Next Article in Journal
The Color Palette of the Mosaics in the Roman Villa of Noheda (Spain)
Previous Article in Journal
Incorporation of Incompatible Strontium and Barium Ions into Calcite (CaCO3) through Amorphous Calcium Carbonate
 
 
Search for Articles:
Title / Keyword
Author / Affiliation / Email
Journal
Article Type
 
 
Advanced Search
 
Section
Special Issue
Volume
Issue
Number
Page
 
Journals
Minerals
Volume 10
Issue 3
10.3390/min10030271
minerals-logo
Submit to this Journal Review for this Journal Propose a Special Issue
► Article Menu

Article Menu

share Share announcement Help format_quote Cite question_answer Discuss in SciProfiles thumb_up
...
Endorse textsms
...
Comment
first_page
settings
Order Article Reprints
Font Type:
Arial Georgia Verdana
Font Size:
Aa Aa Aa
Line Spacing:
Column Width:
Background:
Article

Geochemistry and Origin of Scheelites from the Xiaoyao Tungsten Skarn Deposit in the Jiangnan Tungsten Belt, SE China

by
Qiangwei Su
1,*,
Jingwen Mao
1,
Jia Sun
1,
Linghao Zhao
2 and
Shengfa Xu
3
1
MLR Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, China
2
National Research Centre for Geoanalysis, Beijing 100037, China
3
332 Geological Team of Anhui Bureau of Geology and Mineral Resources, Huangshan 245000, China
*
Author to whom correspondence should be addressed.
Minerals 2020, 10(3), 271; https://doi.org/10.3390/min10030271
Submission received: 13 January 2020 / Revised: 10 March 2020 / Accepted: 11 March 2020 / Published: 18 March 2020
Browse Figures
Versions Notes

Abstract

:
The type, association, variations, and valence states of several metal elements of scheelite can trace the source and evolution of the ore-forming fluids. There are four types of scheelite from the Xiaoyao deposit: (1) scheelite intergrown with garnet in the proximal zone (Sch1a) and with pyroxene in the distal zone (Sch1b), (2) scheelite replaced Sch1a (Sch2a) and crystallized as rims around Sch1b (Sch2b), (3) quartz vein scheelite with oscillatory zoning (Sch3), and 4) scheelite (Sch4) within micro-fractures of Sch3. Substitutions involving Mo and Cd are of particular relevance, and both elements are redox-sensitive and oxidized Sch1a, Sch2b, Sch3 are Mo and Cd enriched, relatively reduced Sch1b, Sch2a, Sch4 are depleted Mo and Cd. Sch1a, Sch2a, Sch3, and Sch4 are characterized by a typical right-inclined rare earth element (REE) pattern, inherited from ore-related granodiorite and modified by the precipitation of skarn minerals. Sch1b and Sch2b are characterized by low light rare earth element/heavy rare earth element (LREE/HREE) ratios, influenced by a shift in fO2 during fluid-rock alteration. Sch1b, Sch2b and Sch3 have higher Sr contents than those of Sch1a and Sch2a, reveal that host-rock alteration and fluid–rock interaction have elevated Sr contents. The Y/Ho ratios of scheelite gradually increase from skarn to quartz vein stages, due to fluid fractionation caused by fluid–rock interaction. Thus, the variation in REE and trace elements in scheelite in time and space reflects a complex magmatic-hydrothermal process involving various fluid–rock interactions and fluid mixing.

1. Introduction

Scheelite (CaWO4) is one of the dominant tungsten-containing minerals in porphyry-skarn W deposits, quartz vein W and Au-W deposits, and some metamorphic Au deposits [1,2]. Scheelite incorporates relatively high amounts of REE and Sr in substitution for Ca [3,4], and has been used to characterize the ore-forming fluids [5,6,7,8] and the genetic type of deposits [9,10,11]. The REE patterns in scheelite are highly sensitive to the hydrothermal evolution, making scheelite act as a promising tool to understand prevailing hydrothermal conditions [3,4]. Despite the extensive literature on trace elements in scheelite, only a few studies focus on tungsten skarn deposits [12,13,14,15]. Most tungsten skarn deposits are characterized by multiple scheelite generations which underwent dissolution and re-precipitation processes [16,17,18]. The superimposition of multiple scheelite generations complicates study on the ore-forming processes via the trace element chemistry of scheelite. Cathodoluminescence (CL) imaging has been proven to be an effective technique to reveal internal textures, zoning and trace element distributions in scheelite [3]. However, previous studies did not evaluate dissolution and re-precipitation processes in scheelite from tungsten skarn deposits due to the changing hydrothermal fluids [13,14]. The detailed textural characterization and systematic investigations of scheelite from each stage prior to in situ chemical analysis are critical to constraint the evolution of skarn systems and W ore precipitation.
The Jiangnan tungsten belt in the southeastern margin of the Yangtze Craton is a new giant tungsten province with WO3 reserves over 5.0 million tons [19,20,21,22,23], including the Dahutang (reserves of 1.10 Mt and grade of 0.18%) and the Zhuxi (reserves of 3.44 Mt and grade of 0.54%) deposits, as well as other large-scale tungsten deposits, such as Yangchuling, Xiaoyao, Dongyuan, Zhuxiling deposits [24,25,26]. The present study focuses on the Xiaoyao tungsten skarn deposit, characterized by complex scheelite textural features. The Xiaoyao deposit has reserves of 75,000 tons of WO3 with an average grade of 0.2% [27]. We present both textural and compositional features for scheelite from the Xiaoyao deposit to evaluate the importance of dissolution and re-precipitation processes in the formation of skarn-related scheelite.

2. Geologic Setting

The Xiaoyao tungsten deposit is located in the southeastern part of the Jiangnan tungsten belt (JNB) (Figure 1). The rocks in the mine area are the early Neoproterozoic Xiuning Formation sandstone, late Neoproterozoic Lantian Formation limestone and slate, Piyuancun Formation clastic siliceous rocks, Cambrian Hetang Formation shale, and Yangliugang Formation shale (Figure 2). Most tungsten orebodies are hosted in the Lantian and Hetang Formations.
The granitic intrusion in the Xiaoyao mine area comprises granodiorite, granite, and granite porphyry (Figure 2). The granodiorite has a U-Pb zircon age of 149.4 ± 1.1 Ma [28]. The granodiorite consists mainly of plagioclase (50–55%), K-feldspar (10–15%), quartz (20–25%), biotite (15–20%), and hornblende (3%–5%), with minor apatite, zircon, magnetite, and titanite. The granite porphyry with the U-Pb zircon ages of 133.2 ± 0.8 Ma are younger and crosscuts the granodiorite bodies. Phenocrysts include K-feldspar (20–25%), plagioclase (10–15%), and quartz (5–10%). The granite porphyry matrix is composed of microgranular quartz, plagioclase, and K-feldspar. The granite in the northern part of the mining area was dated to 130–124 Ma by LA–ICP–MS zircon U–Pb methods [29]. This granite contains K-feldspar (45–50%), quartz (30–35%), plagioclase (10–15%), and biotite (2–3%).
Tungsten orebodies mainly occur within skarns at contact zones between the Kaobeijian granodiorite pluton and their wall rocks (Figure 2). The largest tungsten orebody (W1) developed along the contact between granodiorite and the limestone of the Lantian Formation (Figure 3). It has a length of 1300 m and a width of 5–35 m. It strikes in an NE direction and dips toward the north at an angle of 80° (Figure 3).
The Xiaoyao skarn is mainly composed of garnet and pyroxene, with retrograde alteration minerals of epidote, tremolite, actinolite, chlorite, quartz, fluorite and calcite. The main ore minerals are scheelite, molybdenite, chalcopyrite, and pyrrhotite. Four mineralization stages have been identified based on crosscutting relationships and mineral assemblage: skarn, retrograde alteration, quartz–scheelite–sulfide, and carbonate stages.
The skarn stage is characterized by a large amount of garnet and pyroxene distributed in different zones (Figure 4a,b). For example, in drill core ZK4704, the skarn has a pyroxene-dominated distal zone and a garnet-dominated proximal zone from shallow to deep. The garnets in proximal zones are always reddish to red and fine- to coarse-grained and euhedral to subhedral with oscillatory zonation (Figure 4a, sample 15XY-31). They commonly intergrow with pyroxenes. The pyroxenes are generally pale green in color. They occur as fine-grained (0.2–1.0 mm) subhedral to anhedral minerals. The distal zones are dominated by dark green, coarse-grained pyroxene crystals without garnet (Figure 4b, sample 15XY-14). The pyroxene grains are anhedral to subhedral, varying from 100 to 500 µm in size. The retrograde alteration stage is characterized by the precipitation of hydrous silicate minerals such as epidote, actinolite, and chlorite; and the associated mineralization is scheelite replacing garnet and pyroxene (Figure 4c). The quartz–scheelite–sulfide stage is characterized by a scheelite–molybdenite–pyrrhotite–chalcopyrite–quartz assemblage in scheelite- and sulfide-rich veins cutting the early scheelite-bearing skarn ores (Figure 4d–f). The scheelite in this stage generally occurs as large anhedral grains that intergrow with quartz. The carbonate stage is characterized by a calcite–sphalerite–galena assemblage in sulfide-rich veins that cut through the tungsten ores and wall rock.

3. Samples and Analytical Methods

3.1. Sample Descriptions

The samples for electron microprobe and in-situ LA-ICP-MS trace elements analysis were collected from the drill cores taken from the largest W1 orebody (Figure 3). The mineralogical and petrographic features and sampling depth of the samples are summarized in Table 1. Samples were evaluated petrographically employing optical and CL microscopy to characterize the abundance and physical properties of scheelite, including shape, size, color, and luminescence. Selected grains were analyzed by electron probe microanalysis (EPMA) for major element geochemistry and in situ LA-ICP-MS for trace element geochemistry.
Based on CL textures and mineral paragenesis, four types of scheelite have been recognized. Scheelite 1 (Sch1) occurs as disseminated crystal in the skarn (Figure 5a,e), which is further divided based on different pyroxene, garnet and scheelite assemblages. Scheelite 1a (Sch1a) is intergrown with garnet in the proximal zone (Figure 5a) and Scheelite 1b (Sch1b) is intergrown with pyroxene in the distal zone (Figure 5e). Sch1a shows yellowish fluorescent in short-waved UV light. It is mainly fine-grained, euhedral to subhedral, with diameters of 0.1 to 0.2 mm (Figure 5a). Sch1a shows homogeneous textures with dark-CL (weak CL response, Figure 5b), reflecting that no dissolution took place during any stage of growth. Sch1b shows blue fluorescent in short-waved UV light and generally occurs as anhedral coarse grains of 0.5–1.0 mm in size (Figure 5e). The homogeneous textures, as shown by the strong and bright CL of Sch1b, may be precipitation features associated with precipitating under stable conditions (Figure 5f). Scheelite 2a (Sch2a) selectively replaced parts of Sch1a that likely represent relict fluid pathways during the alteration stage (Figure 5c,h). Sch2a occurs as irregular, with a light-CL with a grain size of 0.2–0.5 mm (Figure 5c,h). The Sch2a crystal shows a strong correlation with molybdenite (Figure 5d) and is often associated with epidote, actinolite, chlorite, and quartz (Figure 5g). Scheelite 2b (Sch2b) is crystallized as rims around the Sch1b with dark-CL (Figure 5f). Sch2b generally occurs as anhedral coarse grain of 1.0–1.5 mm in size (Figure 5e). CL images of Sch2a and Sch2b from the mineralized skarn reveal later dissolution–reprecipitation reactions (Figure 5c,f,h).
Scheelite 3 (Sch3) forms abundant large scheelite clusters within scheelite ± sulfide-rich quartz veins that typically crosscut the early scheelite-bearing skarn ores (Figure 5l). Sch3 generally occurs as a subhedral–anhedral coarse grain of 0.2–1.5 mm in size (Figure 5l). Sch3 exhibit obvious oscillatory zoning textures, with a few examples showing the core-rim textures on CL images (Figure 5j,k). The rim is oscillatory growth zoning and the core is homogeneous, as shown on CL images (Figure 5j,k).
Scheelite 4 (Sch4) occurs as rims around Sch3 (Figure 5j) or as micro-fractures within Sch3 with light-CL (Figure 5k). The occurrence of micro-fractures in Sch3, which are filled with Sch4, indicates recrystallization during late hydrothermal processes. The formation of Sch4 is accompanied by the precipitation of molybdenite and other sulfides (chalcopyrite, pyrrhotite; Figure 5l).

3.2. Cathodoluminescence

Cathodoluminescence is an efficient technique for determining the zonation patterns and growth history of scheelite which are otherwise not unobservable using light microscopy. CL imaging of scheelite was obtained using a Gatan MonoCL 4 system attached to the FEI Nova NanoSEM 450 scanning electron microscope (FEI corporation, Hillsboro, OR, USA) at 10 kV, at the Institute of Geology, Chinese Academy of Geological Sciences, Beijing.

3.3. Electron Microprobe Analysis

Chemical compositions of scheelite were determined by electron probe microanalyses using a JEOL JXA-8230 Superprobe (JOEL Ltd., Akashima, Tokyo, Japan) at the Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing. The operating conditions were an accelerating voltage of 15 kV, a beam current of 10 nA, and a count time per element of 10 s for major elements. The quantitative analyses were performed with carbon-coated thin sections in an evacuated chamber with less than 4.0 ppm mbar. The following natural minerals and synthetic oxides were used for calibration: K-fedspar (K), jadeite (Na), apatite (P), wollastonite (Ca), hematite (Fe), MnO (Mn), scheelite (W), Cr2O3 (Cr), wulfenite (Mo), and rutite (Ti).

3.4. In situ LA-ICP-MS Trace Element Analysis

Trace element concentrations were determined by laser ablation–inductively coupled plasma–mass spectrometry (LA–ICP–MS) using a New Wave UP 213 laser ablation system coupled to a Thermo Element II single collector high-resolution magnetic sector (ICP–MS) at the National Research Center for Geoanalysis, Beijing, China. Helium is advantageous as a carrier gas and was thus applied in this study. Single-spot analyses were performed by laser-ablating spot diameters of 40 μm with a repetition rate of 10 Hz at an energy density of 23–25 J/cm2. Each LA-ICP-MS analysis incorporated a ~20 s background acquisition (gas blank) followed by a 60 s data acquisition from the sample. After every ten spots, analysis was followed by one NIST SRM 610 analysis to correct the time-dependent drift in sensitivity and mass discrimination of the ICP-MS. Reference glasses (GSE, NIST612, NIST614) were analyzed prior to and after the sample measurements. Calcium44 was used as an internal standard and fixed at 19.55 wt. %, based on the average EMPA composition.

4. Analytical Results

4.1. Major Element Geochemistry

Microprobe analyses of scheelite from the Xiaoyao tungsten deposit are shown in Table 2. The scheelite at Xiaoyao has a wide range of WO3 (66.67–80.45%), MoO3 (0.19–10.30%) contents, and CaO concentrations of 18.70–20.97% (Table 2 and Figure 6a). Sch1a in the proximal zone has low WO3 (68.95–73.87%) and CaO (18.75–20.97%) and high MoO3 (5.77–10.30%) contents, while Sch1b in the distal zone has high WO3 (79.78–79.88%) and CaO (19.51–19.59%) and low MoO3 (0.38–0.42%) contents. In the retrograde alteration stage, Sch2a has relatively high WO3 (76.59–78.13%) and CaO (18.70%–19.70%), and relatively low MoO3 (1.71–3.51%) contents, while Sch2b has low WO3 (70.03%–70.71 %) and CaO (19.25–20.93%), and high MoO3 (8.06–10.17%) contents. In the quartz–scheelite–sulfide stage, Sch3 has relatively low WO3 (66.67–74.55%) and CaO (19.00–20.83 %), and relatively high MoO3 (4.09–9.78%) contents. Sch4 has relatively high WO3 (79.13–80.48%) and CaO (18.73–19.70%), and relatively low MoO3 (0.19–0.76%) contents (Table 2 and Figure 6a).

4.2. Trace Element Geochemistry.

The representative trace element analyses from LA-ICP-MS on garnet, pyroxene and scheelite are listed in Table 3; and the chondrite-normalized REE patterns are shown in Figure 7.
Garnet is characterized by a slight LREE enrichment relative to HREE with low LREE/HREE ratios of 1.4–3.0 (Figure 7a,b), and the total REE contents are 85.9–91.0 ppm, accompanied by Eu/Eu* values of 0.57–0.62. In addition, garnet has W contents of 219–384 ppm, Mo contents of 4.2–7.4 ppm, and Y contents of 15.7–33.2 ppm. Pyroxene is characterized by HREE enrichment relative to LREE, with low LREE/HREE ratios of 0.5 (Figure 7c,d), and the total REE contents are 8.1–8.2 ppm, accompanied by varying Eu/Eu* values of 0.56–2.41. In addition, pyroxene has Sr contents of 7.4–11.7 ppm and Y contents of 4.9–5.0 ppm.
Sch1a is characterized by a typical right-inclined REE pattern with high LREE/HREE ratios of 16.9–41.0 (Figure 7a,b), and the total REE contents are 93.8–280.2 ppm, accompanied by the lowest Eu/Eu* values of 0.22–0.33. In addition, Sch1a has Sr contents of 67.0–87.1 ppm, Y contents of 2.0–3.5 ppm. As contents of 3.3–11.0 ppm, and high Ta contents of 779.4–863.9 ppm. Sch1b is characterized by an HREE-enrichment pattern with low LREE/HREE ratios of 0.3–0.7 (Figure 7c,d), and the total REE contents are 237.3–454.4 ppm, accompanied by Eu/Eu* values of 0.34–0.57. The Sr contents of 76.7–110.2 ppm, Y contents of 143.3–496.8 ppm. As contents of 4.3–12.9 ppm, Ta contents of 1397.2–1568.9 ppm in the Sch1b are generally higher than those of Sch1a.
Sch2a displays the same pattern, with high LREE/HREE ratios of 16.0–47.8, lower total REE contents of 21.2–186.5 ppm, and higher Eu/Eu* values of 0.50–1.09, compared with Sch1a (Figure 7a,b). The Y contents of 0.4–1.9 ppm and Y/Ho values of 13.78–20.43 in Sch2a are lower than those of Sch1a. However, Sch2a has higher Sr contents of 73.2–89.7 ppm and Ta contents of 860.2–928.0 ppm. Sch2b is characterized by an LREE-enrichment pattern with low LREE/HREE ratios of 0.7–2.1 (Figure 7c,d) and the total REE contents are 256.7–600.8 ppm, accompanied by Eu/Eu* values of 0.50–0.77. In addition, Sch2b has higher Sr contents of 117.7–159.6 pm and as contents of 6.2–18.5 ppm; however, compared with Sch1b, Sch2b is relatively depleted in Y contents of105.5–195.5 ppm and Ta contents of 1124.9–1359.4 ppm.
Sch3 has different REE patterns in a single grain and varying total REE contents of 162.9–890.1 ppm (Figure 7e–h). The change from core to rim in a single Sch3 grain shows a systematic change from negative to positive Eu-anomaly (Eu/Eu* = 0.51–4.89) and progressive increase in the LREE/HREE ratios of 2.5–96.2 (Figure 7e–f). Compared with Sch2a, Sch3 have higher Sr contents of 92.0–185.8 ppm and Y contents of 3.0–142.6 ppm.
Sch4 displays the same REE patterns as the core of Sch3 with low LREE/HREE ratios of 8.4–11.9, lower total REE contents of 188.6–249.1 ppm and Eu/Eu* ratios of 0.40–0.73, compared with those of Sch3 (Figure 7g,h). Sch4 has lower Sr contents, 87.6–89.2 ppm, and Y contents, 7.9–16.4 ppm, than those of Sch3.

5. Discussion

5.1. Oxidation State of Ore-Forming Fluids

Molybdenum cation Mo6+ enters scheelite by substituting W6+ under high fO2 conditions; under low fO2 and high fS2 conditions, Mo6+ is reduced to Mo4+ and precipitates as molybdenite. Thus, the molybdenum contents within scheelite crystals can be used to indicate the oxidation conditions of ore-forming fluids [34,35,36]. In the proximal zone, the MoO3 contents of Sch1a are high with 5.77–10.30%, indicating oxidized conditions (Figure 8A). The redox state of early ore-forming fluids could be inherited from magmas, and Xiaoyao granodiorite is oxidized. The existence of accessory magnetite in the Xiaoyao granodiorite indicates that the magmas had a high oxygen fugacity. Sch1b in the distal zone has lower MoO3 contents of 0.38–0.42% (Table 2 and Figure 8B). The carbonaceous wall rocks may lessen the effects of such a relatively oxidized magma [17,18]. However, the lack of association between molybdenite and Sch1b under reduced conditions suggests that the ore solution may be already depleted in molybdenum and/or under low fS2 conditions [34]. The activity of molybdenum decreases from the proximal zone to the distal zone [16]. In addition, Sch2b and Sch3 have higher MoO3 contents (8.07–10.17% and 4.09–9.78%, respectively), compared with Sch1b and Sch2a (Table 2 and Figure 8E–G). The late oxidized Mo-rich granodiorite dike overprints the sample location of Sch2b (Figure 3), and Sch2b and Sch3 have the same REE patterns with ore-related granodiorite (Figure 7d,f). The elevated Mo content may be provided by the high oxidation state, as well as an overprinting or remobilization of the oxidized Mo-rich magmatic-hydrothermal system [17]. However, Sch2a and Sch4 have low MoO3 contents (1.71–3.51% and 0.19–0.76%, respectively), accompanied by MoS2 precipitation (Figure 8C,H). These variations may be related to low fO2 and high fS2, caused by fluid–rock interaction. Furthermore, the precipitation of Mo-rich scheelite likely resulted in a Mo-depletion in residual fluids. The varying redox state of ore-forming fluids is influenced by the replenishment of oxidized Mo-rich magmatic-hydrothermal fluids and various interactions with carbonaceous wall rocks.
The presented results indicate a positive correlation between Mo and Cd in the scheelite (Figure 9a); therefore, the Cd content in scheelite increases under oxidized conditions. In contrast, under reduced conditions, the Cd content of scheelite decreases. This is corroborated by the changing valence state of Cd in an evolving ore forming fluid. Cd has two valence states, i.e. +1 and +2. Cd migrates as Cd1+ and its ionic radius is 1.14 Å; Cd migrates as Cd2+ and its ionic radius is 0.97 Å [37]. Cd2+ has the same valence states as Ca2+ and its ionic radius is close to 0.99 Å of Ca2+ and preferentially enters scheelite by substituting Ca2+ in fluids under oxidized conditions. The Cd average content of scheelite in the proximal skarn is 5.60 ppm, while, in the distal skarn, it is 0.15 ppm (Table 3), indicating lower oxidized conditions in the distal zone. These results are consistent with the lower Mo contents of the distal zone. This suggests that, in addition to the Mo content, the Cd content of scheelite can also be used to estimate the redox conditions of ore-forming fluids.

5.2. Disequilibrium Processes in Scheelite.

5.2.1. Dissolution and Re-Precipitation

The majority of the analyzed skarn-related scheelite has been extensively modified by dissolution and re-precipitation (DRP) processes. The high-Mo primary Sch1a is replaced to various extents by a secondary variety along fractures and/or grain boundaries (Figure 8A,B). This high-Mo Sch1a may have originally formed at high temperatures and under relatively oxidizing conditions. Furthermore, it was subsequently modified through the decrease in MoO3 contents and molybdenite precipitation, caused by a partial reduction of Mo6+ to Mo4+ in response to decreasing fO2. Secondary Sch2a is generally in sharp contact with the primary Sch1a and intergrown with molybdenite (Figure 8C). Low-Mo Sch1b has been modified by DRP processes (Figure 8D,E) through increases om MoO3 contents, caused by the substitution of W6+ and Mo6+ in response to increasing fO2. The replacement of garnet released large amounts of calcium ion into the ore-forming fluid and thus raised the activity of calcium ion in solution. Consequently, this led to a disequilibrium between precipitated scheelite and evolving fluids [16,17]. In addition, the W contents of garnet from the Xiaoyao deposit are 219–384 ppm (Table 3); therefore, garnet breakdown can lead to disequilibrium. Fluid–rock interaction led to the dissolution of the primary scheelite and the formation of secondary varieties [35]. These have been identified as important components in the formation of Xiaoyao tungsten skarn and similar deposits in the same district. Carbonate rocks contributed to an increase in the Ca contents of ore-forming fluids, enhanced WO42− solubility, and consequently led to disequilibrium. In addition, the re-equilibration of scheelite must have resulted in an increase in the extent of grain boundaries. This is favorable for fluid infiltration and further promotes the dissolution and re-precipitation of scheelite.

5.2.2. Recrystallization

Sch3 displays a homogeneous core and growth zoning rim (Figure 8F,G). In this study, scheelite grains with distinctive texture comprise a Mo-rich core, and a low-Mo rim (Figure 8F,G). Both generations have significantly different trace element compositions (Figure 7e–h). Both the oxidation state and the types of REE complexing may also be important during the recrystallization of scheelite and may have caused the observed LREE/HREE fractionation. Sch3 grains were modified by DRP processes and were replaced to various extents by Sch4 along fractures together with MoS2 and other sulfide precipitations (e.g., chalcopyrite and pyrrhotite) (Figure 8H). Therefore, scheelite from the Xiaoyao tungsten skarn deposit can be concluded to have undergone complex re-equilibration processes, where the precursor scheelite was partially modified or locally completely destroyed. Identification of such multiple re-equilibration processes reflects the dynamic changes in the fluid systems that are responsible for tungsten skarn formation.

5.3. Control of Chemical Variation in Scheelite.

Scheelite contains multiple groups of trace elements, such as REEs, LILEs (Sr and Pb), Mo, As, and HFSEs (Y, Nb, and Ta) (Table 3). Scheelite can incorporate significant amounts of REEs, Sr, Pb, and Y because of substitution for Ca2+, while Mo, As, Nb and Ta enter scheelite via substitution for W6+ [5]. Subtle variations in the trace element geochemistry of scheelite samples from this study were found between sample locations and scheelite types; the most significant include variations in Mo, Sr, Y, LREEs, and HREEs.
Different substitution mechanisms lead to different chondrite-normalized REE patterns of scheelites [5]. Three main mechanisms have been identified as responsible for REE substitution [5]: (1) 2Ca2+ = REE3+ + Na+; (2) Ca2+ + W6+ = REE3+ + Nb5+; and (3) 3 Ca2+ = 2 REE3+ + Ca, where Ca is a Ca-site vacancy. Regarding mechanism (1), MREEs preferentially substitute into a Ca site because of their similar ionic radii if Na is available to provide the charge balance in scheelite. Mechanism (2) requires that scheelites are Nb5+-enriched and have Nb contents close to the ΣREEs, with a positive correlation of Nb5+ and Nd3+ [6]. As shown in Figure 7, none of the scheelites from Xiaoyao display MREE-enriched REE patterns, and contain very low Nb contents of 1.33–38.45 ppm, which are much lower than their REE contents of 21–1032 ppm (Table 3). This indicates that mechanism (3) is more applicable than either (1) or (2). Because of the vacancy in mechanism (3), the restrictions of ionic radii were slightly modified, and the scheelite may inherit its REE composition from ore-forming fluids [9]. Sch1a, Sch2a, Sch3, and Sch4 in the proximal zone display LREE-enriched and slightly HREE-depleted patterns (Figure 7). These are similar to the pattern of ore-related granodiorite, indicating that the scheelites inherited REE compositions from magmatic-hydrothermal fluids. However, they have higher LREE/HREE ratios compared with the ore-related granodiorite which may be caused by the precipitation of skarn minerals with low LREE/HREE ratios of 1.4–3.0 (Figure 7b). Many researchers reported that the REE patterns of skarn-type scheelites are enriched in LREEs but depleted in HREEs, which is likely caused by the precipitation of HREE-rich skarn minerals [9]. Prominent examples include the Zhuxi and Jitoushan tungsten skarn deposits in the JNB [9] and the Kyanigan tungsten skarn deposit in the Mogok metamorphic belt, Myanmar [39]. However, the Sch1b and Sch2b of the distal zone with low LREE/HREE ratios of 0.3–2.1 were identified by their distinctive REE fractionation patterns (Figure 7d). Such low LREE/HREE ratios can be interpreted by several explanations. Firstly, mineral/mineral REE partitioning may have occurred. However, because pyroxene intergrowth with scheelite has much lower REE contents of 0.6–13.1 ppm (Table 3), this is insufficient to change the LREE/HREE ratios, and thus REE partitioning cannot be explained via this process. Secondly, if the HREE-enriched patterns were assumed to be inherited from the ore-forming fluids, the ore-forming fluids should be HREE-enriched; in contrast to the LREE-enriched patterns of ore-related granodiorite, the inherited process cannot be explained. Thirdly, a minor distortion in Ca2+ will result in a shift from LREE enrichment to HREE enrichment, depending on the reduction in the relative size of the crystallographic site from light to heavy REE (i.e., from 1.12 A˚ to 1.00 A˚) [40]. The extensive replacement of Ca2+ for Sr2+ may be linked to site distortions because of differences in their ionic radii (Ca2+, 1.12 A˚; Sr2+, 1.26 A˚) [40]. Sch1b and Sch2b in the distal zone are characterized by low LREE/HREE ratios and relatively low Sr contents of 76.7–159.6 ppm. Both display a positive correlation between LREE/HREE ratios and Sr contents (Figure 8b), which may be slightly influenced by Ca2+ site distortions.
Moreover, changes from LREE- to HREE-enrichment correlate with variation in MoO3 contents in the distal zone (Figure 9c). This is corroborated by high MoO3 contents of 8.06–10.17% for Sch2b and low MoO3 contents of 0.38–0.42% for Sch1b in the distal zone (Table 2 and Figure 6a), suggesting that scheelites evolved from LREE-enrichment to HREE-enrichment because of a shift in fO2. This is consistent with the change from HREE-enrichment to LREE-enrichment because of a shift in fO2 [41]. Figure 9a,b shows positive correlations between Mo and (La/Lu)N in scheelite from Xiaoyao and in other tungsten skarn deposits. Furthermore, the positive correlations between Mo and LREEs (La, Ce, and Nd) (Figure 10a–c) gradually change to negative corrections between Mo and HREEs (Gd, Dy, and Ho) (Figure 10d–f). This indicates that the redox state may directly or indirectly influence the REE patterns of Sch1b and Sch2b.
Strontium concentrations of Sch1b in the distal zone (76–110 ppm) exceed those of Sch1a in the proximal zone (67–87 ppm; Figure 11e). Furthermore, the Sr contents of Sch2a, Sch2b, and Sch3 are higher compared with those of Sch1a and Sch1b (Figure 11e). This may be attributed to fluid–rock interactions, which, in general, elevate Sr contents due to Ca-bearing minerals such as carbonates (i.e., as a substitution for Ca2+) during wall-rock alteration by the tungsten-bearing fluid [42,43]. Many studies of tungsten deposits reported fluid–rock interactions as important processes during mineralization, especially in skarn deposits [44]. Studies of the Sr content and isotope on scheelite from the Felbertal tungsten deposit, Austria [45], and the Dahutang tungsten deposit [33] indicated that fluid–rock interaction and alterations in host rocks by granite-derived hydrothermal fluids can cause the observed Sr enrichment. The lower Sr concentrations of Sch4 in the quartz vein (Figure 11e) may be due to dilution via mixing of magmatic fluids with externally-derived (meteoric) fluids [40], which is consistent with the lower REE contents. The large variation in Sr contents in scheelite reflect the changing Sr composition of the mineralizing fluids, which is, in turn, influenced by fluid–rock interaction and fluid mixing.
Yttrium concentrations in scheelite also vary substantially (0.5–496.8 ppm; Figure 11a–d). Yttrium is positively correlated with REEs, LREEs, and especially HREEs (Figure 11b–d), which is likely because Y has a similar charge to REE3+ and a similar ionic radius in eightfold coordination (1.015 Å), near Ho (1.02 Å) [5]. Similar to HREE, Y also displays negative correlations with Mo (Figure 11a) and is related to the redox state. However, both Sch1a and Sch2a deviate from this correlation. Garnet intergrowth with Sch1a and Sch2a has significant Y contents (i.e., a Y content of 24.45 ppm; Table 3), suggesting that its precipitation may influence Y, which is depleted in Sch1a and Sch2a. Variations in Y concentrations in the Xiaoyao scheelite most likely relate to the redox state or the precipitation of Y-rich hydrothermal minerals.
Because of their similar charge and ionic radii, Y–Ho, Zr–Hf, and Nb–Ta pairs display coherent behavior and hold their respective chondritic ratios in mafic to intermediate rocks [46]. In the present study, Y and Ho are positively correlated with Y/Ho of 13.78–43.82, whereas Zr–Hf and Nb–Ta relationships displayed widely scattered patterns with Zr/Hf of 4.63–20.83 and Nb/Ta < 0.05 (Table 3). The positive correlation between Y and Ho suggests their similar chemical behavior in hydrothermal systems [46]. However, an explanation for the deviation of these ratios from the chondritic values is still under debate. These elements are mainly concentrated in minor/accessory minerals, the crystallization of which can modify the ratio [47]. Trace element fractionation by scheelite in the hydrothermal system leads to the variable non-chondritic Y/Ho and Zr/Hf ratios of scheelite [39]. The Y/Ho ratios of scheelite from Xiaoyao gradually increase (17.86–26.54, 13.70–34.50, and 22.32–43.82) from the skarn stage to the quartz vein stage. This may be due to fractionation caused by fluid-rock interaction and metasomatism [48] or the breakdown of skarn minerals with high Y/Ho (28.94–39.65, Table 3). The Zr/Hf ratios of scheelite increase (4.63–6.92 and 6.23–20.83) from the skarn stage to the retrograde alteration stage, which may be due to fractionation or the breakdown of skarn minerals with high Zr/Hf (average of 19.38, Table 3). The Zr/Hf ratios of scheelite decrease (5.37–10.33) in the quartz-vein stage, which may be due to the precipitation of hydrothermal zircon. This suggestion is supported by the mineral assemblage of hydrothermal zircon, which is intergrown with scheelite in the quartz-vein stage (Figure 5h). Compared with most geological materials (e.g., Nb/Ta of chondrites ~17.5; average continental crust ~11) [49], scheelites have a very low Nb/Ta ratio (<0.05), reflecting relatively high abundances of Ta. Fluid fractionation leads to an enrichment of Ta relative to Nb [50]. The data in this paper support this model and show that hydrothermal fluids efficiently fractionate the Nb/Ta ratio.
Based on the above textural and geochemical characteristics, the REE and trace element characteristics of scheelites are influenced by substitution mechanisms, fluid–rock interaction, redox state, fluid mixing, fluid fractionation, and mineral/mineral REE partitioning. The texture may reflect multiple fluid pluses with fluctuating chemical properties and depositional conditions and may indicate modification of the pre-existing scheelite by late-stage fluids in the ore-system.

5.4. Implication for Ore-Forming Processes

Granodiorite has a zircon U-Pb isotope age of 149.4 ± 1.1 Ma, which is consistent with the molybdenite Re-Os age (148.7 ± 2.5 Ma) at the Xiaoyao deposit, suggesting that it is genetically related to skarn formation and mineralization [28]. Paragenetic studies on textural and physicochemical data show that the Xiaoyao skarn may be classified as an oxidized tungsten deposit that can form in an evolving magmatic-hydrothermal system. Alterations and mineralizations at the Xiaoyao have been associated with calc-alkaline magmatic activity.
The tungsten-rich magmatic fluids migrated and interacted with wall rock, thus forming garnet skarns in the proximal zone and pyroxene skarns in the distal zone (Figure 3). Andradite is characterized by low LREE/HREE ratios and a negative Eu anomaly. The tungsten was incorporated into garnet, reaching high contents of 219−384 ppm (Table 3). The precipitation of garnet with low LREE/HREE ratios likely resulted in an enrichment of LREE and a depletion of HREE in the residual fluids. Sch1a in the proximal zone inherited magmatic-hydrothermal fluids with LREE enrichment, HREE depletion, and negative Eu anomaly (Table 3 and Figure 7b). The tungsten-rich magmatic fluids interacted with the carbonaceous wall rock, which may have led to lower fO2 in the distal Sch1b. The low fO2 can lead to HREE and Y enrichment in scheelite and an alteration in carbonate wall rocks by granite-derived hydrothermal fluids, which release high Sr contents. Sch1b in the distal zone is characterized by an HREE-enriched pattern with lower MoO3 contents, as well as higher Sr and Y contents (Table 3 and Figure 7d).
Following intensive fluid–rock interaction, the ore-forming fluids showed lower fO2. Replacement of garnet released large amounts of calcium ions into the ore-forming fluid, thus raising the activity of calcium ion in solution, and leading to the dissolution and re-precipitation of Sch1a and Sch1b, as well as the formation of Sch2a and Sch2b [16,17]. The lower fO2 resulted in a decrease in MoO3 contents in Sch2a. The HREE-depleted patterns of Sch1a and Sch2a were influenced by the precipitation of garnet with low LREE/HREE ratios (Figure 7b). The fluid–rock interaction and alteration in the host rocks by granite-derived hydrothermal fluids can cause Sr enrichment in Sch2a and Sch2b. Sch2a is characterized by HREE-depletion patterns with lower MoO3, and higher Sr contents (Table 3 and Figure 7b). As a result of the overlaying of the late oxidized granodiorite dike to the sample of Sch2b (Figure 3), the ore-forming fluids became higher in fO2. Sch2b displayed a similar pattern, with granodiorite with higher MoO3 and higher Sr contents (Table 3 and Figure 7d).
The subsequently appearing magmatic-hydrothermal fluids formed quartz-scheelite veins, which typically crosscut early tungsten skarn ores (Figure 5a). The ore-forming fluids increased in fO2 and interacted with the wall rock, thus causing the hydrothermal growth of Sch3. Sch3 exhibits a homogeneous core and growth zoning rim (Figure 5f−h). The homogeneous core of Sch3 displays a similar pattern to that of ore-related granodiorite, which further demonstrates that scheelite is derived from magmatic-hydrothermal fluids. The growth zoning rim displays a strong HREE-depletion pattern, similar to Sch1a and Sch2a, which may be caused by the precipitation of HREE-rich hydrothermal minerals. Continuing fluid–rock interaction can cause Sr enrichment. Sch3 is characterized by LREE-enrichment patterns with higher MoO3 contents, higher REE, Sr, and Y contents compared with Sch2a (Table 3 and Figure 7f). Mixing with meteoric water resulted in the recrystallization of Sch3 and formation of Sch4. Meteoric waters normally show very low contents of REE and trace elements, which could cause a decrease in REE and trace element contents of ore-forming fluid as a result of dilution. Sch4 has a similar pattern to Sch3, but has lower REE, Mo, Sr, and Y contents (Table 3 and Figure 7h). In addition, the hydrogen-oxygen isotope data from both the Jitoushan and Dongyuan deposits (which are closely situated to the Xiaoyao deposit) further demonstrate that the ore-forming fluids are mainly magmatic with the addition of meteoric water during the late stage [51,52].
In summary, textural and trace element signatures indicate a magmatic–hydrothermal formation model and the mechanism of tungsten ore enrichment. Fluid–rock interaction and fluid mixing may be important enrichment mechanisms that generated the Xiaoyao tungsten deposit.

6. Conclusions

(1)
Scheelite can record the following complex growth histories based on CL images: homogeneous Sch1a and Sch1b, dissolution and re-precipitation Sch2a and Sch2b, oscillatory zoning Sch3, and Sch4 in micro-fractures. These four types of scheelite have different MoO3 and Cd contents, indicating fluctuating changes in the oxygen fugacity from the skarn stage to the quartz vein stage;
(2)
Variations in REE patterns in scheelite are influenced by the REE patterns of ore-related granodiorite, the precipitation of hydrothermal minerals with low LREE/HREE ratios, and changing oxygen fugacity during fluid–rock interaction;
(3)
The increasing Sr contents and Y/Ho ratios of scheelite from the skarn stage to the quartz vein stage indicate continuing fluid–rock interaction. This fluid–rock interaction may be an important enrichment mechanism underlying the generation the Xiaoyao tungsten deposit.

Author Contributions

Q.S. contributed significantly to the data analyses and wrote the manuscript. J.M. conceived and designed the experiment and study design. J.S. helped improve discussions. L.Z. helped perform the trace element analyses experiment. S.X. provided very valuable help during field work. All authors have read and agreed to the published version of the manuscript.

Funding

National Nature Science Foundation of China (No. 41430314).

Acknowledgments

We are grateful to thank the editors and two anonymous reviewers for their critical and constructive comments and suggestions, which helped to improve the paper. We thank Xie Guiqing for his important help to improve the discussion. We are very grateful to Franco Pirajno to polish the language. We would like to thank Wen Wangfei, Fu Jianzhen, and their co-workers from the Anhui Bureau of Geology, Mineral Resources, Exploration and Development, and its affiliated No.332 Geological Team, for support and field help.

Conflicts of Interest

The authors declare no conflicts of interest.

References

  1. Allen, C.C.; Folinsbee, R.E. Scheelite veins related to porphyry intrusives Hollinger Mine. Econ. Geol. 1944, 39, 340–348. [Google Scholar] [CrossRef]
  2. Noble, S.; Spooner, E.T.; Harris, F. The Logtung large tonnage, low-grade W (scheelite)-Mo porphyry deposit, south-central Yukon Territory. Econ. Geol. 1984, 79, 848–868. [Google Scholar] [CrossRef]
  3. Brugger, J.; Bettiol, A.; Costa, S.; Lahaye, Y.; Bateman, R.; Lambert, D.; Jamieson, D. Mapping REE distribution in scheelite using luminescence. Mineral. Mag. 2000, 64, 891–903. [Google Scholar] [CrossRef]
  4. Hazarika, P.; Mishra, B.; Pruseth, K.L. Scheelite, apatite, calcite and tourmaline compositions from the late Archean Hutti orogenic gold deposit: Implications for analogous two stage ore fluids. Ore Geol. Rev. 2016, 72, 989–1003. [Google Scholar] [CrossRef]
  5. Ghaderi, M.; Palin, J.M.; Campbell, I.H.; Sylvester, P.J. Rare earth element systematics in scheelite from hydrothermal gold deposits in the Kalgoorlie-Norseman region, Western Australia. Econ. Geol. 1999, 94, 423–437. [Google Scholar] [CrossRef]
  6. Dostal, J.; Kontak, D.J.; Chatterjee, A. Trace element geochemistry of scheelite and rutile from metaturbidite-hosted quartz vein gold deposits, Meguma Terrane, Nova Scotia, Canada, Genetic implications. Mineral. Petrol. 2009, 97, 95–109. [Google Scholar] [CrossRef]
  7. Zhang, Z.Y.; Xie, G.Q.; Mao, J.W.; Liu, W.G.; Olin, P.; Li, W. Sm-Nd dating and in-situ LA-ICP-MS trace element analyses of scheelite from the Longshan Sb-Au deposit, Xiangzhong metallogenic Province, South China. Minerals 2019, 9, 87. [Google Scholar] [CrossRef] [Green Version]
  8. Zhu, L.Y.; Jiang, S.Y.; Chen, R.S.; Ma, Y. Origin of the Shangfang Tungsten deposit in the Fujian Province of Southeast China: Evidence from scheelite Sm-Nd geochronology, H-O isotopes and fluid inclusions studies. Minerals 2019, 9, 713. [Google Scholar] [CrossRef] [Green Version]
  9. Song, G.X.; Qin, K.Z.; Li, G.M.; Evans, N.J.; Chen, L. Scheelite elemental and isotopic signatures: Implications for the genesis of skarn-type W-Mo deposits in the Chizhou Area, Anhui Province, Eastern China. Am. Mineral. 2014, 99, 303–317. [Google Scholar] [CrossRef]
  10. Poulin, R.S.; McDonald, A.M.; Kontak, D.J.; McClenaghan, M.B. On the relationship between cathodoluminescence and the chemical composition of scheelite from geologically diverse ore-deposit environments. Can. Mineral. 2016, 54, 1147–1173. [Google Scholar] [CrossRef]
  11. Sciuba, M.; Beaudoin, G.; Grzela, D.; Makvandi, S. Trace element composition of scheelite in orogenic gold deposits. Miner. Depos. 2019, 1–24. [Google Scholar] [CrossRef]
  12. Li, J.D.; Li, X.F.; Xiao, R. Multiple-Stage tungsten mineralization in the Silurian Jiepai W skarn deposit, South China: Insights from cathodoluminescence images, trace elements, and fluid inclusions of scheelite. J. Asian Earth Sci. 2019, 181, 1–22. [Google Scholar] [CrossRef]
  13. Yuan, L.L.; Chi, G.X.; Wang, M.Q.; Li, Z.H.; Xu, D.R.; Deng, T.; Geng, J.Z.; Hu, MY.; Zhang, L. Characteristics of REEs and trace elements in scheelite from the Zhuxi W deposit, South China: Implications for the ore-forming conditions and processes. Ore Geol. Rev. 2019, 109, 585–597. [Google Scholar] [CrossRef]
  14. Wu, S.H.; Mao, J.W.; Ireland, T.R.; Zhao, Z.; Yao, F.J.; Yang, Y.P.; Sun, W.D. Comparative geochemical study of scheelite from the Shizhuyuan and Xianglushan tungsten skarn deposits, South China: Implications for scheelite mineralization. Ore Geol. Rev. 2019, 109, 448–464. [Google Scholar] [CrossRef]
  15. Sun, K.K.; Chen, B.; Deng, J. Ore genesis of the Zhuxi supergiant W-Cu skarn polymetallic deposit, South China: Evidence from scheelite geochemistry. Ore Geol. Rev. 2019, 107, 14–29. [Google Scholar] [CrossRef]
  16. Kwak, T.A.P.; Tan, T.H. The geochemistry of zoning in skarn minerals at the King Island (Dolphin) mine. Econ. Geol. 1981, 76, 468–497. [Google Scholar] [CrossRef]
  17. Newberry, R.J. W-and Sn-Skarn Deposits: A 1998 Status Report. Miner. Intrusion-Relat. skarn Syst. 1998, 26, 289–335. [Google Scholar]
  18. Meinert, L.D.; Dipple, G.M.; Nicolescu, S. World skarn deposits. Econ. Geol. 2005, 100, 299–336. [Google Scholar]
  19. Wang, D.E.; Zhou, X.; Yu, X.Q.; Du, Y.D.; Yang, H.M.; Fu, J.Z.; Dong, H.M. SHRIMP zircon U-Pb dating and characteristics of Hf isotopes of the granodiorite porphyries in the Dongyuan W-Mo ore district, Qimen area, southern Anhui. Geol. Bull. China 2011, 30, 1514–1529. (In Chinese) [Google Scholar]
  20. Xiang, X.K.; Wang, P.; Sun, D.M.; Zhong, B. Re-Os isotopic age of molybdeinte from the Shimensi tungsten polymetallic deposit in northern Jiangxi province and its geological implications. Geol. Bull. China 2013, 32, 1824–1831. (In Chinese) [Google Scholar]
  21. Mao, J.W.; Xiong, B.K.; Liu, J.; Pirajno, F.; Cheng, Y.B.; Ye, H.S.; Song, S.W.; Dai, P. Molybdenite Re/Os dating, zircon U-Pb age and geochemistry of granitoids in the Yangchuling porphyry W-Mo deposit (Jiangnan tungsten ore belt), China: Implications for petrogenesis, mineralization and geodynamic setting. Lithos 2017, 286–287, 35–52. [Google Scholar] [CrossRef]
  22. Mao, Z.H.; Cheng, Y.B.; Liu, J.J.; Yuan, S.D.; Wu, S.H.; Xiang, X.K.; Luo, X.H. Geology and molybdenite Re-Os age of the Dahutang granite-related veinlets-disseminated tungsten ore field in the Jiangxin Province, China. Ore Geol. Rev. 2013, 53, 422–433. [Google Scholar] [CrossRef]
  23. Chen, G.H.; Shu, L.S.; Shu, L.M.; Zhang, C.; Ouyang, Y.P. Geological characteristics and mineralization setting of the Zhuxi tungsten (copper) polymetallic deposit in the Eastern Jiangnan Orogen. Sci. China Earth Sci. 2015, 45, 1799–1818. (In Chinese) [Google Scholar] [CrossRef]
  24. Mao, Z.H.; Liu, J.J.; Mao, J.W.; Deng, J.; Zhang, F.; Meng, X.Y.; Xiong, B.K.; Xiang, X.K.; Luo, X.H. Geochronology and geochemistry of granitoids related to the giant Dahutang tungsten polymetallic deposit, middle Yangtze River region, China: Implications for petrogenesis, geodynamic setting, and mineralization. Gondwana Res. 2015, 28, 816–836. [Google Scholar] [CrossRef]
  25. Song, S.W.; Mao, J.W.; Xie, G.Q.; Chen, L.; Santosh, M.; Chen, G.H.; Rao, J.F.; Ouyang, Y.P. In situ LA-ICP-MS U-Pb geochronology and trace element analysis of hydrothermal titanite from the giant Zhuxi W (Cu) skarn deposit, South China. Miner. Depos. 2019, 54, 569–590. [Google Scholar] [CrossRef]
  26. Song, S.W.; Mao, J.W.; Zhu, Y.F.; Yao, Z.Y.; Chen, G.H.; Rao, J.F.; Ouyang, Y.P. Partial-Melting of fertile metasedimentary rocks controlling the ore formation in the Jiangnan porphyry-skarn tungsten belt, South China: A upcletn, case study at the giant Zhuxi W-Cu skarn deposit. Lithos 2018, 304, 180–199. [Google Scholar] [CrossRef]
  27. Team, No. 332. Exploration Report of the Xiaoyao Tungsten Polymetallic Deposit, Jixi County, Anhui Province; Anhui Bureau of Geology and Mineral Resources: Anhui, China, 2011. [Google Scholar]
  28. Su, Q.W.; Mao, J.W.; Wu, S.H.; Zhang, Z.C.; Xu, S.F. Geochronology and geochemistry of the granitoids and ore-forming age in the Xiaoyao tungsten polymetallic skarn deposit in the Jiangnan Massif tungsten belt, China: Implications for their petrogenesis, geodynamic setting, and mineralization. Lithos 2018, 296–299, 365–381. [Google Scholar] [CrossRef]
  29. Chen, F.; Wang, D.H.; Du, J.G.; Xu, W.; Hu, H.F.; Yu, Y.L.; Tang, J.L. New dating of the fuling granite body with LA-ICP-MS zircon U-Pb in Jixi, Anhui Province and their geological significance. Rock Miner. Anal. 2013, 32, 970–977. (In Chinese) [Google Scholar]
  30. Sun, K.K.; Chen, B. Trace elements and Sr-Nd isotopes of scheelite: Implications for the W-Cu-Mo polymetallic mineralization of the Shimensi deposit, South China. Am. Mineral. 2017, 102, 1114–1128. [Google Scholar]
  31. Zaw, K.; Singoyi, B. Formation of magnetite-scheelite skarn mineralization at Kara, Northwestern Tasmania: Evidence from mineral chemistry and stable Isotopes. Econ. Geol. 2000, 95, 1215–1230. [Google Scholar] [CrossRef]
  32. Timon, S.S.M.; Moro, B.M.C.; Cembranos, P.M.L. Mineralogical and physiochemical evolution of the Los Santos scheelite skarn, Salamanca, NW Spain. Econ. Geol. 2009, 104, 961–995. [Google Scholar]
  33. Sun, S.S.; Mcdonough, W.F. Chemical and isotopic systematics of oceanic basalts: Implications for mantle composition and processes. Geol. Soc. Lond. Spec. Publ. 1989, 42, 313–345. [Google Scholar] [CrossRef]
  34. Hsu, L.C.; Galli, P.E. Origin of the scheelite-powellite series of minerals. Econ. Geol. 1973, 68, 681–696. [Google Scholar] [CrossRef]
  35. Rempel, K.U.; Williams-Jones, A.E.; Migdisov, A.A. The partitioning of molybdenum (VI) between aqueous liquid and vapour at temperatures up to 370 °C. Geochim. Cosmochim. Acta 2009, 73, 3381–3392. [Google Scholar] [CrossRef]
  36. Xu, J.; Ciobanu, C.L.; Cook, N.J.; Slattery, A. Crystals from the powellite-scheelite series at the nanoscale: A case study from the Zhibula Cu Skarn, Gangdese Belt, Tibet. Minerals 2019, 9, 340. [Google Scholar] [CrossRef] [Green Version]
  37. Liu, Y.; Cao, L.; Li, Z.; Wang, H.; Chu, T.; Zhang, J. Element Geochemistry; Science Press: Beijing, China, 1984; p. 548. [Google Scholar]
  38. Liu, B.; Li, H.; Wu, Q.H.; Evans, N.J.; Cao, J.Y.; Jiang, J.B.; Wu, J.H. Fluid evolution of Triassic and Jurassic W mineralization in the Xitian ore field, South China: Constraints from scheelite geochemistry and microthermometry. Lithos 2019, 330–331, 1–15. [Google Scholar] [CrossRef]
  39. Guo, S.; Chen, Y.; Liu, C.; Wang, J.; Su, B.; Gao, Y.; Wu, F.; Sein, K.; Yang, Y.; Mao, Q. Scheelite and coexisting F-rich zoned garnet, vesuvianite, fluorite, and apatite in calc-silicate rocks from the Mogok metamorphic belt, Myanmar: Implications for metasomatism in marble and the role of halogens in W mobilization and mineralization. J. Asian Earth Sci. 2016, 117, 82–106. [Google Scholar] [CrossRef]
  40. Poulin, R.S.; Kontak, D.J.; McDonald, A.; Beth, M.; McCLenaghan, B.M. Assessing Scheelite as an ore-deposit discriminator using its trace-element REE chemistry. Can. Mineral. 2018, 56, 265–302. [Google Scholar] [CrossRef]
  41. Ismail, R.; Ciobanu, C.; Cook, N.J.; Teale, G.S.; Giles, D.; Mumm, A.S.; Wade, B. Rare earths and other trace elements in minerals from skarn assemblages, Hillside iron oxide-copper-gold deposit, Yorke Peninsula, South Australia. Lithos 2014, 184–187, 456–477. [Google Scholar] [CrossRef]
  42. Kinsman, D.J.J. Interpretation of Sr2+ concentrations in carbonate minerals and rocks. J. Sediment. Petrol. 1969, 39, 486–508. [Google Scholar]
  43. Friedmann, I.; O’Neil, J.R. Compilation of stable isotope fractionation factors of geochemical interest: Chapter KK. In Data of Geochemistry, 6th ed.; Fleischer, M., Ed.; U.S. Geological Survey Professional Paper; U.S. Government Printing Office: Washington, DC, USA, 1977; Volume 440, p. 12. [Google Scholar]
  44. Lecumberri-Sanchez, P.; Vieira, R.; Heinrich, C.A.; Pinto, F.; Wälle, M. Fluid-Rock interaction is decisive for the formation of tungsten deposits. Geology 2017, 45, 579–582. [Google Scholar] [CrossRef]
  45. Kozlik, M.; Gerdes, A.; Raith, J.G. Strontium isotope systematics of scheelite and apatite from the Felbertal tungsten deposit, Austria-results of in-situ LA-MC-ICP-MS analysis. Miner. Pet. 2016, 110, 11–27. [Google Scholar] [CrossRef]
  46. Burt, D.M. Compositional and phase relations among rare earth elements. Rev. Mineral. 1989, 21, 259–307. [Google Scholar]
  47. Schmidt, M.W.; Dardon, A.; Chazot, G.; Vannucci, R. The dependence of Nb and Ta rutile-melt partitioning on melt composition and Nb/Ta fractionation during subduction processes. Earth Planet Sci. Lett. 2004, 226, 415–432. [Google Scholar] [CrossRef]
  48. Yaxley, G.M.; Green, D.H.; Kamenetsky, V. Carbonatite metasomatism in the southeastern Australian lithosphere. J. Petrol. 1998, 39, 1917–1930. [Google Scholar] [CrossRef]
  49. Taylor, S.R.; McLennan, S.M. The Continental Crust: Its Composition and Evolution; Blackwell: Oxford, UK, 1985; p. 312. [Google Scholar]
  50. Dostal, J.; Chatterjee, A.K. Contrasting behaviour of Nb/Ta and Zr/Hf ratios in a peraluminous granitic pluton (Nova Scotia, Canada). Chem. Geol. 2000, 123, 67–88. [Google Scholar] [CrossRef]
  51. Du, Y.D.; Liu, J.J.; Yu, X.Q.; Zhou, X.; Yang, H.M.; Yang, L.B.; Huang, Y.H. The sources of metallogenic materials and mineralization of the Xiaoyao W polymetallic deposit in Anhui Province: Evidence from carbon, sulfur and lead isotopes. Geol. China 2013, 40, 566–579. (In Chinese) [Google Scholar]
  52. Song, G.X.; Qin, K.Z.; Li, G.M.; Li, X.H.; Qu, W.J. Geochronology and ore-forming fluids of the Baizhangyan W-Mo deposit in the Chizhou area, middle-lower Yangtze valley, SE-China. Resour. Geol. 2012, 63, 57–71. [Google Scholar] [CrossRef]
Minerals 10 00271 g001 550
Figure 1. Distribution of the Middle-Lower Yangtze River Valley porphyry-skarn Cu-Au-Mo-Fe ore belt at north and the Jiangnan porphyry-skarn tungsten belt at the south [21].
Figure 1. Distribution of the Middle-Lower Yangtze River Valley porphyry-skarn Cu-Au-Mo-Fe ore belt at north and the Jiangnan porphyry-skarn tungsten belt at the south [21].
Minerals 10 00271 g001
Minerals 10 00271 g002 550
Figure 2. Geological map of the Xiaoyao tungsten deposit [27].
Figure 2. Geological map of the Xiaoyao tungsten deposit [27].
Minerals 10 00271 g002
Minerals 10 00271 g003 550
Figure 3. Geological cross-section along exploration No. 47 (A-A’ in Figure 2) of the Xiaoyao tungsten deposit [27].
Figure 3. Geological cross-section along exploration No. 47 (A-A’ in Figure 2) of the Xiaoyao tungsten deposit [27].
Minerals 10 00271 g003
Minerals 10 00271 g004 550
Figure 4. Photographs of tungsten ores. (a) Garnet skarn with disseminated scheelite; (b) Pyroxene skarn with disseminated scheelites; (c) Retrograde alteration skarn; (d) Quartz–scheelite–sulfides vein cutting the garnet skarn; (e) Quartz vein scheelite replaced pyroxene and garnet; (f) Quartz vein scheelite with blue luminescence under ultraviolet light. Grt—garnet; Px—pyroxene; Chl—chlorite; Sch—scheelite; Qz—quartz.
Figure 4. Photographs of tungsten ores. (a) Garnet skarn with disseminated scheelite; (b) Pyroxene skarn with disseminated scheelites; (c) Retrograde alteration skarn; (d) Quartz–scheelite–sulfides vein cutting the garnet skarn; (e) Quartz vein scheelite replaced pyroxene and garnet; (f) Quartz vein scheelite with blue luminescence under ultraviolet light. Grt—garnet; Px—pyroxene; Chl—chlorite; Sch—scheelite; Qz—quartz.
Minerals 10 00271 g004
Minerals 10 00271 g005 550
Figure 5. Light, Back scattered Electron (BSE) and Cathodoluminescence (CL) images of scheelites. (a) Sch1a intergrowth with garnet with transmitted light; (b) CL image of Sch1a with homogeneous texture; (c) CL images of Sch1a replaced/overgrowth by Sch2a; (d) BSE images of Sch2a intergrowth with molybdenite; (e) Pyroxene replaced by scheelite with transmitted light; (f) CL images of Sch1b replaced/overgrowth by Sch2b; (g) Retrograde alteration stage scheelite with transmitted light; (h) CL images of Sch1a replaced/overgrowth by Sch2a; (i) Transmitted light image of Sch3-rich quartz vein; (j) Core-rim texture revealed by CL image of Sch3 with Sch1, and Sch4 filled within microfractures of Sch3; (k) CL image of Sch4 filled within microfractures of Sch3 with oscillatory growth zoning; (l) BSE image of Sch4 intergrowth with molybdenite. Sch—scheelite; Mo—molybdenite; Grt—garnet; Px—pyroxene; Chl—chlorite; Qz—quartz; Zrn—zircon.
Figure 5. Light, Back scattered Electron (BSE) and Cathodoluminescence (CL) images of scheelites. (a) Sch1a intergrowth with garnet with transmitted light; (b) CL image of Sch1a with homogeneous texture; (c) CL images of Sch1a replaced/overgrowth by Sch2a; (d) BSE images of Sch2a intergrowth with molybdenite; (e) Pyroxene replaced by scheelite with transmitted light; (f) CL images of Sch1b replaced/overgrowth by Sch2b; (g) Retrograde alteration stage scheelite with transmitted light; (h) CL images of Sch1a replaced/overgrowth by Sch2a; (i) Transmitted light image of Sch3-rich quartz vein; (j) Core-rim texture revealed by CL image of Sch3 with Sch1, and Sch4 filled within microfractures of Sch3; (k) CL image of Sch4 filled within microfractures of Sch3 with oscillatory growth zoning; (l) BSE image of Sch4 intergrowth with molybdenite. Sch—scheelite; Mo—molybdenite; Grt—garnet; Px—pyroxene; Chl—chlorite; Qz—quartz; Zrn—zircon.
Minerals 10 00271 g005
Minerals 10 00271 g006 550
Figure 6. Plots of WO3 vs. MoO3 of Xiaoyao scheelites (a) and scheelites from other porphyry-skarn tungsten deposits are shown for comparison (b), including the Dahutang tungsten deposit [30], the Jitoushan and Baizhangya tungsten deposits [9], the King-Island-oxidized skarn deposit [17], the Kara-oxidized skarn deposit [31], and the Los-Santos-reduced skarn deposit [32].
Figure 6. Plots of WO3 vs. MoO3 of Xiaoyao scheelites (a) and scheelites from other porphyry-skarn tungsten deposits are shown for comparison (b), including the Dahutang tungsten deposit [30], the Jitoushan and Baizhangya tungsten deposits [9], the King-Island-oxidized skarn deposit [17], the Kara-oxidized skarn deposit [31], and the Los-Santos-reduced skarn deposit [32].
Minerals 10 00271 g006
Minerals 10 00271 g007 550
Figure 7. Chondrite-normalized REE patterns of scheelites from Xiaoyao deposit. (a) and (b) are Sch1a and Sch2a in the garnet skarn, sample 15XY-31; (c) and (d) are Sch1b and Sch2b in the pyroxene skarn, sample 15XY-14; (e–h) are Sch3 and Sch4 hosted in scheelite-rich quartz veins, sample 15XY-29. The chondrite values are from [33]. The granodiorite data are from [28].
Figure 7. Chondrite-normalized REE patterns of scheelites from Xiaoyao deposit. (a) and (b) are Sch1a and Sch2a in the garnet skarn, sample 15XY-31; (c) and (d) are Sch1b and Sch2b in the pyroxene skarn, sample 15XY-14; (e–h) are Sch3 and Sch4 hosted in scheelite-rich quartz veins, sample 15XY-29. The chondrite values are from [33]. The granodiorite data are from [28].
Minerals 10 00271 g007
Minerals 10 00271 g008 550
Figure 8. Sketches illustrating multiple re-equilibration processes in scheelite from the Xiaoyao tungsten skarn deposit. The high-Mo scheelite in the proximal zone has undergone the dissolution and re-precipitation, forming some molybdenite grains (A,B,C). The low-Mo scheelite grains in the distal zone (D) have extensively re-equilibrated by DRP (E). Scheelite grains from the quartz–scheelite–sulfide stage comprise the homogeneous core and growth-zoning rim (F,G). Both high-Mo and low-Mo scheelites may have been subjected to recrystallization (F,G) and then locally modified by DRP (H). For more details, see the text. Abbreviations: DRP = dissolution and re-precipitation, RC = re-crystallization. The numbers 1 to 4 refer to the types of scheelite.
Figure 8. Sketches illustrating multiple re-equilibration processes in scheelite from the Xiaoyao tungsten skarn deposit. The high-Mo scheelite in the proximal zone has undergone the dissolution and re-precipitation, forming some molybdenite grains (A,B,C). The low-Mo scheelite grains in the distal zone (D) have extensively re-equilibrated by DRP (E). Scheelite grains from the quartz–scheelite–sulfide stage comprise the homogeneous core and growth-zoning rim (F,G). Both high-Mo and low-Mo scheelites may have been subjected to recrystallization (F,G) and then locally modified by DRP (H). For more details, see the text. Abbreviations: DRP = dissolution and re-precipitation, RC = re-crystallization. The numbers 1 to 4 refer to the types of scheelite.
Minerals 10 00271 g008
Minerals 10 00271 g009 550
Figure 9. (a) Plot of Mo vs. Cd. (b) Plot of LREE/HREE vs. Sr. (c,d) Plot of Mo vs. (La/Lu)N. the scheelite data from the oxidized tungsten skarn deposits, including the Jitoushan and Baizhangya [9], Xitian [38]; the reduced tungsten skarn deposits, including the Zhuxi [15], Xianglushan [14], Kyanigan [39].
Figure 9. (a) Plot of Mo vs. Cd. (b) Plot of LREE/HREE vs. Sr. (c,d) Plot of Mo vs. (La/Lu)N. the scheelite data from the oxidized tungsten skarn deposits, including the Jitoushan and Baizhangya [9], Xitian [38]; the reduced tungsten skarn deposits, including the Zhuxi [15], Xianglushan [14], Kyanigan [39].
Minerals 10 00271 g009
Minerals 10 00271 g010 550
Figure 10. Chemical Variation in Scheelite: (a) Plot of Mo vs. La. (b) Plot of Mo vs. Ce. (c) Plot of Mo vs. Nd. (d) Plot of Mo vs. Gd. (e) Plot of Mo vs. Dy. (f) Plot of Mo vs. Ho.
Figure 10. Chemical Variation in Scheelite: (a) Plot of Mo vs. La. (b) Plot of Mo vs. Ce. (c) Plot of Mo vs. Nd. (d) Plot of Mo vs. Gd. (e) Plot of Mo vs. Dy. (f) Plot of Mo vs. Ho.
Minerals 10 00271 g010
Minerals 10 00271 g011 550
Figure 11. Chemical Variation in Scheelite: (a) Plot of Mo vs. Y. (b) Plot of REE vs. Y. (c) Plot of LREE vs. Y. (d) Plot of HREE vs. Y. (e) Plot of Y vs. Sr. (f) Plot of Ho vs. Y.
Figure 11. Chemical Variation in Scheelite: (a) Plot of Mo vs. Y. (b) Plot of REE vs. Y. (c) Plot of LREE vs. Y. (d) Plot of HREE vs. Y. (e) Plot of Y vs. Sr. (f) Plot of Ho vs. Y.
Minerals 10 00271 g011
Table
Table 1. Details of scheelite samples from the Xiaoyao deposit.
Table 1. Details of scheelite samples from the Xiaoyao deposit.
SampleScheelite TypeLocation Sample Description
15XY-31Sch1a, 2a353m, ZK4704Proximal skarn tungsten ore
15XY-14Sch1b, 2b208m, ZK4704Distal skarn tungsten ore
15XY-28Sch1a, 2a313m, ZK4704Retrograde skarn tungsten ore
15XY-25 Sch1a, 3, 4300m, ZK4704Scheelite-rich quartz veins
15XY-29Sch3, 4320m, ZK4704Scheelite-rich quartz veins
15XY-24Sch3, 4290m, ZK4704Scheelite-rich quartz veins
Table
Table 2. Major elements of four types of scheelites from the Xiaoyao deposit (%).
Table 2. Major elements of four types of scheelites from the Xiaoyao deposit (%).
No.TypeWO3P2O5CaOFeOMnOV2O3TiO2MoO3Total
15XY-31-1-1Sch1a72.410.0320.850.02000.025.7799.11
15XY-31-1-2Sch1a71.060.0520.970.070.020.020.017.2699.49
15XY-31-1-3Sch1a68.95019.99000.020.0210.399.32
15XY-31-1-4Sch1a69.380.120.260.04000.0110.23100.06
15XY-31-1-5Sch1a72.030.0420.86000.0107.05100.05
15XY-31-1-6Sch2a77.760.0219.70.170.030.090.031.7199.53
15XY-28-2-5Sch2a76.590.0618.890000.023.5199.1
15XY-28-2-6Sch1a71.230.0219.040.0200.040.028.799.12
15XY-28-2-7Sch1a73.870.0318.750.010008.03100.76
15XY-28-2-8Sch2a78.130.0818.700.010.0102.1499.12
15XY14-3-1Sch1b79.79019.5900000.4299.84
15XY14-3-2Sch2b70.710.0419.25000010.17100.22
15XY14-3-3Sch2b70.030.0520.930.0300.040.028.0799.2
15XY14-3-4Sch1b79.880.0119.5100000.3899.86
15XY-25-2-1Sch1a69.790.1120.06000.080.019.3499.46
15XY-25-2-2Sch1a73.79018.9500.01007.61100.39
15XY-25-2-3Sch369.280.0520.0900.02009.7899.23
15XY-25-2-4Sch366.670.0520.360.10.04008.9896.19
15XY-25-2-5Sch479.80.0619.440.020.0300.010.3399.7
15XY-25-2-6Sch1a71.290.0720.250.0700.0408.1399.87
15XY-25-2-7Sch371.440.0920.5200.040.030.026.8899.01
15XY29-3-1Sch372.530.0420.830000.016.61100.06
15XY29-3-2Sch374.430.0219.0900.070.030.035.6399.32
15XY29-3-3Sch374.550.0920.24000.030.014.0999.01
15XY29-3-4Sch479.130.0819.70.220.05000.7699.95
15XY-24-2-1Sch372.150.02190.040008.0599.29
15XY-24-2-2Sch372.6019.070.010008.1799.95
15XY-24-2-3Sch371.810.0619.390.10.08009.37100.83
15XY-24-2-4Sch371.8301900.0300.019.49100.46
15XY-24-2-5Sch371.580.0819.070.030009.35100.15
15XY-24-2-6Sch372.660.0119.020.070.02009.06100.88
15XY-24-2-7Sch480.480.0218.7300000.1999.44
Table 3. Rare earth element and trace element concentrations determined by LA-ICP-MS in four types of scheelite and garnet and pyroxene from the Xiaoyao deposit (ppm).
Table
SampleSch TypeLaCePrNdSmEuGdTbDyHoErTmYbLuΣREEΣLREEΣHREELREE/HREEEu/Eu*(La/Sm)N(Gd/Lu)N
15XY-31-1Sch 1a67.1595.308.9926.662.440.191.660.180.630.100.200.010.030.04203.58200.744.8941.020.2717.306.05
15XY-31-3Sch 1a32.0942.053.6411.691.500.151.210.120.700.130.250.020.180.0793.8091.135.3916.920.3313.442.33
15XY-31-6Sch 1a100.86132.3910.8928.483.010.202.300.241.140.200.340.030.140.04280.23275.827.9034.910.2221.097.21
15XY-31-2Sch 2a3.7411.481.173.670.470.060.280.040.180.030.060.000.020.0521.2420.591.1018.680.504.970.75
15XY-31-4Sch 2a6.6713.411.605.680.440.160.690.070.220.040.090.000.010.0429.1027.951.7516.010.889.622.48
15XY-31-5Sch 2a67.5189.287.4218.381.460.430.840.090.400.090.170.040.270.07186.46184.483.8647.831.0929.151.49
15XY-14-1Sch 1b18.8047.6810.4182.4027.555.6048.256.6841.7610.0225.002.3811.101.45339.07192.44392.510.490.470.434.27
15XY-14-2Sch 1b10.4643.0411.58100.6436.655.9874.5811.2278.5418.7242.843.8515.011.30454.41208.36742.830.280.340.187.38
15XY-14-3Sch 1b22.5147.869.0265.8319.214.9234.924.5526.676.3417.421.415.600.73266.99169.34252.570.670.570.746.14
15XY-14-8Sch 1b22.1750.069.1157.9319.153.7431.074.1724.676.0714.411.496.160.86251.06162.16232.210.700.470.734.62
15XY-14-11Sch 1b20.0842.947.9554.9816.772.6532.103.8725.735.6314.381.497.930.85237.34145.37237.370.610.340.754.85
15XY-14-6Sch 2b24.7452.769.1360.8316.063.6930.554.5025.676.0014.141.416.550.67256.72167.22234.350.710.500.975.87
15XY-14-7Sch 2b40.06102.9117.5496.1420.944.6922.112.6815.363.069.000.865.870.56341.78282.29164.991.710.661.205.04
15XY-14-9Sch 2b67.73152.2623.47134.4926.306.0431.484.7427.446.0815.421.9712.101.42510.94410.28296.121.390.641.622.85
15XY-14-10Sch 2b69.51151.7123.51117.7520.095.6024.783.0915.863.9210.331.126.830.85454.97388.17185.412.090.772.183.72
15XY-14-12Sch 2b87.42199.1930.75146.7628.056.9130.704.2826.685.9616.532.1113.951.53600.82499.06295.671.690.721.962.57
15XY-29-2-1Sch 3139.81171.9712.5630.532.441.051.480.150.750.110.270.020.210.07361.43358.376.4155.871.5635.982.71
15XY-29-2-2Sch 3240.02314.2422.8954.095.663.834.820.562.660.470.700.080.320.04650.38640.7321.2830.112.1926.6714.12
15XY-29-2-3Sch 3303.46434.5326.5662.705.405.553.770.371.910.260.300.070.100.05845.03838.1915.6253.663.5835.389.84
15XY-29-2-4Sch 3298.57434.2423.4949.603.173.921.440.170.910.180.300.010.110.04816.14812.988.4596.244.8959.244.29
15XY-29-2-5Sch 3248.33290.7216.9233.882.891.271.790.160.880.130.370.040.250.06597.68594.009.3063.901.5954.134.08
15XY-29-2-6Sch 3208.14222.8316.5842.954.651.163.230.372.330.451.090.120.330.08504.32496.3122.8621.710.8728.185.29
15XY-29-2-7Sch 3116.48178.6721.2895.7618.063.5720.302.4113.772.525.400.481.450.14480.28433.82120.943.590.574.0618.20
15XY-29-2-8Sch 3264.81373.4435.97123.4721.394.7523.863.4119.294.4210.281.023.650.35890.13823.84208.973.940.647.798.87
15XY-29-2-9Sch 467.12110.2612.4841.435.230.695.120.623.200.621.580.120.580.10249.14237.2028.288.390.408.076.71
15XY-29-2-10Sch 446.7484.8910.0634.664.080.933.570.332.140.360.670.030.110.06188.64181.3715.2011.930.737.207.07
15XY-29-1-1Sch 391.01143.5614.0050.636.561.425.930.703.880.721.400.140.300.07320.32307.1832.209.540.688.7211.59
15XY-29-1-2Sch 356.70111.0714.1967.3313.042.7413.831.699.111.693.260.290.760.09295.77265.0677.803.410.622.7319.45
15XY-29-1-3Sch 354.73107.8615.2283.1816.323.0420.022.4212.672.534.830.371.460.10324.74280.35112.812.490.512.1125.06
15XY-29-1-4Sch 381.78129.4414.3159.5411.142.3313.851.698.881.403.420.210.450.08328.54298.5572.994.090.574.6223.25
15XY-29-1-5Sch 3111.35171.1818.0373.9213.182.5314.901.909.552.054.240.431.290.10424.66390.2091.284.270.555.3119.66
15XY-29-1-6Sch 3112.31174.0518.2071.1415.462.9816.852.0711.662.465.160.451.660.16434.59394.13109.083.610.564.5713.72
15XY-29-1-7Sch 389.02137.1714.2866.2812.422.8715.861.769.811.914.640.361.130.15357.66322.0394.463.410.634.5113.63
15XY-29-1-8Sch 3148.15200.3416.9153.497.521.456.070.813.960.821.760.150.410.09441.93427.8638.9810.970.6412.398.77
15XY-29-1-9Sch 3130.06180.1713.9434.613.821.552.020.291.340.240.560.010.270.06368.94364.1612.8128.421.5421.394.53
15XY-29-1-10Sch 3100.53139.6211.2427.201.960.801.690.120.610.100.260.030.020.07284.25281.355.9347.441.3232.252.96
15XY-29-1-11Sch 395.33134.3010.2622.992.440.811.850.260.950.190.310.010.180.06269.94266.1410.1726.181.1224.574.14
15XY-31-7Garnet14.8835.284.3017.303.550.693.060.402.980.501.670.200.900.1885.8976.0025.632.970.575.670.74
15XY-31-8Garnet14.1135.754.2414.642.700.614.110.685.031.153.400.503.520.6191.0472.0552.151.380.622.642.14
15XY-14-4Pyroxene0.741.820.301.160.330.150.000.120.830.120.280.081.740.598.244.498.660.520.563.290.87
15XY-14-5Pyroxene0.281.350.221.670.450.170.140.090.630.140.430.181.870.538.154.158.950.462.411.400.00
Table
SampleSch TypeNaMoAsSrYZrNbHfTaCdPbZr/HfNb/TaY/Ho
15XY-31-1Sch 1a26.7545,593.046.1767.042.059.5815.001.38850.675.981.896.920.0220.51
15XY-31-3Sch 1a12.4020,578.053.3282.702.729.604.551.60863.902.520.656.010.0120.58
15XY-31-6Sch 1a42.0260,560.3511.0087.153.498.878.961.61779.388.303.055.520.0117.86
15XY-31-2Sch 2a2.6710,628.820.0089.710.459.621.331.54928.031.110.386.230.0013.78
15XY-31-4Sch 2a0.008390.981.4387.840.6010.243.341.63907.671.020.676.290.0015.74
15XY-31-5Sch 2a0.0013,343.187.8973.231.8833.3632.093.09860.231.512.1210.780.0420.43
15XY-14-1Sch 1b233.911083.3012.94102.80245.8811.2010.861.751469.780.342.906.410.0124.55
15XY-14-2Sch 1b0.0058.804.2976.72496.7810.9822.192.191568.930.001.675.000.0126.54
15XY-14-3Sch 1b0.001386.6412.15110.21154.9213.8810.542.081538.070.002.606.680.0124.42
15XY-14-8Sch 1b0.002205.3410.28110.18143.3110.4110.021.681397.170.403.056.210.0123.62
15XY-14-11Sch 1b0.00622.948.58108.78145.4010.0310.182.171399.360.002.184.630.0125.83
15XY-14-6Sch 2b0.005814.946.17117.73144.8510.8612.091.731359.430.002.876.260.0124.14
15XY-14-7Sch 2b256.4986,771.3210.90159.58105.4935.8512.881.721124.927.423.7620.830.0134.50
15XY-14-9Sch 2b0.0047,068.4811.83144.46195.4736.3646.832.841181.121.984.3412.800.0432.14
15XY-14-10Sch 2b28.5356,974.3118.48154.41118.6113.9826.221.811218.514.565.077.720.0230.28
15XY-14-12Sch 2b0.0053,754.9313.20141.41193.9244.5853.073.051125.684.044.1114.630.0532.52
15XY-29-2-1Sch 3179.1544,234.7714.68104.953.3512.4216.211.561088.535.3927.707.960.0131.80
15XY-29-2-2Sch 378.4652,207.242.31113.5411.6411.886.581.651065.893.462.707.180.0124.77
15XY-29-2-3Sch 3111.1956,637.385.12110.608.7910.6213.941.621068.3952.7615.056.560.0133.58
15XY-29-2-4Sch 365.8161,604.739.68103.105.2910.518.021.531063.146.192.266.850.0130.03
15XY-29-2-5Sch 368.7472,813.944.4993.145.629.745.241.251048.246.562.097.780.0043.82
15XY-29-2-6Sch 3200.1889824.215.79106.4714.8510.634.271.35990.886.871.767.860.0033.23
15XY-29-2-7Sch 30.0011,675.751.32109.7474.4810.4125.061.631170.840.551.136.390.0229.59
15XY-29-2-8Sch 3147.3975,612.318.22114.14142.6911.9911.761.321048.014.921.909.090.0132.27
15XY-29-2-9Sch 444.9732,894.582.0789.2316.359.1826.991.501179.636.151.996.110.0226.46
15XY-29-2-10Sch 40.0017636.971.7587.587.9310.8621.351.571186.751.095.716.930.0222.32
15XY-29-1-1Sch 30.0086685.1018.00119.7219.0510.187.231.321055.651.812.917.700.0126.51
15XY-29-1-2Sch 30.0024606.245.14102.3547.099.6723.111.741268.901.161.795.560.0227.92
15XY-29-1-3Sch 375.7118,813.402.73101.1268.4110.5229.701.541295.134.771.596.840.0227.07
15XY-29-1-4Sch 316.5917,920.214.7092.0242.999.8523.061.301238.478.313.087.590.0230.67
15XY-29-1-5Sch 359.3369,605.234.98101.2056.8213.0411.561.261078.531.327.0010.330.0127.76
15XY-29-1-6Sch 382.3979,410.899.31104.6368.6112.129.301.421090.6310.038.468.530.0127.87
15XY-29-1-7Sch 30.0016,264.145.37102.8158.8310.1024.791.881242.522.901.765.370.0230.79
15XY-29-1-8Sch 30.0089,459.704.95106.9624.9111.353.961.44963.194.502.257.870.0030.27
15XY-29-1-9Sch 363.9359,743.5810.98106.498.0311.289.491.891102.086.282.585.960.0133.40
15XY-29-1-10Sch 30.0051,315.6414.24120.363.0310.398.601.731124.431.521.805.990.0129.80
15XY-29-1-11Sch 370.2191,626.289.87112.346.3610.816.681.53984.722.592.057.080.0134.15
SampleSch TypeNaMoAsSrYZrNbHfTaAuPbZr/HfNb/TaY/Ho
15XY-31-7Garnet384.437.381.140.2415.747.041.680.170.550.010.4741.893.0731.31
15XY-31-8Garnet219.274.222.680.4933.1637.895.511.610.640.000.2623.608.6028.95
15XY-14-4Pyroxene0.060.001.8111.674.916.410.060.000.010.000.240.0010.8739.66
15XY-14-5Pyroxene0.180.230.007.414.956.030.000.500.000.0227.4712.030.0036.03

Share and Cite

MDPI and ACS Style

Su, Q.; Mao, J.; Sun, J.; Zhao, L.; Xu, S. Geochemistry and Origin of Scheelites from the Xiaoyao Tungsten Skarn Deposit in the Jiangnan Tungsten Belt, SE China. Minerals 2020, 10, 271. https://doi.org/10.3390/min10030271

AMA Style

Su Q, Mao J, Sun J, Zhao L, Xu S. Geochemistry and Origin of Scheelites from the Xiaoyao Tungsten Skarn Deposit in the Jiangnan Tungsten Belt, SE China. Minerals. 2020; 10(3):271. https://doi.org/10.3390/min10030271

Chicago/Turabian Style

Su, Qiangwei, Jingwen Mao, Jia Sun, Linghao Zhao, and Shengfa Xu. 2020. "Geochemistry and Origin of Scheelites from the Xiaoyao Tungsten Skarn Deposit in the Jiangnan Tungsten Belt, SE China" Minerals 10, no. 3: 271. https://doi.org/10.3390/min10030271

Note that from the first issue of 2016, this journal uses article numbers instead of page numbers. See further details here.

Article Metrics

Back to TopTop