forming material source and new ore deposit location epoch". Mineralization is often the superposition of long-term and multi-stage geological processes, which has obvious inheritance characteristics.