The SYGT has a old geological and tectonic history, with a double-layer structure composed of a lower basement and overlying cover (Han et al., 2014). The basement consists of the middle–lower Proterozoic Kunyang Group (1,800–1,000 Ma) and Dahongshan Group (2,500–1,800 Ma) (Fang, 2014) formations. Among them, shallow-marine carbonate-dominated and fluvial siliciclastic-dominated rock formations dominate the low-grade metamorphic greenschist-facies Kunyang Group (Greentree et al., 2006; Han et al., 2006). The cover is composed of upper Proterozoic, Upper Sinian (850–700 Ma) (Fang, 2014), and Palaeozoic strata. Upper Proterozoic rocks include a Lower Sinian igneous suite of mainly volcanic rocks and the Upper Sinian Dengying Formation of marine dolomite. Palaeozoic strata are comprised of Middle–upper Devonian, Carboniferous, and Permian rocks (Liu and Lin, 1999). The Sinian, Devonian, Carboniferous, and Permian carbonates are the primary host rocks of the Zn–Pb deposits. In these strata, the lower Carboniferous Baizuo Formation (Fm.; C₁ b), upper Devonian Zaige Fm. (D ₃ zg), and Upper Sinian Dengying Fm. (Zbd) carbonates are the most important host rocks. In the Huize district, argillaceous dolomitic limestone intercalated with thin-layered barite-bearing evaporite in the middle parts of C₁ b is lithologically similars to the wall rocks of the MVT deposits. Therefore, we presume that the Huize district was situated within a lagoonal environment and positioned between tidal flat and inter-beach environments in a region of extensive marine sedimentation during the Carboniferous Period. Ore host rocks in other districts of the SYGT formed in similar sedimentary environments. The exposed late Permian Emeishan basalts are the only igneous rocks in the SYGT.

We note that the middle–upper parts of C₁ b and D ₃ zg mainly consist of greyish-white, yellowish-red, cream-coloured, and coarse crystalline dolomite, whereas its middle–lower parts are mainly composed of compact light grey massive limestone and argillaceous dolomitic limestone. When comparing the compressive and shearing strength, dolomite in the middle–upper strata is noticeably weaker than limestone in the middle–lower strata. The strength of parallel bedding directions is significantly lower than that of the vertical bedding directions, which more easily results in interlayer faults within the dolomite (Han et al., 2001b). Consequently, ore-controlling interlayer fault zones likely formed in specific positions within the dolomite. Here, Zn–Pb deposits with dolomite and limestone-bearing dolomite in the Dengying and Maokou Fms. Are similar in their mechanisms.

Based on structural geological mapping (Figure 1) (Han et al., 2007a; Han et al., 2012b; Han et al., 2014), an analysis of seismic exploration data (Figure 2), and ore-field structural research, we can show that the intracontinental strike-slip tectonic classification system controls SYGT mineralisation in different areas; that is, the deposit concentration districts, ore deposits (ore-field), and ore-bodies (veins). At a regional scale, the strike-slip fault-fold group controls the SYGT mineralisation area, including the Zn–Pb polymetallic deposit concentration districts, such as the NE Yunnan (NEYD), NW Guizhou (NWGD), and SW Shichuan Deposit (SWSD). The NE-trending oblique upward strike-slip belts control the NEYD, the NW-trending diagonal fall strike-slip belts control the NWGD, and the north–south-trending sheer fault belts control the SWSD. At the ore district or smaller scales, a single strike-slip fault-fold structure may control an ore-field or deposit while secondary fault zones or their assorted components may control the ore-bodies or veins.

In the NEYD, there are eight oblique strike-slip belts that compose a NE-trending structural group (Han et al., 2007b; Han et al., 2012a) (Figure 1). These are the Xundian–Xuanwei, Dongchuan–Zhenxiong (also referred to as the Jinniuchang–Kuangshanchang belt in the Huize district), Huize–Yiliang, Ludian–Daguan–Yanjin, Qiaojia–Jinsha, Yiliang–Qujing, Luliang–Fuyuan, and Luoping–Puan belts. Just as the Dongchuan–Zhenxiong belt controls the Zn–Pb ore-field, composed of the Huize, Yulu, and Daibu deposits, the Qilinchang–Kuangshanchang and Yinchanpo oblique strike-slip structures control the Huize Kuangshanchang and Qilinchang large and Yinchangpo middle Zn–Pb districts (Han et al., 2007a; Han et al., 2012b; Han et al., 2015) (Figure 1). Secondary NE interstratified compression-shear faults in altered dolomite zones of the upper plate of the Kuangshanchang–Qilinchang–Yinchnagpo fault directly control the rich and thick ore-bodies (Han et al., 2012a; Han et al., 2014). The Huize–Niujie belt controls the Maoping Zn–Pb district, which is composed of the Fangmaba, Maoping, and Tuogumei deposits (Han et al., 2012b). These NE-trending oblique strike-slip belts have developed into a complicated ore-controlling system, which has been documented as a typical xi-type structural tectonic pattern (Han et al., 2001a; Han et al., 2006).

The structural system of the NEYD is composed of major components, including NE-trending anticlines with sinistral ore-bearing interstratified faults (which control the Huize, Maoping, Fule, and Maozu deposits, among others), as well as other assorted components, including NW-trending high-angle tension-shear faults and SN-, NNW-, and EW-trending shear faults. The average orientation of the principal compressive stress axis (σ ₁) was NW–SE during the Zn-Pb mineralisation period. The NE-trending folds and sinistral compression-shear faults were the main conduit structures of the ore-forming fluid migration while the NW-trending tension-shear faults were ore-matching structures. The lower-order NE-trending interstratified fault zones were also the main ore-allocation or ore host structures and appear as an echelon fracture group, identified as xi-type structures (on a plane) or stepped-type (along profile) ore-controlling structures (e.g., the Huize and Maoping deposits) (Han et al., 2012a; Han et al. 2014; Han et al. 2015).

There are four strike-slip fault belts in the SWSD, establishing a SN-trending structural group, including the Xichang–Huili–Yimen, Xiangluoshan–Ningnan, Hanyuan–Leibo–Qiaojia, and Shimian–Huidong belts. The Xichang–Huili–Yimen belt (Han et al., 2014) (Figure 2) controls the Tianbaoshan Zn–Pb-(Cu) Zn–Pb deposits, among others.

There are also two diagonal tensile strike-slip fault-fold belts in the NWGD, making up a NW-trending structural group, including the Weining–Shuicheng and Yadu–Mangdong belts (Figure 2) (Han et al., 2014). The former controls the Qingshan, Shanshulin, and Shangshiqiao medium-sized deposits while the latter controls the Zhugongtang super large-sized deposit and a series of medium-sized deposits, including the Yadu, Xiaojiwan, Zazichang, Maomaochang, and Tianqiao deposits (Figure 1).

There are up to 52 igneous outcrops of intermediate to basic-ultrabasicity rocks along the NS-trending Xiaojiang fault zone of the SYGT (Yuan et al., 1985b; Song et al., 2001). There is, however, only one location where pyritised ultramafic rocks supported Pb and Zn mineralisation. These diabase and gabbro-diabase sills and dikes (K–Ar ages: 246–283 Ma) lie on the eastern side of the Xiaojiang fault (Liu and Lin, 1999). Certain diabase contact zones experienced intense hydrothermal alteration (e.g., silicification and epidotisation) and Pb, Zn, and Cu mineralisation.

Late Permian Emeishan basalt (K–Ar ages: 218.6–253.3 Ma; Zircon U–Pb age: 258.6 Ma) (Yuan et al., 1985a; Cong, 1988; Zhou et al., 2002; Guo et al., 2004; Zhong and Zhu, 2006; Zhou et al., 2006; Tao et al., 2009) is vital when attempting to understand local magmatic activity. The basalt may spatially coincide with Zn–Pb-(Ag–Ge) deposits and ore occurrences (Figure 1), but is not related to Zn–Pb metallogenesis (Han et al., 2012b).

This district, which is one of richest super-large rich Ge–Ag-bearing Zn–Pb deposits worldwide and typical of the NEYD (Figure 1; Table 1), is situated at the eastern side of the Xiaojiang fault belt and comprised of the Kuangshanchang, Qilinchang, and Yinchangpo deposits, located 40 km from Huize town, which has supported mining in both ancient and present times (Han et al., 2006). Numerous advances have occurred, especially in terms of deposit geology (Liu and Lin, 1999; Han et al., 2006; Han et al. 2007b; Han et al. 2012a; Han et al. 2014; Han et al. 2015; Han et al. 2016). Therefore, we focus on the characteristics of the tectonic mineralisation and alteration, which have received less attention in previous studies.

The Huize Zn–Pb ore district controlled by the NE-trending Dongchuan–Zhenxiong oblique strike-slip belt tectonically, which resulted from sinistral shear of the Xiaojiang fault, while the Maoping–Qujing concealed the fault during the Indosinian orogeny period (Figure 1). In general, deposits in this district are controlled by NE-trending Kuangshanchang, Qilinchang, and Yinchangpo fault-fold structure series, as confirmed by magnetotellurics exploration (Figure 2B) and ore-forming structural analysis (Figure 3).

The major faults in the NEYD have experienced multiple movements and are spatially related to the Zn–Pb-(Ag–Ge) ore-bodies (Han et al., 2015). There are five orientation faults in the district: the NE-, NW-, NNW-, ‘north–south-, and east–west-trending faults. From the late Permian to Middle–Late Triassic, crustal movements changed from extension to compression strike-slip. The north–south-, NE-, and NW-trending tectonic zones formed during the Triassic Indosinian orogeny period (230–200 Ma).

The NE-trending ore-controlling faults led to the development of various types of tectonites, including clastic, clast-porphyritic, mylonite, and cataclastic tectonites with different textures (Figure 3). For example, the Qilinchang fault zone developed Zn–Pb mineralised tectonic lenticels and foliated cataclastic belts, which led to widespread hydrothermal alteration of ferrous dolomitisation and pyritisation (Figure 4). In contrast, other trending faults are mostly associated with a single type of tectonite (i.e., mainly cataclastic). NE-trending ore-bearing interlayer fractures result in SW-trending lateral dip of the orebody group.

Hydrothermal alteration results in an intense water-rock reaction along ore-controlling fault zones. As shown in Figure 4, across the ore-controlling oblique fault zone upward to the ore-hosting rocks, mineral assemblage zoning and alteration shows that associations of alteration and mineralisation occur in the following order: barite + pyrite + quartz zone in the Kuangshanchang fault → weakly dolomitised limestone zone (VIII) → net veined coarse-grained dolomite with residual calcitised fine-crystalline calcareous dolomite zone (VII) → reddish medium-coarse crystalline dolomite zone (VI) → beige pinhole-like coarse crystalline dolomite zone (V) → grey coarse-grained dolomite zone (IV) → star-like Zn–Pb and pyrite-mineralised porous coarse crystalline ferro-dolomite zone (III) → (lower surface of interlayer fault belt) Zn–Pb mineralised pyrite zone (II) → (Zn–Pb ore zone (I1; dark grey sphalerite + densely disseminated pyrite zone → sphalerite + galena + pyrite ore zone) → fine-grained pyrite + dolomite + calcite in coarse crystalline dolomite zone (I2; upper surface of interlayer fault belt) → grey-beige impregnated pyritisation hole and pinhole with coarse crystalline ferro-dolomite zone (III–V) → coarse-grained dolomite with small residual limestone zone (VI, VII).

The Maoping district, which is also one of the super-large rich Ge-Ag-bearing Zn–Pb deposits and typical of the NEYD, lies on a structural junction between the NE-trending Huize–Niujie oblique strike-slip fault-fold belt and NW-trending Yadu–Mangdong fault belt (Figure 1; Table 1). This district is composed of the Maoping super-large deposit (controlled by the Maoping fault-fold structure), the Fangmaba small-sized deposit (controlled by the Fangmaba -fold structure), and the Yunluheba medium-sized deposit (controlled by the Daibu fault-fold structure). The primary strata in the district are Devonian, Carboniferous, and Permian. The Proterozoic Kunyang Group is the unexposed base in the district.

Multiple ore-hosting strata, including the Zaige Fm. Of the upper Devonian (D₃ zg) and Baizuo (C₁ b) and Weining Fms. (C₂ w) of the lower–upper Carboniferous, are the typical feature of this deposit. These strata are mainly composed of greyish to white, pinkish, and cream coarse crystalline dolomite; light grey compact massive limestone; and siliceous limestone. The ore-bodies are distributed along the northwest plunging wing of the Maomaoshan overturned anticline, and controlled by the interstratified fault zones which result in SW-trending lateral dip of the orebody group. In this district, the only igneous rock is the upper Permian Emeishan basalt.

The ore-body shapes vary with their spatial distributions, which include large vein, chamber, lenticular, and stratiform shapes, with continual expansion and contraction (Figures 5A,B). The ore grades of Pb and Zn in the Noes. One and six ore-body groups are high (up to 25%–30%), mostly occurring as compact massive ores. In the No. Two and No. Three ore-body groups, the ore grades of Pb and Zn are up to 15%–20%. In addition to being rich in Pb and Zn, the Ag grade can reach 495.6 ppm. The ores also contain other dispersed elements, including Ge (≤203 ppm) and Cd (≤735.5 ppm; Table 1). The mineral composition includes sphalerite, galena, pyrite, ferro-calcite, calcite, and dolomite in the sulphide ores, with minor proportions of quartz and barite. The bead-like and columnar ore-bodies occur at full thicknesses in flat fault areas and thin thicknesses along steep faults, stably extending to an elevation of −38 m (Figures 7, 8). Ore-forming processes have been divided into the hydrothermal ore-forming period (including pyrite-sphalerite, sphalerite-galena-pyrite, and calcite-pyrite stages) and the epigenesis period (Han et al., 2007b). Mineral zoning and alteration from ore-bodies to wall rocks occurs in four parts (Figure 5C): Zn–Pb ore zone (net vein and dense, massive Pb-Zn ore zone) → ore-nearing zone (pinhole with coarse crystalline dolomite zone with strong ferrous dolomitisation-pyritisation) → transitional zone (coarse crystalline dolomite zone with strong dolomitisation and calcitisation) → peripheral zone (fine-crystalline dolomite zone with calcitisation).

The Daliangzi district, which is one of the large Zn–Pb deposit and typical of the SWSD, is located in the NWW–EW-trending right-hand strike-slip fault-fold zone between the near north–south-trending Xiaojiang deep fault and the Puduhe deep fault in the ore concentration area of Southwest Sichuan (Figure 6A). The primary strata in the district are dolomite of the Dengying Fms. (Zbd; Sinian), sand shale of the Qiongzhusi Fms. (∈₁ q; lower Cambrian), and epimetamorphic rock series of the Mesoproterozoic basement Huili Group (Pth). There is a parallel unconformity contact relationship between the Qiongzhusi and Dengying Fms., and unconformity contact relationship between the shallow metamorphic rock series of the Huili Group and overlying Neoproterozoic Lower Sinian carbonate rock series. The ore deposit is obviously controlled by a structural and lithologic combination. The NWW–EW-trending main faults (e.g., F15, F1 and their derived NW-trending faults such as F5, F6, F8 and F9) control the shape and occurrence of the ore-body group; the main host rocks are siliceous dolomite and phosphorous dolomite of the Dengying Fm. (Sinian system), and the upper strata are calcareous fine sandstone, siltstone, and a thin layer of lower Cambrian marl (Figure 6A).

The deposit is composed of the No. 1 and No. 2 ore-body groups; the No. 1 main ore-body group is divided into five blocks (I–V). The ‘black fracture zone’controlled by the F6N and F6S faults divides the main ore-body group into two parts (Figure 6B). The ore block thickness and ore grade in the northeast panel are significantly higher than those in the southwest panel. The ore-bodies in the northeast panel are funnel-shaped (Figure 6C), and are mainly composed of high-grade massive and breccia ores. The ore bodies in the southwest panel have the characteristics of “small in the upper part and large in the lower part” (Figure 6D), and are mainly composed of low-grade vein, fine net vein, and breccia ores. The network vein is the major type. The ore-body strikes the NWW–EW-trending fault, with a length of more than 630 m, inclines to the NE or SW (locally), and has a steep dip angle (>75°). The thickness of the ore body is 0.81–169.79 m (average 52.67 m), and the average grades of Pb and Zn are 0.70% and 10.50%, respectively. The ore structures are mainly massive, brecciated, disseminated, veins and veinlets. The ore minerals are mainly sphalerite, followed by galena. There are also oxide minerals such as plumbite, bauxite, chlorophosphonite, smithsonite, hemimorphite, hydrozinite and sillimanite, along with minerals such as pyrite, chalcopyrite, and Malachite. Gangue minerals are mainly dolomite, calcite, and quartz, followed by sericite, kaolinite, collophanite, chalcedony, barite, and graphite. The main wall rock alteration types include silicification, carbonation, pyritisation, and carbonation. Among them, silicification is mainly represented by vein and disseminated quartz; pyritisation is mainly represented by disseminated and veinlet fine-grained pyrite; carbonation is mainly vein and disseminated calcite and dolomite; carbonatisation is mainly characterised by asphalt and carbonisation, which is widely developed in the’black fracture zone’and the strata fissures of the upper and lower walls of ore the body.

According to the characteristics of vein interpenetration, different altered mineral assemblages, and ore fabrics, the metallogenic process of the deposit can be divided into a hydrothermal metallogenic period and supergene stage. The hydrothermal mineralisation period can be divided into three stages: i. A quartz-pyrite stage, characterised by quartz vein and agglomerate pyrite; ii. A sphalerite-galena-pyrite polymetallic sulphide stage, for which the main ore minerals are sphalerite, galena, pyrite, and smaller amounts of chalcopyrite, tetrahedrite. Gangue minerals are calcite, dolomite, asphalt, etc.; sphalerite is light yellowish brown to orange red, with a euhedral granular structure, and both vein and colloidal structures; galena is common in edge structures with chalcopyrite and tetrahedrite; and iii. Carbonate stage, for which the main minerals are sphalerite, dolomite, calcite, and pyrite; sphalerite is light brown yellow. At a depth of 1,944 m, the homogenisation temperatures of fluid inclusions of sphalerite and calcite for the main metallogenic stage are 146.3°C–288.5°C, with an average of 186.8°C; the salinity is 5.3–18.8 wt% NaCleq., with an average of 11.3 wt% NaCleq. depos

Qingshan deposit is a typical middle-sized deposits of the SW wing of the Weining–Shuicheng anticline in the middle of the Weining–Shuicheng Pb-Zn sub-metallogenic belt in NWGD. The main exposed strata in the mining area (Figure 7A) are dolomitic limestone of the Baizuo Fms. (C₁ b; lower Carboniferous), limestone of the Huanglong Fms. (C₂ h; upper Carboniferous), limestone of the Maping Fms. (C₂ mp; upper Carboniferous), argillaceous sandstone, carbonaceous shale and inferior coal of the Liangshan Fms. (P₂ l; Middle Permian), and marlite of the Yangxin Fms. (P₂ y; Middle Permian). Among them, the crystalline limestone of the Maping formation is the main host rock of the deposit. The main fold structure is the Weining–Shuicheng anticline, which is a tight long axis fold with a NW-trending axis. There are two main groups of NW- and NE-trending faults; north–south trending faults are rare (Figure 1A). Hercynian diabase dikes are also exposed in the mining area, which has only a spatial relationship with Pb–Zn mineralisation.

The deposit is mainly composed of the No. 13, 14, and 15 rich Pb-Zn ore bodies, and the average grade of Pb and Zn is >30%. Among them, the No. 13 ore-body is 20–70 m long, with an average thickness of 32.10 m, and a dip extension depth of ∼145 m; the average thickness of the No. 14 ore-body is 2.6 m, and the extension depth is >40 m; the length of the No. 15 ore-body is 42 m, the average thickness is 6.28 m, and the extension depth is >15 m. The ore-bodies are mainly distributed in the interlayer fault zone at the footwall of the F1 and F2 faults with a steep NW dip (Figure 7B). The strike of the ore-bodies is NW at 47°–70° with a SW dip, and is flanked by SE. The extension direction of the main ore-body is roughly the same as that of the NW-trending ore-hosting strata. The main ore-body appears in the form of sacs, blocks, breccias, and veins. The ore is mainly composed of galena, sphalerite, pyrite, calcite, barite, and a small amount of dolomite. They have euhedral subhedral and metasomatic residual structures and massive, stellar, breccia, disseminated, veinlet, and banded structures. The wall rock alteration is weak, only pyritisation, calcitisation, and baritisation are found. From the ore-body to the crystalline limestone, the mineral assemblage zoning of sphalerite + galena → pyrite + calcite is presented in turn. To date, the Pb-Zn metal reserves of the deposit are estimated to be> 300,000 tonnes. In recent years, stratoid rich and thick ore-bodies have been found on the side of F2 fault. Ore bodies are also found at 1,500 m depth in drilling holes within the Laoyingyan ore block, with a Pb-Zn grade of >30%. It is speculated that the deposit extends over a larger scale than currently recognised.

The homogeneous temperatures and salinities of the mineral fluid inclusions in typical MVT deposits are approximately 90°C–150°C and 10–30 wt% NaCl eq., respectively (Basuki and Spooner, 2002; Leach et al., 2005). In contrast, the homogeneous temperatures of fluid inclusions from deposits in the SYGT are significantly higher. Higher ore-forming temperatures and medium salinities have been reported in the Huize and Maoping districts. Under conditions of no pressure correction, calcite fluid-inclusion data indicate that ore fluids had homogenisation temperatures of 183°C–223°C, with salinities reaching 13–18 wt% NaCl eq. However, brown sphalerite fluid-inclusion data, obtained via infrared micro-thermometry, show homogenisation temperatures of 250°C–355°C (without pressure correction) for salinities of ∼1.8–4.0 wt% NaCl eq. (Han et al., 2007a; Han et al., 2016).

The fluid-inclusion types of two liquid-vapour phases (L_H2O +V_H2O) and a pure liquid phase (L_H2O) are similar to those from the MVT fluids (Huang et al., 2019a). Besides, there is also a pure vapour phase (V_H2O), three phases with a seed crystal (S + L_H2O +V_H2O), a CO₂-containing immiscible (V_CO2 + L_CO2 + L_H2O) fluid phase, and gas components that include CO₂, CH₄, and N₂ in the deposits throughout the SYGT area (Han et al., 2004; Han et al., 2007a). These characteristics differ from those of the MVT Zn–Pb deposits, showing that the immiscible processes and boiling of ore-forming fluids are the important ore-forming mechanisms in the mineralisation process for the Zn–Pb deposits in the SYGT (Figures 8A,B).

The sulphur isotope composition δ³⁴S_CDT values range from +5‰ to ∼+15‰ for the deposits in the SYGT, which indicates that the sulphur originates from the strata, whereas δ³⁴S_CDT values in most MVT deposits (−39‰ to −34‰) show that sulphate primarily originates from the ocean (Figure 9). The C–H–O isotopes are complicated and their compositions in the SYGT deposits differ from those in the MVT deposits (Figure 10). Hydrogen and oxygen isotopes can effectively identify the ore-forming fluid source (Huang et al., 2019b). Zhang et al. (2017a) identified the two different metallogenic fluids by C-H-O isotope: a high temperature, low salinity, and acidic Fluid A, which originates from deep-seated fluids and is enriched in lighter C - O-H isotopes (−3‰ < δ¹³C‰ < −4‰; 10‰ < δ¹⁸O‰ <17‰; −92‰ < δD‰ < −50‰), and a low temperature, high salinity Fluid B, which is a subsurface brine formed by atmospheric precipitation. Fluid B is characterized by heavier C–O–H isotopic compositions (−2‰ < δ¹³C‰ < 1‰; 2‰ < δ¹⁸O‰ < 24‰; −66‰ < δD‰ < −43‰) than Fluid A and cycles continuously within the strata. By combining analyses of Sr-Nd-Pb tracers, Han et al. (2004; Han et al., 2007b) stress that the ore-forming elements in the deposits mainly derive from the folded Mesoproterozoic basement. The metallogenic fluid is a mix of a deep-origin fluid and basin fluid (Zhang et al., 2017b). The isotopic statistical data indicate that the initial value of mixed Sr in the ores (i.e., ⁸⁷Sr/⁸⁶Sr = 0.7114) is a deep basement signature.

Based on comprehensive analyses of the SYGT, as presented in the previous sections, we can summarise the typical geological characteristics of the deposits with the following eight main points.

1) High grade (Rich): The average grade of the Zn–Pb ores in the deposits is high (mostly Pb + Zn ≥ 20%–35%, even reaching 50%), far exceeding the typical grade in MVT Zn–Pb deposits (normally ∼3%–10%) (Leach et al., 2005).

Ore deposits controlled by oblique strike-slip structural belts. The mechanical and kinematic characteristics of differently trending faults in the different district result in different ore-body locations and lateral orientations.

All NE-trending compression-shear ore-bearinging interlayer fractures distinctly show sinistral transpressional movement features in the NEYD, where ore-bodies occur in the upper plate of major ore-controlling faults in the structural belts (Han et al., 2012a; Han et al., 2015), and resulted ore bodies to bend sideways towards SW-trending direction.

NW-trending tension-shear ore-bearing faults distinctly show right-hand transpressional movement characteristics in the NWGD, where vein ore-bodies mainly occur in the Yadu–Mangdong fault belt (e.g., the Zhugongtang deposit). Certain ore-bodies occur in the lower plates of the Weining–Shuicheng major faults (e.g., the Shanshulin, Qingshan, and Tianqiao deposits), and resulted ore bodies to bend sideways towards SE-trending direction.

The NWW-near EW-trending primarily shear ore-controlling faults between the Xiaojiang north–south-trending deep fault and the Puduhe fault distinctly show left-hand shear movement characteristics in the SWSD, and resulted ore bodies to bend sideways towards E or SEE-trending direction. There is a close relationship between strike-slip faults and folds dragged by faults (Han et al., 2012b). These situations reflect identical characteristics within the NW–SE-trending compressing stress processes during the metallogenic period. In addition, all boundaries between the ore-bodies and wall rocks are distinct (Han et al., 2007b; Han et al., 2012a), showing that ore-forming fluids may have been injected into fractures, possibly resulting in the rapid precipitation of metal sulphide.

Numerical simulations have shown that large amounts of Zn and Pb metal can migrate through a chlorine complex. Physical chemistry phase diagrams indicate a lower pH, higher solubility, and enhanced ability to transport metals (Zhang et al., 2020). Moreover, hydrolysis experiments (Zhang et al., 2019a) indicate that a pH of less than four is a favourable condition for transporting a large number of metals. Precipitation experiments show that an increase in the pH can promote the precipitation of Pb-Zn sulphides, boiling affects the formation of ores at certain high grades, and mixing effects yield precipitation and mineralisation. The fluid inclusions, temperature measurements (Table 3), and isotopic compositions reveal the mixing of two fluid types (Zhang et al., 2017b).

Combined with the ore-forming conditions, the metallogenic theory of the Huize-style deposits (Han et al., 2014), and experimental geochemical research (Zhang et al. 2019a-Zhang et al., 2019b), the major controlling factors of the Zn and Pb supernormal enrichment mechanisms include the physicochemical conditions (e.g., pH value) in the hydrothermal system, adequate ore sources, boiling and mixing effects, and a strong tectonic driving force. As Table 3 summarises the physicochemical conditions of the ore-forming fluid and ore deposition in the Huize and Maoping Zn–Pb deposits, we observe that the original fluids had medium and high temperatures under acidic conditions, such that Pb and Zn ions were able to migrate as chloride complexes [i.e (PbCl₄)^2– and (ZnCl₄)^2–]. When fluids flowed past the carbonate rocks and temperatures dropped to ∼200°C, the neutralisation reaction led to the precipitation of metal sulphide. In summary, large-sized and super-large-scale rich Zn–Pb deposits formed in these conditions, which are favourable for a metallogenic tectonic setting, abundant mineral resources and fluids, a strong driving force (in terms of the strike-slip structure, superior storage space, strong decompression boiling, and mixing), ‘injection’, and replacement of the mixing fluid.

Based on the above comparison with respect to the typical geological and geochemical characteristics of Zn–Pb deposits in the SYGT and typical MVT deposits (Table 4), the metallogenic regularities of the deposits can be described in terms of the three following ore-forming factors: i) a strike-slip structure ore-controlling system, ii) typical mineral assemblages, and iii) mineralisation alteration zoning and a metallogenic acid–alkali geochemical barrier. Table 4 indicates that these deposits differ from the MVT deposits in terms of the metallogenic geological bodies, ore-forming structures, ore-forming fluid features, and ore-forming regularities.

According to the classic theory, MVT-type Pb-Zn deposits mainly form in cratonic carbonate platform and continental extensional environments, and in weakly deformed and stable carbonate platforms controlled by normal faults (Leach and Sangster, 1993).

The essential characteristics of MVT-type Pb-Zn deposits are epigenetic mineralisation; ore-bearing diagenetic carbonates (reef-limestone assemblages); no genetic relationship with magmatic activity; mainly Pb-Zn sulphide compositions; locations in the peripheries of cratonic platforms, foreland basins, and rift basins; related to basin fluids, ore-controlling normal faults, fissures, and karst caves; and low-temperature and high-salinity fluids (Leach and Sangster, 1993; Leach et al., 2001). Although some scholars have classified epigenetic hydrothermal deposits un-magma under different ore-controlling tectonic settings as MVT type deposits (Leach and Song, 2019), classic MVT theory cannot explain the formation mechanism of the Ge-rich Pb-Zn deposits in the SYGT area

Deposits in the SYGT area are the result of multiple geological effects, including strike-slip fault-fold structure trapping, rich mineral fluids, superior ore storage, fluid immiscibility, and mixing processes. These deposits are, therefore, particular to this region (Table 4). Based on the following four factors, we propose a new Huize-style Pb-Zn deposit, which is different from the classic MVT deposit (Han et al., 2012a; Han et al., 2014). First, in the metallogenic tectonic settings of Pb-Zn deposits in the SYGT, the main ore-controlling factors, mineralised alteration zoning laws, lateral plunging law of ore-bodies, ore-forming physicochemical conditions, geochemical characteristics, metallogenic mechanisms, and prospecting methods are all different from classic MVT deposits, such as the Huayuan Pb-Zn deposit distributed in the SE side area of the Xuefengshan tectonic belt in southwestern Hunan. Second, and more importantly, the prospecting investigation methods, used with respect to the MVT deposits and to the Huize-style deposits are markedly different. Third, this type of deposit was first discovered in the Huize Pb-Zn mine of Yunnan province along the SW margin of the Yangtze Continental Block. From a mining perspective, this deposit has been well known since ancient times because of its unique mineralisation characteristics (Han et al., 2012b). Fourth, certain deposits globally also show identical ore-forming features and metallogenic structural settings to the Huize-style deposits; for example, the La Calamine Zn–Pb deposit (Coppola et al., 2008), Iran’s rich Zn–Pb deposit, and a series of large–super large Zn–Pb deposits in the Sanjiang area of the Tethys metallogenic belt. For example, the eastern Dongmozazhua Zn–Pb deposit in the Sanjiang metallogenic belt along the NE edge of the Qinghai-Tibet plateau belongs to the orogenic-type Zn–Pb-Ag–Cu (Hou et al., 2008) and MVT-like Zn–Pb deposits (Liu, 2012). These deposits are similar to the Huize-style Zn–Pb deposits in terms of their continental collision and orogeny backgrounds, where they were controlled by an oblique-slip structure. This also reflects the universality of the Huize-style deposits internally and abroad.

Based on the typicality of the Huize Zn–Pb deposits and the universality of the metallogenic features of this deposit type across the SYGT (Han et al., 2004; Han et al. 2006; Han et al. 2007a; Han et al. 2012b), new Huize-style Zn–Pb deposits have been proposed as a style of epigenetic Zn–Pb deposit. This deposit is named for the Huize ore district, which has had a strong association with mining in both ancient and modern times (Han et al., 2006). These deposits in the SYGT area are dominated by hydrothermal metasomatism against an intracontinental strike-slip tectonic background. The deposits formed from metallogenic fluids with medium–high temperatures (≥200°C–350 °C), low–medium salinity, and a CO₂-rich gas phase or gas-liquid-phase. These deposits ascended and injected into the fracture zones, such that they are mainly hosted by hydrothermal metasomatic carbonates. The conceptual model of ore deposit genesis sees Han et al. (2022).

The classification of Zn–Pb deposits has posed a significant problem for prospecting predictions (Han et al., 2012a; Ye et al., 2017). Although the characteristics of the Huize-style deposits are different from those of the typical MVT deposits in terms of their tectonic setting, main ore-controlling factors, ore structures, physical-chemical conditions, and metallogenic models, among other factors (Table 4), the Huize-style deposits are representative of a new Pb-Zn deposit type, which is not contradictory to MVT deposits. We suggest that Huize-style deposits and typical MVT deposits are members of carbonate-hosted epigenetic hydrothermal-type Zn–Pb deposits of a non-magmatic origin, and constitute two unit-deposit types of the overall CNHT Zn–Pb deposits. Numerous deposits are characterised as a transitional type between the two (e.g., the Fankou super-large Zn–Pb deposit in eastern Guangdong).

The authors believe that the classification of deposit types is not only of theoretical significance, but also of the most important significance in guiding the exploration practice and prospecting deployment. The prospecting methods associated with the Huize-style deposits are different from those of typical MVT Pb-Zn deposits. Tectonic ore-control exploration techniques dominate the prospecting exploration of Huize-style deposits, such as ore-field structural analysis (Wang et al., 2020), tectono-geochemical exploration (Han et al., 2015), tectonic-altered rock facies measurements (Han, 2017; Wang et al., 2019), tunnel gravity exploration (Han et al., 2020), and electromagnetic detection (Han et al., 2019a). However, combinations of strata and lithology, with certain exploration techniques, such as ore-bearing sedimentary facies analysis, basin structure analysis, and geochemical exploration, dominate explorations of classic MVT deposits.