Geofluids

Geofluids / 2020 / Article

Research Article | Open Access

Volume 2020 |Article ID 7352821 | https://doi.org/10.1155/2020/7352821

Xinglin Chen, Yongjun Shao, Chunkit Lai, Cheng Wang, "Genesis of the Longmendian Ag–Pb–Zn Deposit in Henan (Central China): Constraints from Fluid Inclusions and H–C–O–S–Pb Isotopes", Geofluids, vol. 2020, Article ID 7352821, 21 pages, 2020. https://doi.org/10.1155/2020/7352821

Genesis of the Longmendian Ag–Pb–Zn Deposit in Henan (Central China): Constraints from Fluid Inclusions and H–C–O–S–Pb Isotopes

Academic Editor: Micòl Mastrocicco
Received18 Aug 2019
Revised16 Jun 2020
Accepted25 Jun 2020
Published13 Jul 2020

Abstract

The Longmendian Ag–Pb–Zn deposit is located in the southern margin of the North China Craton, and the mineralization occurs mainly in quartz veins, altered gneissic wallrocks, and minor fault breccias in the Taihua Group. Based on vein crosscutting relations, mineral assemblages, and paragenesis, the mineralization can be divided into three stages: (1) quartz–pyrite, (2) quartz–polymetallic sulfides, and (3) quartz–carbonate–polymetallic sulfides. Wallrock alteration can be divided into three zones, i.e., chlorite–sericite, quartz–carbonate–sericite, and silicate. Fluid inclusions in all Stage 1 to 3 quartz are dominated by vapor-liquid two-phase aqueous type (W-type). Petrographic and microthermometric analyses of the fluid inclusions indicate that the homogenization temperatures of Stages 1, 2, and 3 are 198–332°C, 132–260°C, and 97–166°C, with salinities of 4.0–13.3, 1.1–13.1, and 1.9–7.6 wt% NaCleqv, respectively. The vapor comprises primarily H2O, with some CO2, H2, CO, N2, and CH4. The liquid phase contains Ca2+, Na+, K+, SO42−, Cl, and F. The sulfides have to +2.35‰ and to 38.795, to 15.686, and to 18.101. The H–C–O–S–Pb isotope compositions indicate that the ore-forming materials may have been derived from the Taihua Group and the granitic magma. The fluid boiling and cooling and mixing with meteoric water may have been critical for the Ag–Pb–Zn ore precipitation. Geological and geochemical characteristics of the Longmendian deposit indicate that the deposit is best classified as medium- to low-temperature intermediate-sulfidation (LS/IS) epithermal-type, related to Cretaceous crustal-extension-related granitic magmatism.

1. Introduction

The Longmendian Ag–Pb–Zn deposit is located in the Shagou (Xiayu) orefield of the Xiong’er region (western Henan Province) in central China. Tectonically, the deposit is located at the southern margin of the North China Craton (NCC), bordered with the eastern Qinling–Dabie Orogen. The NCC is one of the world’s oldest craton, with a history dating back to >3.8 Ga. It is also an important mineral province, hosting a variety of ore deposits [1, 2]. The Mesozoic granites and hydrothermal mineralization systems in the Xiong’er region (southern NCC margin) have been widely studied [311]. The regional Au and Mo mineralization was coeval with the first Mesozoic magmatic phase there (late Jurassic-early Cretaceous, ca. 158–136 Ma), which was related to the Paleo-Pacific plate subduction beneath Eastern China [1]. Meanwhile, Ag–Pb–Zn mineralization was mostly coeval with the second magmatic phase (early Cretaceous, ca. 134–108 Ma) [1214], which is related to lithospheric thinning–asthenospheric upwelling caused by the subduction-direction change of the Paleo-Pacific Plate [1, 2]. In addition, Neoproterozoic Mo mineralization was also reported locally, as represented by the Zhaiao and Longmendian deposits [15, 16].

The Longmendian Mo mineralization is spatially related to the migmatites but distal from intrusions or faults [17]. Four types of fluid inclusions (FIs) have been recognized in the Mo-bearing quartz and calcite grains, i.e., -bearing FIs (PC-type), CO2–H2O-bearing FIs (C-type), daughter mineral-bearing FIs (S-type) and H2O–NaCl FIs (W-type). The ore fluid temperature and pressure were estimated to be around 225 to 390°C and 114 to 265 MPa, respectively [17]. Geological and FI features indicate that the Mo mineralization, which was molybdenite Re–Os dated to be 1875 Ma, was caused by the high temperature migmatitic fluid/melt [1517]. The Paleoproterozoic mineralization event was interpreted to have linked to the collision between the western and eastern NCC along the Trans North China Orogen at 1.85 Ga [15, 16].

Meanwhile, Longmendian Ag-Pb-Zn mineralization is of a much larger scale than the Mo mineralization. The relationship between the Ag-Pb-Zn and Mo mineralization, as well as their respective ore material/fluid source and metallogenesis, remains unclear. In this study, therefore, we addressed these issues via FI microthermometric and H–O–C–S–Pb isotope analyses.

2. Regional Geology

The Xiong’er terrane is an important part of the Kunlun–Qinling–Dabie Orogen. The terrane, encompassing an area of 80 km long (E-W) and 15 km wide (N-S), is bound by the EW-trending Machaoying fault in the south and the Luoning fault in the north (Figure 1). Prolonged and multiphase intensive orogenic events have controlled the formation of the structural framework, magmatism, and sedimentation of the region, with consequently influenced the Xiong’er metallogeny. The regional tectonic events include the formation of the continental nucleus and then the cratonic basement in the Paleoproterozoic, Mesoproterozoic rifting, Neoproterozoic-to-Paleozoic sedimentation, and Mesozoic tectonic reactivation. The study area is located in the western Xiong’er (Figure 1).

Local stratigraphy is characterized by crystalline basement with metavolcanic-sedimentary cover. The crystalline basement is primarily composed of the Neoarchean Taihua Group (Gp) metamorphosed terrane, while the metavolcanic-sedimentary cover is composed of Mesoproterozoic Xiong’er Group (Gp.) low-grade metavolcanic rocks. The Taihua Group in the study area strikes ENE and is dominated by biotite/amphibole plagioclase interlayered with (plagioclase) amphibolite, granulite, and leptite. Regionally, the Xiong’er Gp. volcanic rocks overlie the Taihua Group along an unconformity, which was formed by the 1.85 Ga collision between the eastern and western NCC. The rock types of the Xiong’er Gp. consist of mainly (pyroxene) andesite porphyry with local siltstone-mudstone/shale interbeds.

Local structure is controlled by a series of NE-trending detachment faults along/around a metamorphic core complex, the most important of which lies on the unconformity between the Xiong’er Group and Taihua Group (Figure 2). The main detachment fault and the NE-trending shears are the major Ag-Pb-Zn ore-hosting structures [20]. Local folds include mainly the EW-trending recumbent-overturned folds and the NS-trending anticlines and synclines. The Machaoying fault is the major regional fault and is located in the southern Xiong’er. Faults/fractures are well developed in the study area and are mainly NE-trending and minor NW-trending and NS-trending. NE-trending structures are the main ore host.

In the study area, the widely exposed magmatic rocks were mainly formed in the Archean, Mesoproterozoic, and Mesozoic: Archean magmatic rocks include mafic to felsic volcanic rocks and late-stage ultramafic intrusions (e.g., dykes). The rocks are metamorphosed into gneiss, plagioclase amphibolite, and migmatite; Mesoproterozoic magmatic rocks comprise extensive intermediate-mafic volcanic rocks (ca. 1780–1320 Ma [21]) and the Xiong’er diorite in Songxian County (zircon U–Pb age: 1440 Ma [22]); Mesozoic magmatic rocks are widespread and multiphase. Their formation was primarily restricted largely to the Yanshanian (Jurassic-Cretaceous), although Indosinian (Triassic) one is also reported [23]. The Yanshanian magmatic rocks are mostly granite batholiths and minor granite stocks and medium-felsic dykes. Furthermore, numerous outcrops of small-sized explosive-breccias are observed and generally regarded to be closely ore-related [23]. The granite batholiths are distributed mainly in the eastern Xiong’er, e.g., the Huashan, Jinshanmiao, Wuzhangshan, and Heyu intrusions. Previous works indicated that Yanshanian magmatism may have facilitated extensive migration of metallogenic materials along/across the sequences and that the postmagmatic hydrothermal fluids constitute an important component of the ore fluids [24].

3. Deposit Geology

The Longmendian deposit is located to the west of the Xiong’er metamorphic core complex (Figure 3). The exposed metamorphosed sequences comprise primarily the Neoarchean Taihua Group and the Mesoproterozoic Xiong’er Group. The Taihua Group is distributed to the north of Longmendian and comprises dominantly biotite plagioclase gneiss and migmatized amphibole-plagioclase gneiss. The sequence is underlain by numerous amphibolite bodies. The Xiong’er Group is distributed to the southeast of Longmendian and comprises mainly andesite, particularly pyrite-bearing amygdaloidal and porphyritic ones. Andesitic rocks at Longmendian are generally altered, with the plagioclase strongly sericitized and the groundmass chlorite- and epidote-altered.

At Longmendian, detachment faults and secondary NE faults are the dominating structures, whereas folds are not well developed. The detachment faults strike NE with dip angles of 20–35°. The unconformity interface between the Taihua Group and Xiong’er Group is overprinted by slickensides of the detachment faults. The NE-trending (NW-dipping) faults, tectonic breccia, and mylonites are commonly altered. Magmatic rocks include mainly diabase and few ultramafic rocks. The diabase intruded into the Taihua Gp. sequence in the form of near-vertical dykes. The major minerals include pyroxene and plagioclase. The plagioclase phenocrysts (5–10 vol%) are commonly sericite- and epidote-altered, while the pyroxenes are generally altered to actinolite. Accessory minerals include ilmenite, magnetite, apatite, zircon, and ilmenite. Ultramafic dykes (100 m long and 10 m wide) are locally exposed to the north of Longmendian.

The orebodies are mainly of quartz vein and altered-rock types (Figure 4). Metallic minerals include primarily galena and sphalerite, followed by pyrite, chalcopyrite, Ag-bearing tetrahedrite, pyrargyrite, argyrite, polybasite, native Ag, tetrahedrite, and bornite. Nonmetallic minerals include primarily quartz, calcite, siderite, ankerite, fuchsite, and sericite, followed by feldspar, chlorite, amphibole, biotite, and apatite (Figure 4). Ore structures include mainly massive, vein/stockwork, banded, brecciated, and disseminated, while ore textures include (hyp)idiomorphic, xenomorphic granular, skeletal, rimmed, and zoned (Figure 4). Alteration types include silicic, sericite, chlorite, carbonate, and pyrite. Ore proximal wallrock alterations are dominated by silicic and sericite, and locally weak potassic feldspar, while the ore distal ones include mainly chlorite and carbonate.

Three alteration zones were identified according to the alteration minerals and their assemblage (Figure 5): (1)Chlorite-sericite zone: this zone is developed on the periphery of the fractured zone. Altered feldspars, hydrothermal quartz, carbonate veinlets, and few galena veinlets are observed in this zone, and alteration intensity is commonly low.(2)Quartz-calcite-dolomite-sericite zone: this zone is developed within the fracture zone and is characterized by varying widths and ore wallrock interlayers. This stage is mostly associated with Ag mineralization.(3)Silicic zone: this zone is located at the center of the fractured zone and is the mineralization center and the most altered part. The altered rocks are primarily composed of quartz and sulfides. Concentrations of Si and K tend to increase while that of Na decreases from the fresh wallrock to the silicic core, which corresponds to increasing quartz and sericite but decreasing sodic feldspar contents, respectively, by wallrock alteration.

Mineralization is divided into three stages according to spatial distributions and vein crosscutting relationships (Figure 6): (1)Quartz-pyrite stage: this stage is dominated by silicification and formed allotriomorphic granular quartz. Alteration minerals, such as sericite, fuchsite, and few vein/disseminated pyrites, are also observed. Quartz and pyrite show cataclastic texture and are associated with metallic minerals from the late Ag ore period.(2)Quartz-polymetallic sulfide stage: this stage represents the main Ag-Pb-Zn ore stage and has a wide variety of metallic minerals including galena, sphalerite, pyrite, chalcopyrite, (Ag-bearing)-tetrahedrite, sulfosalts, and native Ag. Galena, sphalerite, and Ag sulfides are associated with sulfosalts and occur within the fracture-infilling veins.(3)Quartz-carbonate-polymetallic sulfide stage: hydrothermal minerals include mainly calcite, dolomite, ankerite and siderite, and, locally, quartz, pyrite, and chalcopyrite. Furthermore, carbonate (calcite and dolomite) druses and geodes are often observed.

4. Sampling and Analysis Methods

4.1. Sampling

Doubly polished thin sections were made from 19 quartz and 6 calcite samples associated with the three ore stages (Figure 3). 11 samples for H-O isotope analysis and 26 samples for C-O isotope analysis were selected under the microscope to ensure that they represent all Stages 1 to 3, and all the samples were crushed and ground into 40–80 mesh granules. 26 and 28 representative samples were selected for sulfur and lead isotope analyses, respectively. The samples were milled into 200 mesh.

4.2. Fluid Inclusions

Petrographic observations and temperature measurements of fluid inclusions (FIs) were made with a Linkam THMSG600 heating-freezing stage at the Key Laboratory of Metallogenic Prediction of Nonferrous Metals and Geological Environment Monitoring (Central South University). Analytical precisions were than ±1°C and ±0.1°C for temperatures of 30 to 600°C and −196 to 30°C, respectively. Freezing and heating temperatures were measured using the same inclusions (where possible), and phase transitions were carefully monitored. The temperatures were initially modified by steps of 5°C/min and changed gradually by steps of 0.2°C/min when approaching the phase transition.

Bulk FI analysis was performed for the gas-liquid-phase compositions at single mineral . The analysis was conducted at the same laboratory with a Varian-3400 gas chromatograph (Varian) and a DX-120 ion chromatograph (Dionen). The analytical error was less than 5%.

4.3. Hydrogen-Oxygen Isotope Analyses

The H–O isotope samples were collected from the drill core. Eight mineral samples representing different stages were selected for the analyses. The samples were approximately 20 mesh with a purity of ~99.5%. Vacuum thermal explosion and zinc reduction methods were adopted to extract the hydrogen. The BrF5 method was used to obtain pure O2 from quartz samples (under vacuum conditions; at 500–680°C), which was subsequently transferred into CO2. The H–O isotope analyses were conducted at the BRIUG (Beijing Research Institute of Uranium Geology) Analytical Laboratory with a MAT–253 mass spectrometry. Analytical errors for the H and O isotope analyses are 0.2 and 2‰, respectively.

4.4. Carbon-Oxygen Isotope Analyses

Calcite C–O isotope compositions were obtained using the MAT-251 EM mass spectrometer at the BRIUG Analytical Laboratory. Calcite reacts with pure phosphoric acid to produce CO2. The analytical precisions (2σ) are ±0.2‰ for carbon isotope and ±2‰ for oxygen isotope. C–O isotope compositions are reported relative to PDB ().

4.5. Sulfur-Lead Isotope Analyses

The isotope samples were collected from both open pits and drill cores. Pure single minerals (>95%) were selected for isotope analyses. Cu2O was used as an oxidizing agent for the sulfide sample to produce SO2, which was subsequently frozen and collected for the S isotope analysis with a MAT–251 mass spectrometer. The international standard VCDT was used in this regard, and the accuracy is ±2‰. The Pb isotope analyses were conducted with an IsoProbe–T thermal ionization mass spectrometer. Lead was separated and purified using the conventional cation–exchange technique (with diluted HBr as the eluant). The 208Pb/206Pb, 207Pb/206Pb, and 204Pb/206Pb ratios of the NBS981 Pb standard were (2σ), (2σ), and (2σ), respectively. The analyses were conducted at the BRIUG Analytical Laboratory.

5. Results

5.1. Fluid Inclusions
5.1.1. Morphology

Abundant FIs are trapped in the quartz from Stage 1 to Stage 3 carbonate-quartz veins. These isolated/randomly clustered FIs in the quartz crystals are interpreted as primary ([25]; Figures 7(d)7(h)). The FIs (from Stage 1 to Stage 3) are dominantly vapor-liquid two-phase aqueous (W) type (Figure 7). W-type FIs are composed of gas and liquid phases at room temperature. Individual FIs are 10–30 μm large with a filling percentage of 10–90%. The inclusions are dominantly irregular in shape, followed by ellipsoidal, elongated, and lentoid, with locally rectangular shape. W-type FIs homogenized to liquid or vapor phase by heating.

5.1.2. Thermometry

A total of 152 FIs (from 31 samples) were measured. The thermometric results are given in Table 1 and Figure 8. The homogenization temperatures of Stages 1, 2, and 3 range 198–332°C, 132–260°C, and 97–166°C, respectively. Relations between the freezing point depression and salinity for the W-type FIs can be expressed as Equation (1) [26]: where is the weight percentage of NaCl (0–23.3 wt% NaCl) and is the freezing point depression (°C). From the measurement, fluid salinity of Stages 1, 2, and 3 are 4.0–13.3, 1.1–13.1, and 1.9–7.6 wt% NaCleqv, respectively.


StageMineralsFI typeTmice (°C)Thtot (°C)Salinity (wt% NaCleqv)

1QuartzW-9.4 to -2.4198 to 332 (L)4.0 to 13.3
2QuartzW-9.2 to -0.6132 to 260 (L,V)1.1 to 4.3
6.6 to 13.1
3QuartzW-4.8 to -1.197 to 166 (L)1.9 to 7.6

Tmice: final melting temperature; Thtot: total homogenization temperature. L and V mean that the FIs homogenized to liquid (L) or vapor (V).
5.1.3. Vapor and Liquid Compositions

The vapor and liquid compositions of the FI are listed in Table 2. The vapor phase comprises primarily H2O and minor CO2, H2, CO, N2, and CH4. The liquid phase contains Ca2+, Na+, K+, SO42−, Cl, and F. For the cations, the Ca2+ content is the highest (followed by Na+), whereas the Mg+ and K+ contents are the lowest. For the anions, SO42− content is the highest (followed by Cl), and the F content is the lowest. The ore fluid belongs to a Cl-(SO42−)-Na-K-(Mg) system.


Sample no.
Mineral
Stage 1Stage 2Stage 3
SJ4-04
Quartz
SJ4-05
Quartz
SJ4-07
Quartz
SJ4-14
Quartz
LMD-06
Calcite
LMD-26
Calcite

Vapor/10-6H20.29460.20170.06170.24450.70860.474
N20.08560.30770.23781.2390.02040.2389
CO0.08390.11160.03440.095814.890.158
CH40.08710.05560.02130.0804/0.0496
CO25.0432.7294.2036.032108.614.23
H2O9840011760022470027440011350085970

Liquid/10-6F-3.771.5880.12480.2820.54451.365
Cl-11.3726.2343.1728.3312.643.313
NO3-/0.3314///0.1979
SO42-59.9100.8273.9103.616.4422.71
Na+7.50223.728.2614.9710.135.313
K+1.5672.9914.3863.1142.4162.04
Mg2+1.2841.4360.86860.554718.2110
Ca2+31.9613.349.7646.116.56321.25

5.2. H-O Isotope Compositions

For Stage 1, δ18O values of quartz range from 14.1 to 15.9‰, while δ18OH2O values of the fluid in equilibrium with quartz are of 5.8–7.6‰. δD values range from −92 to −76‰. For Stage 2, the quartz δ18O, δ18OH2O, and δD values are of 7.4–11.2‰, −4.4 to −0.6‰, and−81 to −63‰, respectively. For Stage 3, the quartz δ18O, δ18OH2O, and δD values are of 6.8–7.9‰, −8.2 to −7.9‰, and−79 to −71‰, respectively (Table 3).


Sample no.MineralStageδDδ18OV-SMOWδ18OH2O

ZK1002Quartz1-8315.97.6
ZK1002-9214.86.5
ZK301-7614.15.8
ZK702-8915.16.8

ZK901Quartz2-639.7-3.0
ZK1014-818.3-4.4
ZK1014-697.4-5.3
ZK2701-7611.2-1.5

ZK1002Quartz3-797.9-8.9
ZK1002-717.1-9.7
ZK301Calcite-736.8-10.0

5.3. C-O Isotope Compositions

The C-O isotopic analyses were conducted on 26 calcite samples from Stage 1 to Stage 3 (Table 4). The calcite δ13CVPDB and δ18OSMOW values range from −11.2 to 0.9‰ (avg. −1.67‰) and from 9.21 to 20.86‰ (avg. 13.66‰), respectively.


Sample no.δ13CVPDB (‰)δ18OSMOW (‰)

LMD-020.89.21
LMD-04-214.68
LMD-05019.52
LMD-06-0.118.49
LMD-08018.59
LMD-09-0.110.14
LMD-11-0.114.37
LMD-13-1.117.77
LMD-180.811.177
LMD-20-0.310.04
LMD-210.911.27
LMD-23-1.314.16
LMD-240.99.32
LMD-25-0.214.06
LMD-260.110.45
LMD-29-6.814.57
LMD-30-0.412.2
LMD-32-7.114.57
LMD-47-4.512.41
LMD-48-2.314.57
LMD-49-1.512.82
LMD-51-1.512.61
K8-3011.17
PD1058 K1-1-1.611.58
ZK306-Y1-4.714.47
K23-3-11.220.86

5.4. S-Pb Isotope Compositions

The S and Pb isotope data from the Longmendian deposit are listed in Tables 5 and 6, respectively. The pyrite δ34S values range from −1.42 to 2.35‰ (avg. 0.26‰). The chalcopyrite and galena samples have to 38.795, to 15.686, and to 18.101.


Sample no.δ34SCDT (‰)

SJ4-03-1.35
SJ4-03-1.42
SJ4-04-0.99
SJ4-05-0.21
SJ4-06-0.47
SJ4-09-0.74
SJ4-09-0.82
SJ4-11-0.39
SJ4-11-0.52
SJ4-12-0.44
SJ4-14-0.31
SJ4-21-0.47
SJ4-22-0.38
Sj5-1-0.96
Sj5-20.36
Sj5-20.57
Sj5-30.48
Sj5-51.03
SJ2-1-0.3
SJ41-32.35
SJ07-31.94
SJ07-32
SJ07-42.02
SJ07-61.49
SJ07-71.96
SJ07-102.21


Sample no.Minerals206Pb/204Pb207Pb/204Pb208Pb/204Pb(Ma)

LMD-DB-5Chalcopyrite18.10115.55838.478340
LMD-NagGalena17.8815.53738.275474
LMD-01Galena17.95415.65138.675553
LMD-02Galena18.01815.68638.795548
LMD-05Galena17.93115.5438.314441
LMD-08Galena17.8915.48338.149403
LMD-09Galena17.88115.51138.214443
LMD-11Galena17.95215.55538.378444
LMD-18Galena17.82515.44838.013408
LMD-19Galena17.82815.47838.087442
LMD-22Galena17.83315.46938.121427
LMD-23Galena17.6615.38837.771457
LMD-24Galena17.85615.49538.164442
LMD-25Galena17.78415.41837.962402
LMD-26Galena17.69415.4738.035530
LMD-30Galena17.83415.52438.224492
LMD-45Galena17.87915.56638.38509
LMD-47Galena17.75815.46338.043475
LMD-48Galena17.7615.44738.05454
LMD-49Galena17.73915.52938.208566
LMD-51Galena17.76415.45838.052465
LMD-52Galena17.78415.48538.14482
LMD-53Galena17.82815.50238.174470
LMD-54Galena17.79115.5138.17506

6. Discussion

6.1. Sources of Ore-Forming Material

The δ18OH2O values of Stage 1 ore fluids (5.8–7.6‰, avg. 6.7‰) fall inside the range of magmatic water (5.5–9.5‰) defined by Sheppard [27], but different from those of the Taihua Group and pegmatite (–6.8‰; [28]). As shown in the δ18OH2O vs. δD plot (Figure 9), all Stage 1 data points fall inside/close to the magmatic water field, suggesting a magmatic fluid origin. The Stage 2 δ18OQtz (7.4–11.2‰) and δ18OH2O (–4.4 to –0.6‰, avg. –2.7‰) are lower than their Stage 1 counterparts, and the data points fall between the magmatic water and meteoric water fields (Figure 9), indicating probable meteoric water incursion. Stage 3 data points fall close to the meteoric water line, suggesting that the hydrothermal fluid was dominantly meteoric.

Most data points from the Longmendian, Shagou, Tieluping, and Haopingou deposits fall within the magmatic water field (Figure 10), pointing to a magmatic fluid source. Furthermore, the Longmendian data points also show well-defined linear trend toward the marine carbonate field (Figure 10), suggesting a marine carbonate input for the ore fluids. Carbonate rocks are abundant in the Longtanggou Formation (Taihua Group) and may represent a potential fluid source for the Ag-Pb-Zn mineralization.

The δ34S values of hydrothermal minerals depend not only on the source δ34S values but also on the physicochemical conditions of the S-bearing fluid migration and precipitation. Ohmoto [35] proposed that the hydrothermal mineral δ34S value is a function of the hydrothermal fluid δ34S value (δ34S∑S), oxygen fugacity (fo2), temperature (), pH, and ionic strength (), i.e., . He further hypothesized that the fluid δ34S value is characterized by a relatively simple mineral assemblage and (with the absence of sulfates) should be similar to that of total sulfide (i.e., ). No sulfate minerals were found in the Longmendian deposit, and the mineral composition was relatively simple. Therefore, the sulfide δ34S could approximate the δ34S∑S of the hydrothermal system. The δ34S values of the Longmendian deposit (−1.42 to 2.35‰) are similar to those from magmatic-hydrothermal systems (; [36]) and marginally overlap with the Taihua Gp. metamorphic rocks (Figure 11). This indicates that the sulfur was likely derived from magmatic-hydrothermal fluids and Taihua Gp. metamorphic rocks.

Polymetallic sulfide (pyrite, chalcopyrite, and galena) from the Longmendian deposit yields a single-stage model age of 340–566 Ma (Table 6), which is inconsistent with the Neoarchean Taihua Group metamorphosed terrane (>2.2 Ga) and the regional Ag-Pb-Zn vein-type mineralization (145–133 Ma; see Section 6.3), indicating the presence of excess radiogenic Pb in the fluid system, due to either the decay of U and Th or fluid mixing [3739]. In a 207Pb/204Pb vs. 206Pb/204Pb diagram (Figure 12), the samples plot display a linear correlation. Assuming that the linear distribution of Pb values represents a second isochron (i.e., metallogenesis occurred in multiple phases), we obtain a two-stage model age of 4207–4209 Ma, which does not have geological significance (e.g., >3.8 Ma), indicating that the linear relationship records mixing rather than a second isochron. Therefore, we speculate that the ore-forming fluid system at Longmendian was an open system, containing a mixture of external Pb. For a two Pb-source end member mixing system, Pb isotopic data should fall on a line between the two end members [40]. Figure 12 indicates a clear linear relationship for the ore Pb data. Therefore, the ore Pb was likely derived from two end members, one with low radiogenic Pb and the other with high radiogenic Pb contents [40]. On 207Pb/204Pb vs. 206Pb/204Pb and 208Pb/204Pb vs. 206Pb/204Pb diagrams (Figure 12), the samples plot close to the composition of the metamorphic strata of the Taihua Group and Xiong’er Group, indicating that Pb in the Longmendian deposit was likely derived from the metamorphic strata of the Taihua Group and Xiong’er Group during fluid-rock reaction [38, 39]. In addition, fluids with more radiogenic Pb were probably derived from concealed granitoids.

The ore-forming material of Longmendian deposit mainly derives from magma, and the evidence is as follows: (1) the H–O–C–S–Pb isotope shows that the ore-forming fluid originates from magma. Furthermore, this Na+–Ca2+–(K+)–SO42−–Cl dominated fluids derived from magmatic system also reported in the Jiawula Ag–Pb–Zn deposit [42]. (2) No granite outcrop was found in Longmendian area; only the basic dyke of Paleozoic was found (Figure 3), but the geophysical data also showed that there were concealed intrusions in this area [33]. (3) The wallrock, ore-controlling structure, orebody characteristics, ore minerals, and gangue mineral of the Longmendian deposit were similar to those of the spatially adjacent Haopinggou deposit (Table 7), in which the ore-forming fluid originates from magma [33].


DepositHost rockOre typeOre mineralGangue mineralAlteration zoneOre fluid featureDeposit typeData source

LongmendianTaihua Gp. gneissQuartz-vein and altered-rock type Au oreGalena, sphalerite, pyrite, chalcopyrite, silver-bearing tetrahedrite, pyrargyrite, argentite, bornite, native silver, tetrahedrite, polybasiteQuartz, calcite, siderite, ankerite, sericite, fuchsite, muscoviteSilicic; quartz-carbonate-sericite; chlorite-sericiteMedium-low temperature, low salinity CO2-H2O-NaCl system; vapor comprises H2O and CO2, with some H2, CO, N2, and CH4. Liquid phase comprises Ca2+, Na+, K+, SO42−, Cl, and F

ShagouTaihua Gp. gneissMassive and vein-type Ag-bearing lead-zinc oreSilicic; sericite; chlorite; carbonateMedium-low temperature, low salinity CO2-H2O-NaCl systemEpithermal[33]

TielupingTaihua Gp. gneissQuartz vein type and altered rock type silver oreGalena, sphalerite, pyrite, chalcopyrite, arsenopyrite, pyrargyrite, silver-bearing tetrahedrite, argentite, bornite, native silver, tetrahedrite, skinnerite, minetisite, domingiteQuartz, sericite, chlorite, plagioclase, potash feldspar, amphibole, biotite, siderite, calcite, ankerite, fuchsiteSilicic; sericite; chlorite; carbonateMedium-low temperature, low salinity CO2-H2O-NaCl system; vapor comprises H2O, CO2, N2, O2, CO, CH4, C2H2, C2H4, and C2H6Epithermal[34]

HaopinggouTaihua Gp. gneissQuartz vein type and altered rock type silver oreSilicic; sericite; chlorite; carbonateMedium-low temperature, low salinity H2O-NaCl systemEpithermal[33]

6.2. Ore Fluid Evolution and Ore Precipitation Mechanism
6.2.1. Nature and Evolution of Ore-Forming Fluids

In this study, the ore fluids are determined to be of medium-low temperature and belong to a medium-low salinity H2O–NaCl system that contains Na+-Ca2+-SO42−-Cl. From Stage 1 to Stage 3, significant changes occur in the FI types and the ore fluid temperature and salinity (Figures 8 and 13), as described in detail as follows:

(1) Stage 1. Magmatic intrusion and its subsequent fractionation may have released magmatic fluid to form high-temperature (198–332°C) Stage 1 ore fluids. The salinity-homogenization temperature plot (Figure 13) indicates that the salinity of Stage 1 fluids did not change significantly (4.0–13.3 wt% NaCleqv), and the major temperature drop could have attributed to cooling.

(2) Stage 2. The main-stage mineralization may have contributed by the gradual mixing of magmatic water and meteoric water. The ore fluid temperature and salinity are 132–260°C and 1.1–13.1 wt% NaCleqv, respectively. The salinity-homogenization temperature plot (Figure 13) shows bimodal fluid salinity, i.e., high salinity (>6 wt% NaCleqv) and low salinity (<5 wt% NaCleqv). The coexistence of several FI types (with similar homogenization temperature) further suggests that fluid boiling had taken place (Figures 7(e) and 7(f)).

(3) Stage 3. Fluid inclusions in this stage are dominated by W-type. The further temperature and salinity drop (cf. Stage 1 and 2 FIs) in Stage 3 which could be attributed to the continuous incursion of low-temperature and low-salinity meteoric water (Figures 9 and 13).

6.2.2. Ore Precipitation Mechanism

In general, silver occurs dominantly as Ag+ in hydrothermal fluids [43], and is mainly transported as silver chloride (AgCl2-) or/and silver bisulfide complexes (AgHS0) in the fluids [44, 45]. Under lower temperatures (<200°C), AgHS0 complexes occur dominantly under near-neutral conditions, whereas AgCl2− complexes occur largely under (mildly)-acidic conditions (e.g., [46, 47]). Under higher temperatures (>400°C), silver is transported dominantly in AgCl2− complexes, whereas AgHS0 species are only stable under (mildly)-alkaline conditions (e.g., [44, 48]). The Longmendian ore fluids were in equilibrium with montmorillonite–sericite–quartz and K-feldspar–muscovite–quartz assemblages, which yielded –6.5 at 200–350°C [49, 50]. The Stage 1 and 2 fluids are featured by medium to low temperatures (avg. 291°C and 185°C, respectively), and thus, the silver may have transported mainly in AgHS0 complexes (e.g., [46, 47, 51]). In these fluids, Zn can be transported in both Zn–Cl and Zn(HS)3- complexes [52, 53]. Lead chloride complexes are usually important for Pb transport in intermediate-to-high-salinity fluids [54]. Our FI compositional analysis also shows that Cl- and SO42- contents are high in the Longmendian ore fluid (Table 2).

Generally, vein-type ore precipitation in hydrothermal deposits can by triggered by fluid boiling, mixing, and/or simply cooling [5558]. The physicochemical changes on the fluids by boiling would affect Ag sulfide saturation via H2S degassing and/or pH increase [48]. pH increases quite drastically during boiling, especially in Stage 2 because of degassing of CO2 and to a lesser extent H2S. Conductive cooling leads to pH decrease, plus minor effect on aqueous species activities [48]. The fluid cooling and pH increase caused by mixing with meteoric water (seawater or other high-pH fluids) may have led to Zn deposition because of (i) change in the dominating Zn complex (Zn–Cl complexes in high-temperature acidic fluids and Zn(HS)3- and ZnS(HS) in low-temperature and alkaline fluids), and (ii) Zn solubility drop because of pH increase. Previous experimental studies have shown that temperature drop can effectively dissociate zinc- and lead-chloride complexes (e.g., [59]). As discussed above, fluid inclusion and H–C–O isotope evidence points to fluid boiling, mixing, and cooling at Stage 2 (Figures 8 and 13), which likely formed the quartz-polymetallic sulfide ore veins.

6.3. Metallogenetic Mechanism

Previous studies have reported the K-Ar/Ar–Ar ages and molybdenite Re-Os model ages of the Ag-Pb-Zn-Mo deposits in the study area [311]. The mineralization ages reported fall into two groups: Paleoproterozoic (1888–1686 Ma) and Early Cretaceous (145–133 Ma). The Paleoproterozoic phase has formed the Zhai’ao and the Longmendian Mo deposits. The Early Cretaceous has formed the Tieluping, Shagou, and Haopinggou deposits. Although ca. 1888 Ma molybdenite Re–Os isochron age was obtained [15], the existence of molybdenite in the Pb-Zn-Ag-quartz veins has not been confirmed, and thus, the Paleoproterozoic age may reflect an earlier mineralization phase before the Ag-Pb-Zn vein-type mineralization.

The ore deposit geology (wallrock, ore-controlling structure) and ore/gangue mineral assemblages of the Longmendian deposit resemble those of the nearby Haopinggou, Shagou, and Tieluping deposits (Table 7), and hence, these broadly coeval (145–133 Ma) deposits may belong to the same Ag-Pb-Zn mineral system. Vein-type Ag-Pb-Zn mineralization at Shagou, Haopinggou, Tieluping, and Longmendian can be attributed to crustal extension-related (Figure 14; [18]) because (1) Late Mesozoic granitoids (157–127 Ma; [24, 60, 61]) contain abundant mafic microgranular enclaves (MMEs), which are interpreted to represent mixing of mafic and felsic magmas [62, 63]. In addition, some of the MME-bearing plutons are intruded by slightly younger mafic dykes [7, 6264]. (2) The presence of Early Cretaceous Xiong’er, Xiaoshan, and Xiaoqinling metamorphic core complexes (Figure 1; [65, 66]) demonstrates that large parts of the southern NCC were dominated by extensional tectonics. This extensional event may have linked to lithospheric thinning caused by the west-dipping Paleo-Pacific subduction, which led to partial decratonization of the NCC [7, 8, 24].

The mineralization was strictly controlled by the NE–NNE-trending fault zones. The Ag–Pb–Zn ore-forming temperature (132–260°C) is low to medium, while the ore fluids progressed from dominantly magmatic-sourced to magmatic-meteoric mixed. The S and Pb isotope compositions indicate that the ore-forming materials were primarily originated from the magma with input from the metamorphosed sequences. Geological and geochemical features suggest that the Longmendian deposit likely belongs to medium-to-low temperature hydrothermal-type related to Cretaceous granitic magmatism (Figure 14).

At Longmendian, the ore minerals comprise galena, sphalerite, pyrite, chalcopyrite, (Ag-bearing)-tetrahedrite, and native silver, resembling typical low-sulfidation to intermediate-sulfidation (LS/IS) epithermal mineralization. The LS/IS epithermal affinity is also reflected in the alteration mineral assemblage (quartz+calcite+adularia+illite), intermediate-low ore fluid temperature (150–320°C), and bimodal salinity (<5% NaCleqv and >6% NaCleqv) that suggests fluid boiling.

7. Conclusions

(1)The H–C–O isotope evidence indicates that the ore fluids were derived from magmatic water with increasing meteoric water input toward the later ore stages. The S–Pb isotope evidence indicates that the ore-forming materials were mainly originated from the granitic magma and the Taihua Group wallrocks(2)Ore-forming fluids were largely of medium-low temperature and medium-low salinity, belonging to a low-density H2O–NaCl system that contains Na+-Ca2+-SO42−-Cl. Fluid boiling and cooling, and mixing with meteoric water, may have contributed to the ore precipitation

Mineralization at Longmendian shares similar geological characteristics (in lithology, structure, ore/gangue assemblage, and ore fluid temperature and salinity) with typical low-sulfidation to intermediate-sulfidation (LS/IS) epithermal deposits.

Data Availability

The data used to support the findings of this study are included within the article.

Conflicts of Interest

The authors declare no conflict of interest.

Authors’ Contributions

Xinling Chen, Cheng Wang, and Yongjun Shao conceived and designed the experiment. Cheng Wang and Xinling Chen performed the experiment. All authors wrote the paper.

Acknowledgments

This work was supported by the Innovation-Driven Project of Central South University (2018zzts196) and the Open Topic of Hunan Key Laboratory of Land Resources Evaluation and Utilization (Project SYS–ZX–201804).

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