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Xiaoqinling Gold District - Tongyu, Yanzhihe, Wenyu, Dongchuang, Dahu, Qiangma, Sifangou, Yangzhaiyu, Hongtuling, Qiyugou, Fancha, Kangshan, Shanggong

Shaanxi, China

Main commodities: Au
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The Xiaoqinling (Xiao Qinling or 'Little Qinling') Gold District, which is located between Tongguan in eastern Shaanxi Province and Lingbao in western Henan Province, central China, contains a series of more than 100 orogenic gold deposits of varying sizes, with ores occurring in a number of distinct belts. The key deposits described below include: Yangzhaiyu, Wenyu, Qiangma, Hongtuling, Dahu and Fancha.   Other deposits 50 to 100 km to the SE in the Qinling-Dabie Orogen include:   Kangshan, Qiyugou and Shanggong.

This district represents an eastern extension of the more extensive West Qinling Gold Province of the West Qinling Orogen. It overlaps the Qinling Molybdenum Belt of the Qinling-Dabie Orogen. A number of the key representative deposits are descibed below. Ore occurs in breccias, in quartz veins and as disseminations in altered metamorphic rocks (#Location: Tonggu - 34° 26' 50'N, 110° 12' 03"E; Wenyu - 34° 25' 24"N, 110° 24' 20"E; Qiangma - 34° 23' 58"N, 110° 28' 9"E).

The gold deposits generally lie about 30 to 50 km inland of the southern margin of the North China Craton and are concentrated in the Xiaoqinling, and in the adjacent Xiaoshan and Xiong'ershan areas progressively to the east. See the Qinling-Dabie Orogen map for the districts location - shown as a green rectangle in the upper left of the image.

The Qinling-Dabie, West Qinling and Kunlun orogens are the eastern, central and western segments respectively that collectively make up the greater Central China Orogen. Together they extend for >3000 km, east-west, across central China, from the the major, north south Tan-Lu Fault in the east, to the ENE-WSW trending Altyn-Tagh Fault Complex to the west. The Qinling-Dabie Orogen in the east separates the North China and Yangtze cratons. The East Kunlun Orogen separates the Qaidam Block, a cratonic fragment to the north, from the Bayan-Har Terrane of the Songpan-Ganzi Complex/Terrane to the south. The West Qinling Orogen grades laterally into the Qinling-Dabie and is faulted against the East Kunlun orogens on its extremities. It lies to the east of the Qaidam Block, and is bounded to the north by the Qilian Block, another cratonic fragment that separates the Quidam Block and North China Craton in the west. To the south, the West Qinling Orogen is bordered by the Songpan-Ganzi Complex, mainly composed of Mesozoic turbidites and volcanic rocks overlying Proterozoic basment. The Xiaoqinling Gold District lies at the transition between the structural regimes of the West Qinling and Qinling-Dabie orogens.

For a more detailed description of the Qinling-Dabie Orogen see the Regional Setting section of the Qinling Molybdenum Belt record. See also the description of the geology and stratigraphy of the units described below in the same record.

The Xiaoqinling district deposits lie within the eastern, east-west trending Qinling Orogen of the greater Central China Orogenic Belt that was developed during the Mesozoic collision between the North China and the Yangtze Cratonic blocks (Chen and Santosh, 2014). The orogen incorporates four distinct tectonic units from north to south: i). the Huaxiong Block representing the reactivated southern margin of the North China Craton, ii). the Northern Qinling accretionary belt, iii). the Southern Qinling Orogenic belt, and iv). the Songpan or Mianlue foreland fold-thrust belt along the northern margin of the Yangtze Craton, respectively separated by the regional San-Bao, Luanchuan, Shang-Dan, Mian-Lue and Longmenshan fault zoness (Chen et al., 2009, 2014; Li et al., 2013).

The Xiaoqinling gold district is within the northernmost Qinling Orogen, within the western half of the exposed Huaxiong Block, bounded to the north by the Taiyao Fault (part of the San-Bao fault belt) and to the south by the Xiaohe Fault. It is ~60 km long, with deposits concentrated in the 2 to 5 km wide, WNW-ESE trending Guanyintang shear zone.

The main hosts to mineralisation are Neoarchean to Palaeoproterozoic graphite gneisses, marbles, quartzites, banded iron formations, biotite/amphibole gneisses, migmatite and amphibolites of the Taihua Supergroup. The Taihua Supergroup is separated from the Mesoproterozoic Xiong'er Group to the south by the Xiaohe Fault. The Xiong'er Group is a weakly deformed and metamorphosed volcanic succession comprising basaltic andesite, andesite, dacite and rhyolites, which are well preserved on the southern North China Craton (Chen et al., 2014), but are only found on the southern margin of the Xiaoqinling gold district.

The Taihua Supergroup was metamorphosed to amphibolite to granulite facies between 1.95 and 1.82 Ga, during assembly of the Nuna-Columbia supercontinent (He et al., 2009; Santosh, 2010; Deng et al., 2013). This sequence has been subdivided into the:
i). 3.0 to 2.55 Ga Beizi Group, composed of an intensely migmatitised high-grade greenstone assemblage containing abundant ultramafic rocks;
ii). 2.5 to 2.3 Ga Dangzehe Group, a less migmatitised greenstone assemblage without, or with only minor, ultramafic rocks; and
iii). 2.3 to 2.1 Ga Shuidigou Group, a metamorphosed sedimentary succession which is widespread in the North China Craton (Chen and Zhao, 1997).

The easliest intrusive event in the Xiaoqinling gold district is represented by 2.1 to 1.85 Ga pegmatite dykes (Zhao et al., 2009; Li et al., 2011), followed by the Paleoproterozoic (1748 Ma) Guijiayu granodiorite (Li et al., 1996), the Mesoproterozoic (1463 Ma) Xiaohe biotite granite (Li et al., 1996), Indosinian (213 to 202 Ma) alkalic porphyries and dykes and the Yanshanian (146 Ma) Huashan, Wenyu (138 to 131 Ma) and Niangniangshan (134 to 142 Ma) biotite granites (Mao et al., 2010; Li et al., 2011; Zhao et al., 2012).

Widespread dolerite, gabbro and lamprophyre dykes were emplaced in the Taihua Supergroup metamorphic rocks. Most are east-west striking, although some trend NE and NW. Most were emplaced at ~1.85 to 1.80 Ga, with minor dolerite dykes intruded from 128.6±4.7 to 126.9±4.8 Ma (Wang et al., 2008; Bi et al., 2011).

The Guijiayu granodiorite and Xiaohe biotite granite were emplaced along the Xiaohe Fault, which also subsequently displaced them. The Huashan, Wenyu and Niangniangshan granites occur in the western, central and eastern parts of the Xiaoqinling gold district respectively and are the most prominent intrusions in the district. The Wenyu granite intrudes the central zone of the gold-rich area, (just west of Tongguan) where it is exposed over an area of about 20 sq. km, although deposits are generally hosted in the Precambrian basement rocks hundreds of metres to as much as 10 km from the intrusions and their related hornfelsed aureoles.

The principal structures within the Xiaoqinling gold district are near east-west striking faults and folds. The folds are predominantly Precambrian in age, while the faults largely evolved from the Triassic to Jurassic by south-directed thrusting, and Cretaceous north-directed normal faulting (Zhang et al., 1998; Mao et al., 2002; Li et al., 2011; Zhao et al., 2011, 2012). Some faults possibly branch from reactivated Precambrian structures. The parallel Huanchiyu (to the north) and Guanyintang (~5 km to the south) shear zones, which extend over strike lengths of more than 20 km, are the core structures in the orefield. The latter is the western half of the regional east-west trending, north dipping, >60 km long Maxundao deep fault zone (that extends from Tongguan in Shaanxi Province to Lingbao in Henan), originally a compressional structure, which shows evidence for late extension.

Subsidiary faults branching from the major structures mainly trend east-west, NW or NE, and range from <1 to a few kilometers in length, with widths of several to tens of metres. These structures were developed locally, during Jurassic to Cretaceous time (Mao et al., 2002), and are characterised by an early stage of ductile deformation that was overprinted by a late brittle phase, possibly related to the Mesozoic uplift of the Neoarchean to Paleoproterozoic basement in an extensional regime (Liu et al., 1998; Zhang et al., 2000). These secondary structures are the most favourable sites for localising orebodies and granite porphyry dykes. Zhang et al. (1998) suggested the shear zones, which were intruded by the granites, are coeval with syn-collisional crustal thickening before 127 Ma, whilst the normal faults and shear zones, which crosscut the granites (e.g., the Wenyu pluton), were developed synchronously with post-collisional crustal thinning after 127 Ma.

A string of significant gold deposits, with total resources of 300 to 450 t of contained Au, occur at intersections of second order WNW to east-west striking faults with NE and NW striking faults to the north of the first-order Maxundao fault zone. There are more than 100 gold deposits in the Xiaoqinling gold district. These deposits account for more than 1200 auriferous quartz veins are known in the Xiaoqinling Gold District. These auriferous quartz veins are constrained by the dominantly reast-west trending structures described above, with the veins occurring where the ductile shear zones developed along limbs of the major folds (Mao et al., 2002), forming three three parallel ore belts, namely, the north, middle and the south ore belt (e.g., Liu et al., 2020; 2019).

These deposits of the Xiaoqinling Gold District has a proven reserve of more than 630 t of contained gold (Wu, 2012; Liu, 2013)

Ores contain pyrite, galena, sphalerite and minor magnetite, scheelite, wolframite, molybdenite, stibnite, pyrrhotite and gold. The gangue assemblage includes quartz, calcite, ankerite, minor rutile, barite, siderite and fluorite. The alteration halos sandwiching quartz veins or shear zones comprise mainly quartz, sulphide minerals, white mica and carbonate minerals, with lesser chlorite, epidote, and biotite.

Li et al. (2002) constrained the mineralisation of one of these, the Dongchuang deposit, to have been emplaced between 143 and 128 Ma. They also obtained 40Ar/39Ar plateau ages of 142.9±2.9 Ma, 132.2±2.6 Ma and 128.3±6.2 Ma for hydrothermal quartz separates from stages I, II and III mineralised veins, respectively, and a 40Ar/39Ar plateau age of 132.6±2.7 Ma for sericite separates from a mineralised stage II veinlet. Li et al. (2012) have reported 40Ar/39Ar plateau ages of 124.07±1.27 and 125.4±0.4 Ma for mineralisation related sericite from the Qiangma deposit.

This suggests that the gold mineralisation in the Xiaoqinling gold district was emplaced in the Early Cretaceous, and was intimately involved in the Mesozoic tectonic-metallogenic event caused by the Yangtze-North China continental collision that commenced at the close of the Triassic, culminated in the Jurassic, and waned by the Early Cretaceous (Chen et al., 2009; Jiang et al., 2009, 2010; Xu et al., 2010; Li et al., 2011; Ni et al., 2012, 2014). The tectonic regime within the Qinling Orogen changed from Jurassic compression, through Late Jurassic transpressive compression, to Early Cretaceous extension. During this period, large-scale fluid circulation, granitic magmatism and metallogenesis took place within the Orogen, although Zhou et al. (2014) note that most gold deposits show no direct spatial relationship with Yanshanian intrusions. The gold deposits are interpreted to have formed during the period of relaxation of compressional stresses, following the main collisional phase. Hydrothermal and magmatic events occurred locally where extension-related Precambrian basement uplift took place along the suture between the Yangtze and North China cratonic blocks.

Isotope and fluid inclusion geochemistry studies of the Wenyu and Qiangma deposits (described below) by Zhou et al., (2014 and in press in 2014) show i). a decrease in pressure and temperature from early to late stages of development of the deposit, probably related to uplift and mountain-building; ii). ore fabrics changed from early-stage compressive shearing to late-stage open space filling, with quartz and pyrite changing from structurally deformed early-stage anhedral grains to unstrained late-stage euhedral crystals; and iii). ore-forming fluids (in fluid inclusions) changed from pure carbonic metamorphic to mixed carbonic-aqueous to aqueous water-dominated meteoric fluids. The latter, supported by inclusion geochemistry, shows these deposits were associated with the mixing of mesothermal, CO
2-rich fluids that originated from metamorphic devolatilisation of the host sequence, and descending meteoric waters, in a regime that fluctuated from lithostatic/supralithostatic to hydrostatic fluid pressure, and occurred at depths of 10 to 14 km, straddling the brittle-ductile transition. Whilst these deposits are beyond the metamorphic aureole of the Yanshanian granites (e.g., the anatectic Wenyu Granite), the same authors imply other deposits within the zone of influence of the intrusions may be intrusive-related and epithermal in nature. The same orogenic processes would have driven both metamorphic devolatilisation and granite formation.

From west to east in the Xiaoqinling Gold District, gold deposits hosted in rocks of the Taihua Supergroup are concentrated in three goldfields within a 60 x 15 km corridor, 2 to 15 km north of the Maxundao fault.   These are the (after Mao et al., 2002):
i). Tongyu Goldfield, including the Tongyu (32 t Au @ 8 to 20 g/t Au) and Yanzhihe deposits;
ii). Wenyu Goldfield, including the Wenyu (50 t Au @ 6.5 g/t Au), Dongchuang (55 t Au @ 7 g/t Au), Sifangou (37 t Au @ 10 g/t Au), Yangzhaiyu (50 t Au @ 11 g/t Au) and Qiangma (>50 t Au @ 8.9 g/t Au) deposits; and
iii). Dahu Goldfield, including the Dahu (63 t Au @ 6 g/t Au) and Linghu deposits.
The larger deposits occur as 4 to 20 m wide and >4 km long quartz veins which lie within second order faults, while lesser amounts of gold occur in altered rocks along ductile brittle shear zones and in breccia bodies.
Some 50 to 100 km to the ESE and SE of the main Xiaoqinling Gold District, similar gold deposits are hosted by Neoarchean Taihua Group metamorphic rocks and Mesoproterozoic Xiong'er Group volcanic rocks, including Kangshan in the Xiong'ershan District, as well as Shanggong and Qiyugou, as described below.

DEPOSITS


Yangzhaiyu
The Yangzhaiyu gold deposit (Li et al., 2012). Gold mineralisation is hosted in Neoarchaean to early Palaeoproterozoic amphibolite facies metamorphic rocks, occurring as both auriferous quartz veins and subordinate disseminated ores in the alteration zone proximal to the veins. Ore-related hydrothermal alteration is dominantly sericite + quartz + sulphide assemblages close to gold veins, and biotite + quartz + pyrite ± chlorite ± epidote distal from mineralisation. The dominant sulphide mineral is pyrite, locally coexisting with minor amounts of chalcopyrite, sphalerite and galena. Gold occurs mostly as free gold, enclosed within, or filling, microfractures of pyrite and quartz, and is also present in equilibrium with Au-bearing tellurides, mainly petzite and calaverite coexisting with hessite, tellurobismuthite and altaite.


Wenyu
The Wenyu gold deposit, which comprises ~40 auriferous quartz veins, is located in the southern part of the Xiaoqinling terrane, and hosted by metamorphic rocks of the Taihua Supergroup within the Guanyintang shear zone. The large gold bearing veins at Wenyu are usually hosted in ductile–brittle shear faults that trend the east-west, whilst the relatively small quartz veins occupy NNE and NNW trending structures (Xu and Fan, 2003). These veins commonly dip at 40 to 60° to the south and where the strike and/or dip change tend to swell. The largest vein (S505), has a strike length of 4.2 km, and varies from 0.2 to 8.2 m in thickness. The second largest vein (S512), has a strike length of up to 4 km, with a thickness of 0.1 to 2 m (Jiang, 2000). Other veins are ~100 to 2000 m in length, and 0.5 to 1.5 m thick, but may extend for as much as 1 km down-dip. Ore grades range from 2.3 to 248 g/t, although most are from 5 to 17 g/t Au (Mao et al., 2002; Wang, 2009).
  Orebodies are mainly hosted by ductile–brittle faults with reverse or normal displacement of several to tens metres. High-grades preferentially within structural jogs, strike or dip changes, bifurcations and splays (Li et al., 2012; Wang, 2009). The gold ore is predominantly hosted by quartz veins, with lesser mineralisation in the altered wallrock selvedges.
  Hydrothermal alteration associated with gold mineralisation includes silicification, potassic alteration, pyrite, sericite and carbonates. Major ore minerals are pyrite and native gold and electrum, with subordinate galena, sphalerite, chalcopyrite, and locally molybdenite and scheelite (Chen and Fu, 1992). The dominant gangue mineralogy includes quartz (~90%), feldspars, sericite, chlorite and calcite. Both native gold and electrum are predominantly present as veinlets or inclusions in pyrite coexisting with galena and chalcopyrite, with lesser disseminations in quartz. Minor Au-tellurides (e.g., calaverite) are also found as inclusions in pyrite. The morphology of the gold is variable, ranging from veinlet, tear-drop-like to irregularly-shaped and dendritic forms (Zhao et al., 2011, 2012; Zhou et al., 2011).
  The mineralisation has been divided into:
i). Early stage, characterised by an assemblage of quartz + pyrite. The quartz is white or milky, and comprise ~95 vol.% of the vein, whilst pyrite is ~5 vol.%, occurring as coarse-grained, euhedral and cubic forms.
ii). Main stage, which contains the bulk of the gold mineralisation, and is characterised by quartz–sulphide veins. Locally this phase may occur along both margins of early-stage veins. Quartz is smoky grey and fine-grained, and is characteristically coherent with subhedral to anhedral fine-grained pyrite, as well as chalcopyrite, galena, sphalerite, native gold and tellurides. The sulphides usually occur as bands, thin veinlets and crumb forms within the quartz.
iii). Late stage, which is characterised by carbonate + quartz veins, with trace pyrite containing no gold, commonly occurring as veinlets cross-cutting the earlier formed quartz. (This description os paraphrased after Zhou et al., 2014).
  Published reserves and resources are (Zhou et al., 2014, after Cun, 1992):
   proven reserve - 75.144 t Au @ 7.65 g/t Au, plus
   indicated resource of 34.3 t Au.


Qiangma
The Qiangma gold deposit located in the southern part of the Xiaoqinling gold field. It comprises ~13 auriferous quartz veins, hosted by Taihua Supergroup metamorphic rocks within the Guanyintang shear zone. The host sequence is intruded by numerous dykes in the mine area, including granite, pegmatite and dolerite. Some of the latter, which are dated at 1829.5±7.6 Ma (in-situ zircon U-Pb, Wang et al., 2008) and are strongly deformed and mylonitised, are cut by gold-bearing veins.
 The auriferous veins of the Qiangma deposit are mainly controlled by near east-west trending subsidiary faults that dip to the south at variable angles of from 25 to 70°, and by minor NNW-trending structures, dipping NEE at high angles, to vertical (Yang et al., 2010). The faults hosting mineralised veins are ductile-brittle structures, with reverse or normal displacement of several to a few tens metres. High-grade sections of the veins preferentially occur in structural jogs, changes in strike and dip, bifurcations, and splays (Wang et al., 1993; Li et al., 2012). Some veins show laminated textures.
  Gold occurs both within the quartz veins, and to a lesser degree in adjacent altered wallrocks. The veins have been subdivided into two groups, based on their orientations, as indicated above. The first group strikes at 275 to 290°, and dips south at angles of 25 to 60°. The second group strikes at 330 to 360º, dipping 70 to 90° to the NEE and includes the largest veins in the deposit, e.g., the largest vein of the deposit (No. 410), with a length of 1680 m, and thickness of 0.54 to 1.08 m, and the second largest (No. 101), developed over a strike length of 1250 m, that is 0.48 to 0.83 m thick (Wang et al., 1993; Yang et al., 2010). The other veins are generally 100 to 1000 m long, and 0.1 to 4.15 m thick. Ore grades vary from 0.05 to 386.7 g/t, with the majority in the range 6 to15 g/t (Wang et al., 1993).
  The principal ore minerals are gold and pyrite, with subordinate chalcopyrite, galena, sphalerite and magnetite. Gangue minerals are predominately quartz, feldspars, sericite, chlorite, ankerite, and calcite.
  Three types of pyrite are recognised, based on morphology, texture and paragenesis, namely:
i). Type 1 pyrite, which occurs as coarse (generally >2 mm), euhedral to subhedral grains, which have a cubic or pyritohedral form. These appear as isolated or aggregate masses in milky quartz veins.
ii). Type 2 pyrite is dominantly subhedral to anhedral, and fine- to medium-grained (0.02 to 1 mm). Many grains are broken or brecciated, and show foam textures, micro-fissures, and are brecciated. These porous or fractured pyrites often contain higher Au concentrations and usually coexist with chalcopyrite, galena and sphalerite in smoky grey quartz veins.
iii). Type 3 pyrite is fine-grained (0.01 to 0.5 mm) and euhedral, occasionally observed in quartz+carbonate veins.
  The ore is disseminated, brecciated, stockwork, cloddy, veined or veinlets. Ore minerals are euhedral to subhedral, whilst metasomatic textures and fragmentation are commonly observed, indicating the deposit was formed as a result of hydrothermal replacement, exemplified by the replacement of, chalcopyrite by galena. Hydrothermal alteration is widespread within the deposit, with quartz, sericite, K feldspar, chlorite, carbonates and sulphides being main wallrock alteration phases. Gold mineralisation is closely associated with silica, pyrite, K feldspar and sericite (Yang et al., 2010).
  Three hydrothermal stages can be identified, based on the mineralogical assemblages and crosscutting relationships, namely:
i). An early stage, represented by the assemblage of quartz+pyrite. The quartz is white or milky, characterised by minor coarse-grained, euhedral, cubic pyrite.
ii). A middle stage, which is characterised by quartz-polymetallic sulphide veinlets, representing the main gold-introducing event. Quartz is smoky grey and fine-grained, generally coherent with subhedral to anhedral, fine to medium grained pyrite, as well as chalcopyrite, galena, sphalerite and native gold. The sulphides usually occur as veinlets and disseminations in the middle-stage quartz.
i). A late stage is typified by a quartz-carbonate assemblage, with a trace amounts of pyrite but no gold, commonly occurring as veinlets crosscutting the earlier formed quartz veins and altered wallrocks.
  The deposit contains an estimated reserve of >50 t Au @ 8.9 g/t (Mao et al., 2002; Zhao et al., 2011)


Hongtuling
  The Hongtuling deposit is developed within a host sequence composed of Neoarchaean to Palaeoproterozoic metamorphic rocks of the Taihua group, consisting of biotite plagioclase gneiss, amphibolite and migmatite. The structures in the deposit area are dominated by WNW- to east-west trending faults that have been interpreted to have been produced during the Triassic orogeny (Li et al., 2012), with minor NE-trending structures, both of which host molybdenum and gold veins. Granite pegmatite, monzogranite, and numerous mafic dykes intrude the metamorphic rocks. Whole rock K-Ar results indicate emplacement of mafic dykes in the Early Cretaceous (Pang et al., 2005). There is no spatial relationship between these intrusions and mineralisation veins.
  The Hongtuling deposit comprises ten gold-bearing quartz-sulphide veins. With exception of vein S1002 that is localized in a NE-trending fault, all other gold veins are hosted in WNW- to east-west trending faults dipping at 16 to 60°S. The largest vein in the mine, S8201 accounts for 47% of the known resource (Ye et al., 2003). This vein is 722 m long, 0.15 to 7.55 m thick and extends vertically from 1672 to 936 m above sea level (Qi, 2010). The longest vein, S875, is ∼3.7 km in length, 1.0 to 3.5 m in width and ∼1500m in vertical extent (Wang et al., 2002; Lingbao Hongxin Mining Ltd, 2015).
  Pyrite is the dominant sulphide mineral in gold veining. It is associated with minor to trace amounts of chalcopyrite, galena, sphalerite, melonite, calaverite and tellurobismuthite. The gangue minerals include quartz, sericite and biotite with accessory monazite. Gold mainly occurs as native gold interstitial to pyrite, quartz and galena or included in those minerals (Ye et al., 2003) and is associated with hydrothermal alteration including pyrite, silica and sericite.
  A Mo-dominated vein (M-1) has been encountered at the deepest extremity of vein of S875 in the northern part of the deposit area. This vein is 380 m long and 10.6 to 37.0 m thick, and comprises K-feldspar, quartz, calcite, molybdenite, and other sulphide minerals (Lingbao Hongxin Mining Ltd, 2015)lies within the same fault as the S875 gold vein, but it is locally crosscut by the gold veins. The molybdenum vein is dominated by molybdenite, with lesser pyrite, galena and scheelite, which account for ∼4 vol.% of the vein. Gangue minerals are calcite, quartz, K feldspar, and celestite with accessory monazite, titanite, rutile, xenotime, apatite and aeschynite. Hydrothermal alteration associated with the Mo mineralisation is well developed, forming calcite, quartz and K feldspar as selvages on the molybdenum veins.
  Proved reserves are ∼42 t of contained Au in ore with a grade of 12.87 g/t (Qi, 2010; Lingbao Hongxin Mining Ltd, 2015 as quoted by Zhao et al., 2019) equating to 3.26 Mt of ore.
  This description is drawn from Zhao et al. (2019).


Dahu
  The quartz vein-style Dahu Au-Mo deposit has proved reserves of ~ 6.6 Mt @ 4.7 g/t Au, for 31 t of contained gold and ore averaging 0.13% Mo containing 30 000 t molybdenum (Feng et al., 2011), with an annual gold production of ~0.30 t Au and ~900 t Mo.
  The deposit is located on the northern side of the Wulicun anticline, hosted by biotite plagiogneiss, amphibole plagiogneiss and amphibolite of the Archaean Taihua Supergroup, half way between the Wenyu granite, 7 km to the west, and the Niangniangshan granite, a similar distance to the east. The Taihua Supergroup was intruded by more than 50 mafic dykes (1816±14 Ma by U-Pb zircon; Bi et al., 2011), that dominantly strike NW and dip NE are known in the deposit area, with varying strike lengths and widths from 10 to 1100 m and 0.5 to 50 m, respectively ( Yang et al., 1995). Several granite porphyry dykes are also present, striking NW, and dipping NE, with strike lengths and widths from 10 to 1100 m and 3 to 6 m, respectively (Yang et al., 1995). These rocks are locally cut by mineralised quartz veins, of undetermined age. The major structures at the Dahu deposit are east-west, NW-SE, and NE-SW striking faults. The NW-SE and NE-SW faults are predominantly filled by mafic and granite porphyry dykes, whilst the east-west structures control the mineralised quartz veins, designated from north to south, F1, F8, F7, F35, F5, and F6. The curvilinear 8 km long by 10 to 150 m wide F5 fault zone is the largest ore-bearing structure. It varies in strike from WNW-ESE to ENeast-westSW, but is generally north dipping.
  Mineralised quartz veins dip at 23 to 52°NW, with individual veins being parallel, or slightly oblique to, each other and the host structures. Gold and molybdenum ore blocks are based on a cutoff grade of 1 g/t Au and 0.03% Mo, respectively. The two metals occur in different veins or in different parts of the same vein and locally overlap. Molybdenite is widespread in gold ores and gold and molybdenum ore blocks usually contain sub-economic concentrations of the other metal. Within individual faults, gold orebodies are more developed in the higher levels, while molybdenum orebodies are more developed at deeper levels.
  Twenty-five gold orebodies extend down dip over a ~1200 m vertical interval from surface. The No. 19 orebody, which dips a 33°NW, and is from 0.5 to 17.4 m thick (average 2.0 m) is the largest gold lode, containing 14 t of Au at an average grade of 6.6 g/t and an average molybdenum grade of 0.04% (Yang et al., 1995). It has a total vertical extent of 940 m, and a strike length of about 1490 m, with pinch and swell domains and branches.
  Ten molybdenum orebodies, which are all blind,extend from ~260 m to ~800 m below the surface. The largest molybdenum orebody 'F5-up2', has a molybdenum reserve of 12 000 tonnes at a grade of 0.12% Mo. It dips at 29°NW and varies in thickness from 0.7 to 38.2 m, averaging 8.9 m, with a strike length of 1660 m. The Mo(%):Au (g/t) grade is ~5:1.
  The mineralised quartz veins are mainly composed of quartz (>80%) and sulphides (<10%), with widths typically varying from tens of centimetres to several metres. The dominant sulphides are pyrite, molybdenite, chalcopyrite and galena. Gold and molybdenite often appear closely together, although a direct contact of gold and molybdenite is rare. Other commonly observed vein minerals are K feldspar, covellite, bornite, anhydrite, celestine, barite, calcite, ankerite, monazite and biotite.
  Four mineralisation stages are recognised, from early to late, i). quartz-K-feldspar stage, ii). pyrite-molybdenite, iii). sulphide-telluride-sulphosalts-gold, iv). and carbonate-barite stage. Stage , i). and ii). are molybdenite deposition stages, while stage iii). is the gold deposition event.
  Ore-related hydrothermal alteration assemblages includes K feldspar, biotite, chlorite, sericite, silica and carbonates, divided into an:
• Inner alteration zone - which surrounds all of the molybdenum-mineralised quartz veins and some gold-mineralised quartz veins, comprising a K feldspar rich halo with a characteristic reddish colouration. The width of this selvedge is less than the width of the vein, and varies from several mm to several metres. Wall-rock plagioclase and biotite have been >50% altered, and amphibole virtually obliterated. The alteration assemblage mainly comprises K feldspar, sericite, carbonates and quartz, with K feldspar, formed by replacement of plagioclase, dominating.
• Outer alteration zone - more distal to the veins, where the inner alteration zone gradually gives way to an alteration zone characterised by sericitisation of plagioclase, and chloritisation of biotite and amphibole. Plagioclase has been >30% altered to sericite. Amphibole has been >20% altered to biotite and chlorite.


Fancha
  The Fancha gold deposit is located in the southern east-west ore belt of the Xiaoqinling gold district, located on the eastern plunging crown of the Laoyacha Anticline. Deformation within the district produced a series of ~east-west to NW‐striking faults which localised shearing and folding. The Laoyacha Anticline is the major fold in the deposit area, and has a gently dipping northern and steep dipping southern limb. Numerous subsidiary faults were developed in both limbs of the anticline, providing space for gold‐bearing veins. Gold bearing quartz veins are hosted by biotite plagiogneiss, amphibole plagiogneiss, migmatite and amphibolite of the Neoarchean Taihua Group. The numerous granite pegmatite and mafic dykes in the mining area were formed prior to gold mineralisation, whilst a few mafic dykes have been cut by gold veins and are strongly deformed and mylonitised. In situ zircon U-Pb dating suggests these dykes were emplaced between 140 and 137 Ma (Ren, 2012). Gold mineralisation is predominantly found as auriferous quartz veins and within subordinate altered wall rocks. Tens of mineralised quartz veins have been outlined, most of which are from 0.3 to 6.5 m thick and extend for several kilometres in an ~east-west and NNE direction, with dips to the south and NW respectively at angles averaging ~35°.
  Dominant ore minerals are native gold and pyrite, with lesser chalcopyrite, galena, sphalerite, telluride, Bi‐sulphosalt, bornite, native bismuth and magnetite. Gangue minerals are mainly quartz and calcite, followed by biotite, sericite, K feldspar, monazite, rutile, apatite and chlorite. Ore‐related hydrothermal alteration assemblages include silica, sulphides, K feldspar, biotite, chlorite, sericite and carbonate. A four‐stage mineralising paragenesis is recognised from field and microscopic observations. The pyrite morphology in the first three mineralisation stages suggest pyrite can be divided into three generations: Py1, Py2 and Py3. Stage 1, the initial pyrite‐quartz phase, is characterised by massive milky quartz with minor coarse grained, euhedral to subhedral pyrite (Py1) that are typically inclusion‐free and gold poor. Some of these are well developed in microfractures, indicating deformation during the mineralising process. Stage 2 is pyrite‐dominated, and characterised by fine to medium‐grained, between several µm and 4 mm, euhedral to subhedral pyrite (Py2) hosted by light grey quartz. These light grey quartz‐pyrite veins usually cut the Stage 1 milky quartz. Most pyrite grains are porous or fractured, with the latter usually filled with other minerals, such as native gold, galena, chalcopyrite, sphalerite, tellurides and Bi‐sulphosalts. Stage 3, the base‐metal sulphide phase, is characterised by abundant galena, chalcopyrite and sphalerite, as well as accessory gold and tellurium-bismuth compounds, in which pyrite (Py3) is commonly intergrown with these sulphide minerals. The pyrite of this stage is typically subhedral to anhedral and ranges from 0.05 to 2 mm in diameter, and also contains abundant aforementioned mineral inclusions. Stage 4, the final barren carbonate‐dominated phase, is characterised by millimetre to centimetre wide carbonate and quartz veins. The deposit has proved reserve of 12.66 t Au @ a mean grade of 11.45 g/t Au (Ren, 2012).
  The information in this description is drawn from Liu et al. (2019).

OTHER DEPOSITS to the East and Southeast
Medium to large gold deposits hosted by Neoarchean Taihua Group metamorphic rocks and Mesoproterozoic Xiong'er Group volcanic rocks are also known 50 to 100 km to the ESE and SE of the main Xiaoqinling Gold District. These include Kangshan (22 t Au @ 4 to 8 g/t Au) in the Xiong'ershan District, Shanggong (>30 t Au @ 6.9 g/t Au) and Qiyugou, controlled by a group of NE striking faults and shear zones, which are the second-order structures to another major east-west striking fault zone. Shariggong and Kangshan are on the 33 km long, NE-trending Kangshan-Qiliping ductile-brittle shear. Mineralisation is hosted in Mesoproterozoic felsic to intermediate volcanic rocks. The steeply dipping orebodies are 250 to 750 m long and I to 2.8 m wide veins filling brittle structures, lenses in tension gashes, alteration bands along shear zones and brecciated country rock. The ores generally contain anomalous Ag, Te and Pb concentrations. Alteration halos around the orebodies are characterised by a I to 3 m wide proximal sulphide-ankerite-muscovite zone, a I to 20 m wide pyrite-ankerite-muscovite-chlorite transitional zone, and an outer 50 m wide distal chlorite-calcite zone.


Kangshan
The Kangshan gold-polymetallic deposit lies within the Xiong'ershan District, ~75 km SE of the main Xiaoqinling Gold District, and like the latter district is located on the southern margin of the North China Craton. It is ~20 km west of the Shiyaogou molybdenum deposit (described in the Qinling Molybdenum Belt record and shown on the Qinling-Dabie Orogen map). It lies on a branch of the east-west to ESE-WNW-trending Machaoying Fault Zone (MF on the map linked above) that marks the southern margin of the North China Craton and is a trans-lithospheric structure (Hu et al., 1988). Au-polymetallic mineralization is hosted in the Neoarchean Taihua and Mesoproterozoic Xiong'er groups (described in the Qinling Molybdenum Belt record). Mesozoic granitoid intrusions are widespread within and surrounding the district, e.g., the 131.0 ±0.6 Ma (Cao et al., 2016) Leimengou granitoids.
  Faulting is well developed in the Kangshan deposit area, the largest of which is the Sanmen-Lingtai Fault, which is the northernmost structure of the Machaoying Fault Zone. It is ~35 km long and several metres wide, with an east-west strike and dip of ~60°N. Crosscutting NE-SW trending faults are the principal ore-controlling structures, the largest of which is the 35 km long, several metres wide and 50 to 60°NW dipping Kangshan-Qiliping Fault. This structure possibly post-dates the Sanmen-Lingtai Fault, which it cuts. Most ore veins follow this NE-SW trend and are almost entirely to the south of the Sanmen-Lingtai Fault. North-south, pre-mineralisation, predominantly extensional faults are 0.5 to 1.5 km long, 5 to 20 m wide, and mainly filled by Mesoproterozoic diorite dykes.
  The Kangshan orebodies are auriferous quartz veins in the footwall of the Sanmen-Lingtai Fault. They are 0.1 to 20 m thick, with and lengths of tens to hundreds of metres, with most dipping at 50 to 85°, mostly ~70°NW. Orebodies in the east of the deposit area are veins in which the predominant ore element is Au. The larger have a maximum depth limit of 620 m below the surface. Orebodies in the western part of the deposit area are veins in which Pb, Zn, Ag and Au predominate with a maximum depth limit of ~300 m below the surface. The largest NE-SW trending orebody vein dips at 40 to 75°NW, and is 3000 m long, 0.25 to 2.8 m wide, and spans a vertical interval of 620 m from its deepest point to the surface. Disseminated pyrite in the Sanmen-Lingtai Fault has been interpreted to indicate it was a channel for the introduction of hydrothermal fluids.
  The ore-forming process at Kangshan have been divided into three hydrothermal stages:
Stage 1 - an early barren quartz ±pyrite stage.
Stage 2 - the major mineralising stage, which has been subdivided into Stage 2-1, the major Au mineralising event, mainly comprising banded quartz-sulphide veins containing quartz, pyrite, chalcopyrite and electrum; and Stage 2-2, the major Pb-Zn-Ag mineralising episode containing a little Au but mainly quartz-sulphide veins containing galena, sphalerite, pyrite, quartz and ankerite, with minor chalcopyrite, Ag-bearing tetrahedrite and electrum.
Stage 3 - a late quartz-carbonate phase, with mainly quartz, carbonates such as calcite and ankerite, and minor fluorite (quartz-carbonate ±fluorite).
  The principal ore minerals of the deposit are pyrite, sphalerite, galena and chalcopyrite, with minor bornite, electrum and Ag-bearing tetrahedrite. The principal auriferous mineral is electrum, comprising 66 to 73 wt.% Au and 28 to 34 wt.% Ag. The major Ag mineral is Ag-bearing tetrahedrite, containing 1.8 to 3.5 wt.% of Ag. Major gangue minerals are quartz, ankerite, calcite and fluorite. The ore minerals occur in quartz veins, with different minerals having different forms e.g., pyrite is mainly fine-grained euhedral cubic and medium to coarse grained subhedral aggregates; chalcopyrite, sphalerite, galena and bornite are mainly anhedral, filling fractures in or between minerals, or replacing pre-existing minerals, with some chalcopyrite occurring unevenly in sphalerite grains; electrum is mainly found together with chalcopyrite or in fractures in pyrite or quartz, with some occurring in sphalerite grains; Ag-bearing tetrahedrite occurs mainly with galena.
  Wall-rock alteration predominantly comprises zones of phyllic, sericite, chlorite and carbonate. Phyllic alteration occurs in the innermost 1 to 3 m wide zone, characterised by a quartz and sericite assemblage, containing the highest Au grades. The intermediate transitional sericite-chlorite zone has a width of 2 to 4 m, with grading from sericite-calcite to chlorite-epidote-calcite assemblages. The outermost chlorite-carbonate zone is 4 to 8 m wide and is characterised by an assemblage of chlorite-epidote-calcite. Late stage carbonate alteration is widespread, with euhedral-subhedral carbonate minerals such as calcite and siderite occurring in veins and veinlets.
  The information in this description is drawn from Zhang et al. (2020).


Qiyugou
  The Qiyugou breccia pipes are spatially associated with the Leimengou porphyry Mo deposit which is ~2 km to the west (described in the Qinling Molybdenum Belt record and shown on the Qinling-Dabie Orogen map). At least seven auriferous breccia pipes are found within the Qiyugou district. No. 2 and No. 4 have been the main producers with total 'reserves' of ~40 t of contained gold (Mao et al., 2002). Ore grades range from 3 to 5 g/t and up to 7 g/t Au (Chen et al., 2009). Higher grades occur in zones of complex alteration and of greater clast population.
  The auriferous breccia pipes are hosted by the Taihua Supergroup to the west of a Cenozoic basin. NW- and NE-trending faults are the principal hosting structures, formed by NE–SW and NW–SE compression during the Mesozoic (Gao et al.,1994). The breccia pipes have an elliptical shape in plan, with long axes ranging from <40 m to >1 km and have been traced vertically for more than 300 m. They contain clasts of Archaean basement rocks (migmatite, gneiss and amphibolite), Palaeoproterozoic Xiong'er Group volcanic rocks and Mesozoic granitic lithologies. Clasts range from a few cm to metres across and vary from angular 'jigsaw-fit' to rounded, suggesting multiple phases of volatile activity from hydraulic fracturing to features typical of fluidisation. The outer margins with unbrecciated wallrock are abrupt. Wallrocks proximal to the breccia pipes have been cracked, forming shatter rims several to tens of meters wide (Fan et al., 2000). Orebodies are located in the parts of the breccia pipes that are associated with faults, and the ores are associated with vein-like fine-grained metasomatic chert.
  Mineralisation styles include vein, disseminations and stockworks, with ore zones forming sub-parallel sheets that are near perpendicular to the pipe walls. The bulk of the gold is associated with sub-horizontal quartz veins that contain adularia and pyrite. The main ore minerals are pyrite, chalcopyrite, galena and native gold, with lesser sphalerite, electrum, molybdenite, chalcocite and magnetite, filling open spaces between the breccia clasts. Bi-sulphosalts and -sulphides have been reported (Shao and Li, 1989). Gold is predominantly within the fine-grained pyrite, both as inclusions and as fissure-fillings. The wallrocks have undergone potassic, silica, epidote, sericite, chlorite, carbonate, propylitic and pyritic alteration. Adularia, epidote and silica alteration are mainly confined to the breccia pipe, whereas propylitic alteration affects the wallrock. Within the breccia pipe, the matrix has been more altered and gold mineralised than in the breccia clasts. Potassic alteration (including K feldspar, adularia, biotite and sericite), silicification and abundant sulphides (particularly pyrite) are generally indicative of better gold grades (Chen and Fu, 1992). Two alteration events are recognised. Potassic alteration is the earlier and precedes gold mineralisation, mainly affecting gneisses and volcanic wall rocks and comprising of K feldspar and quartz. The second is restricted to the pipes and comprises two sub-stages: i). Pervasive, comprising chlorite, actinolite, green biotite, epidote, quartz, adularia, calcite and sericite. The paragenetic sequence proceeds from green biotite+actinolite to epidote+chlorite+pyrite. ii). Vein and open space filling quartz, adularia with calcite and minor sericite, which affects not only the breccia clasts, but also the matrix. Calcite is a late phase, and cuts quartz veins, clasts, and the cementing material. Adularia and calcite infill open spaces and/or fissures in pyrite, or form veins that cut altered clasts. Textural relationships suggest gold mineralisation is paragenetically associated with adularia-calcite and pyrite.

Epithermal accumulation are also noted in the district (e.g., Qiyugou and Dianfang ) hosted in volcanic breccia pipes. Other deposits include: Laowan (24 t Au @ 5 g/t Au);  Yindongpo (46 t Au @ 5 g/t Au).

The most recent source geological information used to prepare this summary was dated: 2020.     Record last updated: 21/1/2021
This description is a summary from published sources, the chief of which are listed below.
© Copyright Porter GeoConsultancy Pty Ltd.   Unauthorised copying, reproduction, storage or dissemination prohibited.


Tonggu

Wenyu

Qiangma

  References & Additional Information
   Selected References:
Chang, H., Wu, Y., Zhou, G., Zhang, W., He. Y., Yujie, Z., Hu, P. and Hu, Z.,  2021 - Zircon U-Pb geochronology and geochemistry of the Lajimiao mafic complex in the Shangdan Suture Zone, Qinling orogen: Petrogenesis and tectonic implications: in    Lithos   v.390-391, 16p. doi.org/10.1016/j.lithos.2021.106113.
Chen, Y.-J., Pirajno, F., Li, N., Guo, D.-S. and Lai, Y.,  2009 - Isotope systematics and fluid inclusion studies of the Qiyugou breccia pipe-hosted gold deposit, Qinling Orogen, Henan province, China: Implications for ore genesis: in    Ore Geology Reviews   v.35, pp. 245-261.
Deng, J. and Wang, Q.,  2016 - Gold mineralization in China: Metallogenic provinces, deposit types and tectonic framework: in    Gondwana Research   v.36, pp. 219-274.
Hu, P., Wu, Y., Bauer, A.M., Zhang, W. and He, Y.,  2021 - Zircon U-Pb geochronology and geochemistry of plagiogranites within a Paleozoic oceanic arc, the Erlangping unit of the Qinling accretionary orogenic belt: Petrogenesis and geological implications: in    Lithos   v.394-395, doi.org/10.1016/j.lithos.2021.106196.
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Liu, J., Wang, Y., Huang, S., Wei, R., Sun, Z., Hu, Q. and Hao, J.,  2019 - The gold occurrence in pyrite and Te-Bi mineralogy of the Fancha gold deposit, Xiaoqinling gold field, southern margin of the North China Craton: Implication for ore genesis: in    Geological Journal   Online pp. 1-21. doi:10.1002/gj.3637.
Liu, J., Wang, Y., Mao, J., Jian, W., Huang, S., Hu, Q., Wei, R. and Hao, J.,  2021 - Precise ages for lode gold mineralization in the Xiaoqinling gold field, southern margin of the North China Craton: new constraints from in situ U-Pb dating of hydrothermal monazite and rutile: in    Econ. Geol.   v.116, pp. 773-786. doi:10.5382/econgeo.4800.
Liu, J.-W., Li, L., Li, S.-R., Santosh, M. and Yuan, M.-W.,  2022 - Apatite as a fingerprint of granite fertility and gold mineralization: Evidence from the Xiaoqinling Goldfield, North China Craton: in    Ore Geology Reviews   v.142, 12p. doi.org/10.1016/j.oregeorev.2022.104720.
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Porter GeoConsultancy Pty Ltd (PorterGeo) provides access to this database at no charge.   It is largely based on scientific papers and reports in the public domain, and was current when the sources consulted were published.   While PorterGeo endeavour to ensure the information was accurate at the time of compilation and subsequent updating, PorterGeo, its employees and servants:   i). do not warrant, or make any representation regarding the use, or results of the use of the information contained herein as to its correctness, accuracy, currency, or otherwise; and   ii). expressly disclaim all liability or responsibility to any person using the information or conclusions contained herein.

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