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Article

Separation of Fe from Mn in the Cryogenian Sedimentary Mn Deposit, South China: Insights from Ore Mineral Chemistry and S Isotopes from the Dawu Deposit

by
Zhiming Xu
1,2,
Chengquan Wu
1,*,
Zhengwei Zhang
1,
Jinhong Xu
1,3,
Xiyao Li
1,3 and
Ziru Jin
1,3
1
State Key Laboratory of Ore Deposit Geochemistry, Institute of Geochemistry, Chinese Academy of Sciences, Guiyang 550081, China
2
Fuzhou University, Fuzhou 350108, China
3
College of Earth and Planetary Sciences, University of Chinese Academy of Sciences, Beijing 100049, China
*
Author to whom correspondence should be addressed.
Minerals 2021, 11(5), 446; https://doi.org/10.3390/min11050446
Submission received: 9 March 2021 / Revised: 15 April 2021 / Accepted: 20 April 2021 / Published: 23 April 2021
(This article belongs to the Section Mineral Deposits)
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Abstract

:
Manganese and Fe have similar geochemical properties in the supergene environment. Separation of Mn and Fe is an important process for the formation of high-grade sedimentary manganese deposits. Large-scale manganese carbonate deposits (total reserves of approximately 700 Mt) were formed during the interglacial of the Sturtian and Marinoan in South China. The orebodies are hosted in the black rock series at the basal Datangpo Formation of the Cryogenian period. The Fe contents in ores range from 1.15 to 7.18 wt.%, with an average of 2.80 wt.%, and the average Mn/Fe ratio is 8.9, indicating a complete separation of Mn and Fe during the formation of manganese ores. Here, we present element data of manganese carbonates and sulfur isotopes of pyrite from the Dawu deposit, Guizhou, China, aiming to investigate the separation mechanism of Mn and Fe and the ore genesis. The Fe in ores mainly occurs as carbonate (FeCO3) and pyrite (FeS2). The Mn, Ca, Mg and Fe exist in the form of isomorphic substitutions in manganese carbonate. The contents of FeCO3 in manganese carbonates are similar in different deposits, with averages of 2.6–2.8 wt.%. The whole-rock Fe and S contents have an obvious positive correlation (R = 0.69), indicating that the difference of whole-rock Fe content mainly comes from the pyrite content. The δ34SV-CDT of pyrite varies from 40.0 to 48.3‰, indicating that the pyrite formed in a restricted basin where sulfate supply was insufficient and the sulfate concentrations were extremely low. Additionally, the whole-rock Fe content is negatively correlated with the δ34S values of the whole-rock and pyrite, with correlation coefficients of −0.78 and −0.83, respectively. Two stages of separations of Mn and Fe might have occurred during the mineralization processes. The reduced seawater became oxidized gradually after the Sturtian glaciation, and Fe2+ was oxidized and precipitated before Mn2+, which resulted in the first-stage separation of Mn and Fe. The residual Mn-rich and Fe-poor seawater flowed into the restricted rift basin. Mn and Fe were then precipitated in sediments as oxyhydroxide as the seawater was oxidized. At the early stage of diagenesis, organic matter was oxidized, and manganese oxyhydroxide was reduced, forming the manganese carbonate. H2S was insufficient in the restricted basin due to the extremely low sulfate concentration. The Fe2+ was re-released due to the lack of H2S, resulting in the second-stage separation of Mn and Fe. Finally, the manganese carbonate deposit with low Fe and very high δ34S was formed in the restricted basin after the Sturtian glaciation.

Graphical Abstract

1. Introduction

The abundance of Fe in the continental crust is 7.08 wt.%, which is much higher than that of Mn at 0.14 wt.% [1]. Separation of Mn and Fe is very common in sedimentary manganese deposits [2,3,4], such as the Archean Noamundi Fe-Mn deposit in India, the Late Proterozoic Otjosond Mn-Fe deposit in Namibia, the Neoproterozoic Urucum Fe-Mn deposit in Brazil, and the Eocene Elazığ-Malatya Fe-Mn deposit in eastern Turkey [5,6,7,8,9]. The area of stability of Mn2+ is larger than that of Fe2+ under supergene conditions [9,10]. In a reduced environment, Mn and Fe are dissolved in water in the form of Mn2+ and Fe2+, respectively, and Fe2+ is oxidized and precipitated before Mn2+ in the process of gradual oxidation [10]. Moreover, in the anoxic and sulfur-rich environment, Mn occurs as soluble manganese bicarbonate and manganese sulfide with poor stability, while Fe mainly occurs as stable sulfide [10,11]. Furthermore, some microorganisms selectively promote manganese oxidation and may result in the separation of Mn and Fe [10,11,12]. Therefore, the study of the separation of Mn and Fe can trace the Mn mineralization process and deepen the understanding of ore genesis.
The Cryogenian (also known as the Nanhua period in China) manganese deposits in South China are mainly concentrated in the adjacent area of Guizhou, Hunan, Chongqing, and Hubei [13]. Four super-large (Mn reserves >100 Mt) manganese deposits have been discovered since 2008, with the total Mn resources exceeding 700 Mt [13,14,15]. The orebodies occur in the black rock series at the basal Datangpo Formation of the Cryogenian System, and the ore minerals are mainly manganese carbonates [13,14,16]. Previous studies have shown that the Cryogenian manganese deposits were formed in the restricted basins, and the Mn was precipitated as oxyhydroxide and was then reduced to carbonates [13]. After the Sturtian glaciation, the basin was in a redox stratified environment in the Datangpo stage. The bottom seawater was in a reductive state, where it was conducive to the enrichment of Fe and Mn, while the upper ocean was in an oxidizing environment, which led to precipitation of Fe and Mn [13]. The gradually oxidized environment was favorable for the separation of Fe from Mn. The whole-rock Fe contents of ores are 1.15–7.18 wt.%, with an average of 2.80 wt.%, and the Mn/Fe ratios are 1.9–26.4, indicating that there may be a complete separation of Mn and Fe during the formation of manganese ore [13]. However, the separation process and its control mechanism are still unclear. Here, we present element data of manganese carbonates and in situ sulfur isotopes of pyrite from the Dawu manganese deposit in Guizhou, South China, aiming to investigate the separation mechanism of Mn and Fe and to further understand the genesis of the deposit.

2. Geological Setting

The study area is located at the conjunction of the Yangtze Block and Jiangnan Orogen (Figure 1A). The Yangtze Plate and Cathaysia Plate merged into the South China Plate at ~1.1–0.9 Ga ago due to the Sibao Orogeny (also known as the Jinning Movement or Jiangnan Movement) [17,18,19]. The South China Plate began to break off at ~820 Ma, forming the Nanhua rift [20,21,22,23]. At that time, the southeastern part of the Yangtze Platform was situated on a passive continental margin, and a large number of basins were formed along the rift, which provided the advantageous space for deposition of Neoproterozoic lithologies [21,24,25]. The study area was mainly a rift basin (Nanhua basin) during the Cryogenian period, which evolved into shelf, platform, passive continental margin, or continental margin slope in the Sinian period [26], providing a stable tectonic environment for the formation of manganese deposits.
The Neoproterozoic strata are widely distributed in the study area, gradually changing from basinal facies in eastern Guizhou and western Hunan to transition facies and platform facies in the north and west [27]. The Datangpo Formation with manganese carbonate is distributed in both basinal and transitional facies. The underlying stratum is the Tiesi’ao Formation, and the overlying stratum is the Nantuo Formation (Figure 2), all of which with conformable contact. The zircon U-Pb ages of the tuff interlayers at the bottom and top of the Datangpo Formation are 662.9 ± 4.3 Ma [27] and 654.5 ± 3.8 Ma [28], respectively, constraining the sedimentary age of Datangpo Formation. The Tiesi’ao Formation and Nantuo Formation are glacial sedimentary strata [27], corresponding to the Sturtian and Marinoan glacial sedimentary strata of the Cryogenian System [27,29,30,31,32,33]. The thickness of the Datangpo Formation in the study area is approximately 200–500 m, with dark gray and grayish-yellow silty shale in the upper part and black carbonaceous shale in the lower part (Figure 2). The manganese carbonate orebody occurs in the black shale of the first member of the Datangpo Formation (Figure 2).

3. Deposit Descriptions

The Cryogenian manganese carbonate deposits are distributed in Guizhou, Hunan, Chongqing, and Hubei, and are mainly concentrated in eastern Guizhou (Figure 1). The typical deposits include Yanglizhang, Dawu, Datangpo, Daotuo, Xixibao, Gaodi, and Taoziping deposits in Guizhou (Figure 1B); Rongxi deposit in Chongqing; Minle, Gucheng, and Xiangtan deposits in Hunan; and Gucheng deposit in Hubei [13,14,33].
The manganese-bearing rock series is the black rock series of the first member of the Datangpo Formation, which is mainly composed of manganese carbonate, black carbonaceous shale, manganiferous carbonaceous shale, and tuffaceous sandstone (Figure 2, Figure 3 and Figure 4A). The thickness of the manganese-bearing rock series is generally 14–30 m and is positively correlated with that of manganese carbonate orebodies [14,34]. The lithology of the manganese-bearing rock series displays a zonal distribution, with a manganese carbonate belt, a carbonaceous shale-manganese-dolomite belt, and a carbonaceous shale-silty carbonaceous shale belt from the center to the edge of the sedimentary basin [34,35,36]. The thickness of the manganese-bearing rock series in the Dawu deposit is 13.0−28.4 m, with an average of 18.0 m [34].
The manganese-bearing rock series commonly has 2–3 manganese carbonate layers. The orebodies are stratified and lenticular, and the occurrences are consistent with those of wall rocks (Figure 3). The thickness of the orebody varies greatly, generally ranging from 1 to 5 m. From the center to the edge of the sedimentary basin, the thickness of the orebody gradually becomes thinner, and the number of ore layers gradually decreases. The orebodies are separated by carbonaceous shale, carbonaceous claystone, and tuffaceous sandstone. The wall rocks are mainly black carbonaceous shale (Figure 3 and Figure 4B,C). The orebody of the Dawu deposit is stratified, with approximately 5500 m in length and 500 m in width. The orebody is 0.5–3.1 m thick, with an average of 1.4 m [34]. The upper orebody is 0.19–0.25 m thick, the lower orebody is 0.74–1.64 m thick, and the orebodies are separated by 0.17–0.86 m thick siltstone and shale (Figure 3) [37].
The ore minerals are mainly Ca-rhodochrosite and Mn-calcite. The gangue minerals are mainly quartz, feldspar, muscovite, pyrite, montmorillonite, and illite, with minor apatite. The Ca-rhodochrosite mainly exhibits micrite and microcrystalline texture (Figure 4H,I), and the particle size is generally 2–6 μm. The cement between Ca-rhodochrosite particles is Mn-calcite, argillaceous mineral, and organic matter (Figure 4H,I). Pyrite is very common in the ores, exhibiting idiomorphic–hypidiomorphic granular and framboidal textures (Figure 4G,H). The ore structure is mainly massive (Figure 4D), laminated (Figure 4E,G), and banded (Figure 4F). The massive ore usually has high ore grade and is mainly composed of Ca-rhodochrosite and Mn-calcite, which is common in thick orebodies, and the organic concretions occur in some massive ores (Figure 4D). The laminated ore is the most common, and the thin laminate is mainly composed of manganese carbonate, organic matter, and argillaceous minerals (Figure 4E,G). The ores are generally low-grade, low-Fe, and high-P type manganese carbonates, with 12–30 wt.% Mn (average 21.3 wt.%), 1.51–7.18 wt.% Fe (average 2.76 wt.%), and 0.06–1.27 wt.% P (average 0.22). The Mn/Fe ratios of ores range from 1.9 to 26.4 (average 8.9), and the P/Mn ratios range from 0.003 to 0.064 (average 0.011).

4. Sampling and Analytical Methods

The samples were collected from the 640-tunnel of the Dawu mining area, with geographical coordinates of 28°02′43″ N, 108°51′34″ E.
Electron probe microanalysis (EPMA) of manganese carbonate was conducted using a JXA-5230F Plus Hyper Probe at State Key Laboratory of Ore Deposit Geochemistry, Institute of Geochemistry, Chinese Academy of Sciences (SKLODG, IGCAS), with the 5–10 μm beam diameter, 25 kV accelerating potential, and 10 nA probe current. Rhodochrosite, calcite, magnesite, and siderite were used as standards; all of the standards were tested for homogeneity before their utilization for quantitative analysis. The data were reduced using the ZAF correction method.
The in situ sulfur isotope measurements of pyrite were performed on a Nu Plasma III MC-ICP-MS (Multi-receiver plasma mass spectrometry, Nu Instruments) that was attached to a RESOlution-155 ArF193-nm laser ablation system (Australian Scientific Instruments) at SKLODG, IGCAS. The mass separation was calculated as 0.3333 in the analyses. The instrument was utilized in pseudo-medium resolution mode [39] to resolve polyatomic interferences from 16O–16O for 32S and 16O–18O for 34S, adjusting the source slit to medium (0.05 mm) in conjunction with using the alpha slit. Sulfide was ablated in a mixture of helium (350 mL/min) and nitrogen (2 mL/min) atmosphere using the following parameters: 20 s baseline time, 40 s ablation time, 40 s wash time, 60 μm spot size, 6 Hz repetition rate, and 2–3 J/cm2 energy density. All analyses followed standard sample bracketing procedures of three samples bracketed by chalcopyrite pressed powder tablet (PSPT-1) [40,41]. Two natural pyrite crystals (SB-1 from the Shangbao W-Sn deposit and HYC-1 from the Huayangchuan Nb-U-REE deposit, China) were treated as quality control. The measured δ34SV-CDT for the standard was 16.57‰ (n = 12) for SB-1 and −5.76‰ for HYC-1(n = 12), which was identical to the recommended value (16.57‰ for SB-1 and −5.76‰ for HYC-1) (IRMS).

5. Results

The element data of manganese carbonate in the Dawu manganese deposit are shown in Table 1. The Mn, Ca, Mg and Fe exist in the form of isomorphic substitutions in manganese carbonate, forming Ca-rhodochrosite and Mn-calcite. The MnCO3 is negatively correlated with CaCO3 and MgCO3, and the correlation coefficients are −0.98 and −0.73, respectively (Figure 5A,B). The MnCO3 is positively correlated with P2O5, with a correlation coefficient of 0.64 (Figure 5D). The content of FeCO3 in manganese carbonate ranges from 0.65 to 6.57 wt.%, with an average of 2.63 wt.%. There is no obvious correlation between MnCO3 and FeCO3 (Figure 5C).
Two samples from the Dawu deposit (DW03-1 and DW03-5) were selected for analysis of the in situ S isotope. The S isotopes of pyrite in DW03-1 vary greatly, and the δ34S ranges from 23.1‰ to 56.5‰, with an average of 40.0 ± 13.4‰ (Figure 6a). However, the S isotopes of pyrite in DW03-5 are very uniform, with δ34S ranging from 47.2‰ to 49.2 ‰ and an average of 48.30 ± 0.9‰ (Table 2 and Figure 6b).

6. Discussion

6.1. Separation of Mn and Fe during Sedimentation

Manganese and Fe have similar chemical properties in the supergene environment, and their separation is mainly controlled by Eh-pH conditions [42]. In the gradual oxidation of the reduced water, Fe is oxidized and precipitated before Mn, which results in the separation of Mn and Fe. When the water Eh fluctuates alternately, rhythmic layers with alternating Fe-Mn occur in the stratigraphic profile. The separation of Mn and Fe is not obvious during the rapid oxidation of water, forming Fe-Mn oxides or hydroxides [42].
The Cryogenian manganese deposits occur in the basal Datangpo Formation in South China, and no iron-rich stratum has been found in the manganese-bearing rock series or its adjacent strata [13]. The mineralization of manganese occurred after the Sturtian glaciation. The seawater under the ice sheet was in a reduced state, and Mn and Fe could accumulate as ionic compounds (Mn2+ and Fe2+) in large quantities, which provided a material basis for the subsequent precipitation and enrichment of manganese [13,43,44]. Previous studies have shown that the Nanhua Basin was in a redox stratified environment in the Datangpo stage [45,46,47], and the oxidation of the water in the basin gradually increased, forming the suboxidation–oxidation environment in the shallow parts [48,49,50]. In the process of progressive oxidation in the marine environment after glaciation, Fe2+ was oxidized and precipitated before Mn2+, leading to the first-stage separation of Mn and Fe [51].
The δ34S values of pyrite from manganese-bearing rock series are very high, and the average δ34S of pyrite in Dawu manganese deposit is 40.0–48.3‰, which is similar to the results of previous studies (Table 2 and Figure 7). This indicates that pyrite is formed in the restricted basin where sulfate consumption is much greater than supply [13,52,53], making the residual sulfate concentration extremely low and enriched in 34S [54,55] and eventually forming pyrite with very high δ34S [13]. There is a significant negative correlation (R = −0.73) between the whole-rock δ34S value and S content (Figure 8B), which further indicates that the sulfate concentration in seawater should have been extremely low. The study of lithofacies paleogeography also shows that the manganese deposits were formed in the secondary Nanhua rift basins [15]. The horst formed by the extension provided a barrier for the metallogenic basin, which caused it to be a restricted basin [13,15]. The first-stage separation of Mn and Fe has occurred before the Mn-rich seawater flowing into the metallogenic basin, and the Fe was oxidized and precipitated outside the basin. Therefore, no Fe-rich stratum can be found near the Mn ore beds.

6.2. Separation of Mn and Fe during Diagenesis

The ores from the Cryogenian manganese deposit are rich in organic matter, and Mn exists in the form of carbonates [16,38]. The manganese carbonate is depleted in 13C, and δ13C ranges from −6.33‰ to −10.84‰, with an average of −8.36‰, indicating that the carbon in the manganese carbonate is mainly derived from the oxidation of organic matter [38,54]. The Mn2+ was oxidized to Mn-oxyhydroxide in the oxic seawater and precipitated into the sediments. The buried Mn-oxyhydroxide was reduced to form Mn carbonates in the diagenetic stage [13,25,54,67,68].
There are certain differences in the whole-rock Fe content in different deposits. The highest Fe content in the Dawu and Rongxi deposits is 3.07 wt.% and 3.15 wt.%, respectively, while the lowest Fe content in Datangpo and Daotuo deposits is 1.90 wt.% and 2.14 wt.%, respectively (Figure 8D), indicating that there are differences in the separation of Mn and Fe in various deposits. The Fe mainly occurs as carbonate (FeCO3) and pyrite (FeS2) in the ores. In the manganese carbonate, Mn, Ca, Mg, and Fe exist due to isomorphic substitutions. The MnCO3 is negatively correlated with CaCO3 and MgCO3, with correlation coefficients of −0.98 and −0.73, respectively (Figure 5A,B), while the MnCO3 has no obvious correlation with FeCO3 (Table 1, Figure 5C). The FeCO3 content in the manganese carbonate of Dawu deposit is 0.65–6.57 wt.%, with an average of 2.63 wt.%, while that in the Datangpo deposit is 0.55–6.87 wt.%, with an average of 2.82 wt.% [38], showing no obvious difference between these two deposits.
The whole-rock Fe and S contents have a significant positive correlation (R = 0.69) (Figure 8A). Therefore, the difference in the whole-rock Fe content in the ore mainly comes from the difference in the pyrite content. Pyrite is very common in ores, showing idiomorphic–hypidiomorphic granular and framboidal textures. Pyrite nodules occur in some deposits (e.g., the Daotuo and Gucheng deposits) [66]. These pyrites can be formed in sedimentary and diagenetic stages [13]. Additionally, the whole-rock Fe content is negatively correlated with the whole-rock and pyrite δ34S, with correlation coefficients of −0.78 and −0.83, respectively (Figure 8C,D). There might have been a separation of Mn and Fe in the diagenetic stage, which led to the difference of whole-rock Fe content in the deposits. In the early diagenetic stage, the Mn-oxyhydroxide was reduced to Mn2+, and the bicarbonate was derived from the oxidation of organic carbon, forming the manganese carbonate [67,68]. Due to the extremely low sulfate concentration in the fluid, H2S was insufficient in the restricted basin. Therefore, the Fe2+ reduced in the diagenetic stage was re-released into the upper water due to the lack of H2S, resulting in the second-stage separation of Mn and Fe and a significant negative correlation between the Fe content and δ34S of the whole-rock and pyrite (Figure 8C,D).

7. Conclusions

The Cryogenian manganese deposits in South China are characterized by low Fe contents and very high δ34S. This study demonstrates that two-stage separations of Mn and Fe occurred during the mineralization processes. The oxidation state of seawater increased gradually after the Sturtian glaciation; therefore, Fe2+ was oxidized and precipitated before the Mn2+, leading to the first-stage separation of Mn and Fe. The Mn-rich and Fe-poor seawater flowed into the restricted rift basin. Then, Mn and Fe were precipitated in sediments with further oxidation of the seawater. At the early stage of diagenesis, organic matter was oxidized, and Fe-Mn oxyhydroxide was reduced, forming the manganese carbonate. The H2S was insufficient in the restricted basin due to the extremely low sulfate concentration. The Fe2+ was re-released due to the lack of H2S, resulting in the second-stage separation of Mn and Fe. Finally, the manganese carbonate deposit with low Fe and extremely high δ34S was formed. Therefore, the Cryogenian manganese deposits in South China are sedimentary/diagenetic-type deposits, which were formed in the restricted rift basin after the Sturtian glaciation.

Author Contributions

Conceptualization, Z.X. and C.W.; methodology, J.X.; formal analysis, X.L. and Z.J.; investigation, Z.X., C.W. and Z.Z.; resources, C.W. and Z.Z.; data curation, C.W.; writing—original draft preparation, Z.X.; writing—review and editing, C.W. and Z.Z.; supervision, Z.Z.; project administration, C.W. and Z.Z.; funding acquisition, C.W. and Z.Z. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the National Natural Science Foundation of China (NSFC Nos. 41703051, U1603245, and U1812402), CAS IIT (JCTD-2019-17); the Science and Technology Foundation of Guizhou Province (No. [2018] 1171); the Chinese Academy of Sciences (CAS) “Light of West China” Program; and the frontier project of the State Key Laboratory of Ore Deposit Geochemistry, Institute of Geochemistry, Chinese Academy of Sciences.

Data Availability Statement

All data generated or analyzed during this study are included in this published article.

Acknowledgments

The authors would like to thank Wei Mao and Zhuojun Xie for discussions. This manuscript greatly benefited from the valuable comments and suggestions from two anonymous reviewers and editors of Minerals.

Conflicts of Interest

This manuscript has not been published or presented elsewhere in part or in entirety, and it is not under consideration by another journal. All the authors have approved the manuscript and agree with submission to your esteemed journal. There are no conflict of interest to declare.

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Figure 1. (A) Tectonic sketch map of South China and the location of the study area. (B) Geological sketch map of the Cryogenian manganese deposits in eastern Guizhou, China (modified from [13,33]).
Figure 1. (A) Tectonic sketch map of South China and the location of the study area. (B) Geological sketch map of the Cryogenian manganese deposits in eastern Guizhou, China (modified from [13,33]).
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Figure 2. Stratigraphic details for the Datangpo Formation in eastern Guizhou, China (modified from [13]).
Figure 2. Stratigraphic details for the Datangpo Formation in eastern Guizhou, China (modified from [13]).
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Figure 3. The geological section along exploration line 51 in the Dawu deposit (modified from [37,38]).
Figure 3. The geological section along exploration line 51 in the Dawu deposit (modified from [37,38]).
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Figure 4. Manganese-bearing rock series, morphology of orebody, and ore structures of the Cryogenian manganese deposits in South China. (A) Manganese-bearing rock series occur in the first member of the Datangpo Formation; (B,C) manganese carbonate orebody and wall rock; (D) ore with massive structure and organic concretion; (E) laminated structure—the laminae are 0.1–3 mm and mainly composed of rhodochrosite, argillaceous minerals, and carbonaceous material; (F) banded structure; (G) laminated structure (reflected light); (H,I) micritic and microcrystalline manganese carbonates (BSE); Py—pyrite; Qtz—quartz.
Figure 4. Manganese-bearing rock series, morphology of orebody, and ore structures of the Cryogenian manganese deposits in South China. (A) Manganese-bearing rock series occur in the first member of the Datangpo Formation; (B,C) manganese carbonate orebody and wall rock; (D) ore with massive structure and organic concretion; (E) laminated structure—the laminae are 0.1–3 mm and mainly composed of rhodochrosite, argillaceous minerals, and carbonaceous material; (F) banded structure; (G) laminated structure (reflected light); (H,I) micritic and microcrystalline manganese carbonates (BSE); Py—pyrite; Qtz—quartz.
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Figure 5. Correlation diagrams formajor elements of carbonates from the Dawu deposit. (A) MnCO3 vs. CaCO3; (B) MnCO3 vs. MgCO3; (C) MnCO3 vs. FeCO3; (D) MnCO3 vs. P2O5.
Figure 5. Correlation diagrams formajor elements of carbonates from the Dawu deposit. (A) MnCO3 vs. CaCO3; (B) MnCO3 vs. MgCO3; (C) MnCO3 vs. FeCO3; (D) MnCO3 vs. P2O5.
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Figure 6. Analyzed points and results of the in situ sulfur isotope of pyrite from the Dawu deposit (reflected light photos, taken by a Leica DM4P optical microscope). (a) S isotopes of DW03-1; (b) S isotopes of DW03-5.
Figure 6. Analyzed points and results of the in situ sulfur isotope of pyrite from the Dawu deposit (reflected light photos, taken by a Leica DM4P optical microscope). (a) S isotopes of DW03-1; (b) S isotopes of DW03-5.
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Figure 7. Histogram of sulfur isotopic compositions for pyrite from the Cryogenian manganese deposits in South China. Data of Dawu (red box) are from Table 2 of this study; data of the other deposits (gray box) are from the literature [13,33,35,37,45,54,55,56,57,58,59,60,61,62,63,64,65].
Figure 7. Histogram of sulfur isotopic compositions for pyrite from the Cryogenian manganese deposits in South China. Data of Dawu (red box) are from Table 2 of this study; data of the other deposits (gray box) are from the literature [13,33,35,37,45,54,55,56,57,58,59,60,61,62,63,64,65].
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Figure 8. (A) Correlation diagram for whole-rock Fe and S contents from the Cryogenian manganese deposits; data are from [13,33,66]. (B) Correlation diagram of whole-rock δ34S and S content from the Daotuo deposit; data are from [66]. (C) Correlation diagram of whole-rock Fe content and δ34S from the Daotuo deposit; data are from [33,66]. (D) Correlation diagram of whole-rock Fe content and pyrite δ34S from different manganese deposits; data are from [13,33].
Figure 8. (A) Correlation diagram for whole-rock Fe and S contents from the Cryogenian manganese deposits; data are from [13,33,66]. (B) Correlation diagram of whole-rock δ34S and S content from the Daotuo deposit; data are from [66]. (C) Correlation diagram of whole-rock Fe content and δ34S from the Daotuo deposit; data are from [33,66]. (D) Correlation diagram of whole-rock Fe content and pyrite δ34S from different manganese deposits; data are from [13,33].
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Table
Table 1. EPMA analyses of carbonates from the Dawu manganese deposit (wt.%).
Table 1. EPMA analyses of carbonates from the Dawu manganese deposit (wt.%).
Sample No.MineralMnCO3CaCO3MgCO3FeCO3P2O5Al2O3SiO2Total
DW02-6-1Ca-Rds71.1419.086.791.860.580.020.1199.57
DW02-6-2Ca-Rds74.8218.065.961.130.26bld0.03100.26
DW02-6-3Ca-Rds54.5829.208.614.350.180.030.4597.40
DW02-6-4Ca-Rds69.8022.836.901.470.32bld0.03101.35
DW02-6-5Mn-Cal27.6559.829.792.070.020.020.0899.44
DW02-6-6Mn-Cal27.5556.3113.302.20bldbld0.0299.38
DW02-6-7Mn-Cal27.9955.7811.842.180.02bld0.0797.88
DW03-8-1Ca-Rds72.0021.734.120.650.180.010.0798.76
DW03-8-2Ca-Rds67.4323.905.211.710.180.020.5198.95
DW03-8-3Ca-Rds73.1519.405.731.380.320.070.68100.73
DW03-8-4Ca-Rds71.3017.655.672.350.170.020.6697.82
DW03-8-5Ca-Rds71.6020.184.671.230.22bld0.0397.92
DW03-8-6Mn-Cal39.5745.166.076.570.090.020.1797.64
DW03-8-7Ca-Rds55.8126.4112.233.63bld0.060.2598.38
DW03-8-9Ca-Rds67.9417.855.995.740.020.012.95100.49
DW03-8-10Ca-Rds68.6922.636.482.080.21bld0.03100.12
The contents of MnCO3, CaCO3, MgCO3, and FeCO3 are converted according to the contents of MnO, CaO, MgO, and FeO. Bdl—below detection limit. Rds—rhodochrosite, Cal—calcite.
Table
Table 2. In situ sulfur isotopic compositions of pyrite from the Dawu manganese deposit.
Table 2. In situ sulfur isotopic compositions of pyrite from the Dawu manganese deposit.
No.Samples No.δ34S (‰)±2σ
1DW03-1-Py-149.90.1
2DW03-1-Py-247.00.2
3DW03-1-Py-336.90.1
4DW03-1-Py-423.10.2
5DW03-1-Py-556.50.2
6DW03-1-Py-626.30.2
7DW03-5-Py-147.70.1
8DW03-5-Py-247.90.1
9DW03-5-Py-349.00.1
10DW03-5-Py-447.20.1
11DW03-5-Py-549.00.1
12DW03-5-Py-649.20.1
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Xu, Z.; Wu, C.; Zhang, Z.; Xu, J.; Li, X.; Jin, Z. Separation of Fe from Mn in the Cryogenian Sedimentary Mn Deposit, South China: Insights from Ore Mineral Chemistry and S Isotopes from the Dawu Deposit. Minerals 2021, 11, 446. https://doi.org/10.3390/min11050446

AMA Style

Xu Z, Wu C, Zhang Z, Xu J, Li X, Jin Z. Separation of Fe from Mn in the Cryogenian Sedimentary Mn Deposit, South China: Insights from Ore Mineral Chemistry and S Isotopes from the Dawu Deposit. Minerals. 2021; 11(5):446. https://doi.org/10.3390/min11050446

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Xu, Zhiming, Chengquan Wu, Zhengwei Zhang, Jinhong Xu, Xiyao Li, and Ziru Jin. 2021. "Separation of Fe from Mn in the Cryogenian Sedimentary Mn Deposit, South China: Insights from Ore Mineral Chemistry and S Isotopes from the Dawu Deposit" Minerals 11, no. 5: 446. https://doi.org/10.3390/min11050446

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