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Article

Genesis of Megacrystalline Uraninite: A Case Study of the Haita Area of the Western Margin of the Yangtze Block, China

by
Zhengqi Xu
1,2,3,*,
Minghui Yin
1,3,*,
Youliang Chen
2,3,
Lu Xiang
3,
Hao Song
1,2,3,
Chengjiang Zhang
1,2,3,
Jian Yao
4 and
Hu Guo
5
1
Earth Exploration and Information Technology Key Laboratory of Ministry of Education, Chengdu University of Technology, Chengdu 610059, China
2
Sichuan Key Laboratory of Geoscience and Nuclear Technology, Chengdu University of Technology, Chengdu 610059, China
3
College of Earth Sciences, Chengdu University of Technology, Chengdu 610059, China
4
No. 280 Research Institute, China National Nuclear Corporation, Guanghan 618300, China
5
Tianjin Center, China Geological Survey, Tianjin 300170, China
*
Authors to whom correspondence should be addressed.
Minerals 2021, 11(11), 1173; https://doi.org/10.3390/min11111173
Submission received: 14 September 2021 / Revised: 16 October 2021 / Accepted: 20 October 2021 / Published: 22 October 2021
(This article belongs to the Special Issue Geochemistry, Mineral Chemistry and Geochronology of Uranium Deposits)
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Abstract

:
Megacrystalline uraninite (up to one centimeter in size) represents one of the most important discoveries in uranium mineralogy in the western margin of the Yangtze Block and even in China in recent years. However, the genesis of megacrystalline uraninite remains controversial. In this study, the megacrystalline uraninite found in the felsic and quartz veins in the Haita area is examined for the first time. The study examined the geochemical characteristics of uraninite in the two veins and resulted in two primary findings. (1) The genesis of the uraninite was likely intrusive and was closely related to partial melting. (2) The quartz vein and feldspar vein are cogenetic and have a simple differentiation evolution relationship. Therefore, the partial melting of felsic materials during migmatization may be the most important mechanism of uranium mineralization in the study area. Furthermore, further simple fractional crystallization may be another important mechanism for the formation of megacrystalline uraninite. This study enriches the REE database of uraninite in uranium deposits worldwide, which is meaningful for studying the genesis of megacrystalline uraninite.

1. Introduction

Uraninite is commonly found in uranium deposits formed in a variety of geological environments. These include high-grade metamorphic conditions as well as plutonic, metasomatic, hydrothermal, and basin diagenetic environments. These deposits may also be found in volcanic to sedimentary and superficial environments [1,2,3,4,5]. They contain a variety of elements, such as Th4+, REE3+, and Y3+, substituting U4+ with eight-fold coordination [6,7]. Uraninites of different genesis have significant differences in their chemical composition [2], which are controlled by the respective forming conditions, such as temperature, pressure, fluid composition, and oxygen fugacity [8]. Th has low solubility in low- to intermediate-temperature fluid. High-temperature uraninite tends to have a higher Th content than low-temperature uraninite [7,9,10,11]. In addition, uraninite from different geological conditions also has distinct REE contents and distribution patterns. Consequently, the composition of uraninite (e.g., ∑REE, U/Th ratio, Y and Zr contents, and LREE/HREE ratio) is useful for investigating its genesis [7,12,13,14,15,16,17].
Uraninite crystals are commonly smaller than 1 mm and are widespread in felsic or alkaline igneous rocks as an accessory mineral. Therefore, there are few reports of megacrystalline uraninite [18]. Uranium occurrences containing megacrystalline layers have been discovered in several migmatites along the western margin of the Yangtze Block in Southwest China. The megacrystalline uraninite found in the quartz vein in 2015 has attracted wide attention from geologists [19,20,21]. Its most prominent feature is its large particle size (up to one centimeter in scale) and complete crystal form [19,20]. In 2021, our research team discovered a large number of megacrystalline uraninites in the felsic vein of the A19 uranium occurrences in the Haita area. These megacrystalline uraninites in different veins in the Haita area provide natural and advantageous conditions for conducting research on their genesis.
In the study area, the geochemical and fluid inclusion characteristics of uraninite-rich quartz/felsic veins have led to valuable insights into the petrological, chronological, and geochemical attributes of the migmatite. The studies by Chang [22] and Liu [23] suggest that the initial enrichment of uranium was completed during the process of migmatization, and the uraninite in the felsic vein and quartz vein were formed in the Neoproterozoic. Guo et al. [24] suggest that the high-temperature hydrothermal process during migmatization in the study area led to the occurrence of uranium enrichment events, and the superimposed transformation of a late medium–low-temperature hydrothermal environment was the key factor for the formation of megacrystalline uraninite. Yin et al. [25] showed that the formation of coarse-grained uraninite was closely related to the increase in oxygen fugacity by studying the geochemical characteristics of apatite intergrown with uraninite in the quartz vein. However, the genesis of uraninite remains controversial, including the formation temperature (high temperature [19,20], low temperature [24]); genetic types (hydrothermal [19,26] and high differentiation evolution of magma [20,25,27,28]). In addition, there is controversy as to whether the ore-bearing quartz vein and felsic vein were formed by the same geological event [22,24]. These controversies seriously restrict the further understanding of regional uranium metallogenic events. Therefore, this study selected uraninite in the quartz vein and felsic vein as the object of geochemical testing and compared the test results with uraninite geochemical characteristics in typical uranium deposits worldwide. The origin of uraninite and other metallogenic information is discussed by comparing the uraninite geochemical characteristics in different ore-bearing veins, the internal relationship between the quartz vein and felsic vein, the relationship between these veins and nearby rock masses, and by collecting the Hf content of zircon in different veins. Based on the results, the genesis of uraninite is determined and is discussed. This study is also helpful for the geological exploration of uranium deposits in the region.

2. Geological Background

2.1. Regional Geological Background

The western margin of the Yangtze Block is located in Southwest China (Figure 1a), an area with complex geological structures, diverse rock associations, and abundant ore resources [29,30,31]. Proterozoic to Quaternary rocks are variably exposed in the area and Precambrian rocks are common (Figure 1b). Magmatic rocks include ultramafic, mafic, acidic to alkaline, and intrusive to volcanic rocks that were formed from the Proterozoic to Mesozoic. In particular, many mafic to acidic intrusive rocks that formed during the Jinning period (800 Ma to 1000 Ma) are widespread along the NS-trending structural belt.

2.2. Geological Background of the Study Area

The study area is in the southwest portion of Miyi County, an area that has experienced extensive metamorphism and migmatization (Figure 1c). The strata in the area mainly comprise Proterozoic medium- to high-grade metamorphic rocks of the Wumaqing Group and Sinian—Cambrian carbonate and clastic rocks of the Dengying Formation. Multistage magmatism is widespread in this area. Magmatic rocks are dominated by Jinningian intermediate to felsic rocks and Hercynian—Indochina alkaline rocks. The study area is also characterized by extensive folding and shear zones involving brittle and ductile faults, such as the NS-oriented Mopan Mountain and Anning River faults. Although most rocks in the area have experienced significant deformation and metamorphism, the original structure was variably eliminated by substantial surface weathering processes. The host rocks of the uranium ore body are migmatites of the Proterozoic Wumaqing Formation, which formed during the Neoproterozoic. The leucosomes and melanosomes of the migmatites have sharp boundaries. The melanosome is mainly composed of mica-quartz schist/gneiss. The leucosome mainly comprises quartz, plagioclase, and potassium feldspar, with minor uraninite, apatite, sphene, and sulfide. Three uranium occurrences (A10, A19, and 2811) were discovered in this area. Uraninite at A10 and A19 occurs in felsic veins composed of feldspar and quartz, while the leucosome in 2811 contains >80% quartz and was regarded as a quartz vein.

2.3. Geology of Uranium Occurrences

The uraninite-rich felsic vein is emplaced in the plagioclase gneiss along the schistosity (Figure 2a). More euhedral dark minerals (pyroxene and hornblende) are found in the felsic vein (Figure 2c,d), which may have formed by wall–rock alteration. Uraninite (UrA) intergrown with dark minerals has the characteristics of large particle size but subhedral crystal shape (Figure 2e). Uraninite (UrB), which is intergrown with quartz and feldspar (Figure 2f,g,h), is characterized by a nearly euhedral crystal shape with a smaller particle size. The main accessory minerals are sphene, apatite, zircon, molybdenite, and pyrite (Figure 2b,d,h).
The uraninite-bearing quartz vein occurs as a lens hosted by plagioclase gneiss (Figure 3a). It is up to 35–50 cm wide and nearly parallel to the gneissic schistosity. Hundreds of euhedral uraninite grains up to several centimeters in size were observed in the vein (Figure 3b). Euhedral sphenes were commonly enclosed in uraninite (UrC) (Figure 3d). The coexisting accessory minerals were quartz, apatite, zircon, molybdenite, pyrite, and minor feldspar (Figure 3c,e).

3. Analytical Methods

In this study, six specimens of uraninite-rich felsic vein (Figure 2a) and three hand specimens of uraninite-rich quartz vein (Figure 3a) were collected from the A19 and 2811 uranium occurrences. The samples were preprocessed in the Geochemistry Department at Chengdu University of Technology (CDUT). Thin sections of samples of the quartz vein (No. 2811) and felsic vein (No. A19) were prepared for optical microscopy study and microprobe analysis. Through the detailed rock and ore identification work, the uraninite which was symbiotic with dark minerals and the uraninite which was symbiotic with quartz and feldspar in felsic vein were selected, respectively, and the uraninite occurring in quartz vein was selected for testing. Whereas rock and mineral identification was performed in the Comprehensive Rock and Mineral Identification Laboratory at CDUT using a Nikon LV100 POL polarizing microscope.
Major element (U, Th, Pb) analyses were conducted using an electron probe microanalyzer (EPMA-1600) at the Tianjin Center of the Geological Survey of China. Tests were conducted using the following settings: an accelerating voltage of 15.0 kV, a beam current of 20.0 nA, and a beam spot diameter of 1 µm, with a ZAF calibration mode and operational procedures performed based on the GB/T 15617–2002 standard. The standard sample used in the test process was the SPI standard sample group from the United States, and the test accuracy was better than 2%. The SPI standard sample contains 53 selected minerals, each of which has a high degree of homogeneity within and between crystal grains, and has stable performance in a vacuum, atmospheric environment and electron beams. When measuring the trace element concentrations in the same position, glass reference standards, including SRM610, BHVO–2G, BCR–2G, and IR–1G, were used as the external standard samples. An SRM610 standard sample was clamped with seven sample points, and 238U was used as the internal standard element for the correction of trace elements. The time-resolved analyses data included an approximately 20 s blank signal and 50 s sample signal. The ICPMS-DATACAL software was employed for offline data processing [32,33].

4. Geochemical Composition of Uraninite

In total, 33 points were analyzed. These included 20 uraninite grains from the felsic vein (10 grains each from UrA and UrB) and 13 UrC grains from the quartz vein.

4.1. Major Element Compositions

The contents of major elements of UrA in the felsic vein were as follows (Table 1): UO2 was 88.50–89.91% (mean = 89.11%), ThO2 was 2.94–3.87% (mean = 3.49%), and PbO2 was 2.82–3.10% (mean = 2.95%). The UrB elements in the felsic vein were as follows: UO2 was 88.75–89.94% (mean = 89.25%), ThO2 was 2.37–3.19% (mean = 2.77%), and PbO2 was 2.65–2.94% (mean = 2.83%). The contents of major elements of UrC in the quartz vein were as follows: UO2 was 84.40–86.01% (mean = 85.13%), ThO2 was 4.68–6.15% (mean = 5.34%), and PbO2 was 2.81–3.24% (mean = 3.03%). In addition, the uraninite tested in this study contained lesser amounts of Ca, Fe, Ti, Si, and other elements.

4.2. Trace Element Compositions

The test data are shown in Table 2. ∑REE of UrA was 9625.94–21,224.89 ppm (mean = 17,379.98 ppm), (La/Yb) N = 0.01–0.13 (mean = 0.05). ∑REE of UrA had an obvious negative Eu anomaly (δEu = 0.23–0.40, mean = 0.31). ∑REE of UrB was 15,213.27–18,141.44 ppm (mean = 17,034.62 ppm), and the difference of light REE (LREE) and heavy REE (HREE) was clear (La/Yb) N = 0.08–0.14 (mean = 0.11), with an obvious negative Eu anomaly (δEu = 0.36–0.42, mean = 0.39). The ∑REE of UrC was 12,114.26–15,279.34 ppm (mean = 13,600.93 ppm) and the difference of LREE and HREE was obvious (La/Yb) N = 0.10–0.12 (mean = 0.11), with an obvious negative Eu anomaly (δEu = 0.35–0.37, mean = 0.37). In the REE distribution curve (Figure 4e), UrA and UrB in the felsic vein and UrC in the quartz vein show relatively flat distribution patterns with high total amounts, while the obvious negative Eu anomaly may be related to plagioclase minerals in the source region.
In addition, UrA and UrB in the felsic vein and UrC in the quartz vein have high concentrations of Zr and Y. Zr content in UrA was 78.17–163.70 ppm (mean = 107.58 ppm) and in UrB was 98.91–166.89 ppm (mean = 133.88 ppm). The Zr content in UrC was 101.05–213.52 ppm (mean = 149.02 ppm). The Y content in UrA was 6571.92–15164.90 ppm (mean = 12,087.72 ppm) and the Y content in UrB was 9027.06–11,348.09 ppm (mean = 10,626.93 ppm). The Y content in UrC was 7706.36–10,141.08 ppm (mean = 8813.00 ppm).

5. Discussion

5.1. Comparison of Genetic Type

Uraninite occurring at different temperatures and environments has specific rare earth element (REE) contents and patterns [17,34]. At medium to low temperatures (<350 °C) uraninite has a low REE content and a strongly fractionated REE pattern owing to the crystallographic control of the mineral structure. It demonstrates a preferential incorporation of Tb, Dy, Ho, and Er that have similar ionic radii to U4+, leading to “bell shape” REE patterns. At a temperature of >350 °C, the dilatational nature of the uraninite structure allows the incorporation of large amounts of REEs without fractionation (ΣLREE/ΣHREE ≈ 1, intrusive and synmetamorphic deposits), resulting in “flat” REE patterns and a strong negative Eu anomaly reflecting early fractionation of plagioclase in the silicate melt for intrusive deposits. Therefore, the degree of fractionation and REE content are important criteria for indicating temperature of uraninite crystallization and thus the genetic environment of formation. The results of this test show that all uraninite had a higher total amount of REEs and relatively flat seagull-type REE distribution patterns. The fractionation of REEs during the formation of the studied uraninite is not obvious, indicating that it was formed in a high-temperature environment. Mercadier et al. [17] systematically summarized the REE distribution patterns of uranium minerals in typical intrusive, synmetamorphic, unconformity-related, vein-type, roll-front, and volcanic-related uranium deposits worldwide (Figure 4a–d). Uraninite in the study area was compared with the REE distribution patterns of uraninite in typical uranium deposits worldwide and found to be consistent with REE distribution patterns of uranium minerals in intrusive (pegmatite) uranium deposits (Figure 4a,e). In the REE and LREE/HREE diagrams (Figure 4f), the uraninite in the study area is plotted in the field of intrusive (pegmatite) uranium deposits.
Based on the research results of Mercadier et al. [17] and Frimmel et al. [7], the U/Th ratio, ∑REE, and uraninite distribution patterns can be used to roughly reflect the ore-forming temperature and genetic environment. The concentrations of trace elements such as Zr and Y can be used to indicate the genesis of uraninite.
(1) The U/Th ratio of uraninite varies greatly depending on the crystallization temperature. All examples of low-temperature hydrothermal uraninite do not contain Th (U/Th > 1000), while those formed at higher temperatures (>450 °C) usually have a higher ThO2 content (U/Th < 100).
(2) Because Y and REE have the same geochemical properties, the Y and REE contents are usually positively correlated. Additionally, the higher the temperature, the stronger is the isomorphism. Therefore, the REE and Y concentrations will greatly increase under high-temperature conditions.
(3) The Zr content in all low-temperature hydrothermal uraninite is very low; usually not more than a few ppm.
In this study, the U/Th ratios of UrA, UrB, and UrC were all <100 in the Th and U concentration diagrams (Figure 5a). Owing to the increase in Th content in UrC, the U/Th ratio of UrC was lower than that of UrA and UrB. Therefore, we suggest that all uraninite examined in this study formed at a high temperature. UrA, UrB, and UrC have relatively uniform REE and Y contents. REE and Y concentrations show a significant positive correlation, and all the data plotted in the field of magmatic deposits on the REE vs. Y diagram (Figure 5b). UrA, UrB, and UrC have relatively stable and high concentrations of Zr, which is similar to the intrusive (pegmatite) Ekomedion deposit (Figure 6a).
The above features indicate that the uraninite from the quartz and felsic veins in the study area originated from intrusive rock. We suggest that such uranium mineralization be classified into the subtype of Pegmatite-Alaskite [4] according to the IEAE (International Atomic Energy Agency) classification. This type of uraninite is formed by partial melting in high-temperature and low-pressure environments.

5.2. Relationship between the Felsic and Quartz Veins

Although the ore-bearing veins are not pegmatite, uraninite geochemical characteristics all show an intrusive type origin, which may be due to the relatively low metamorphic temperature (amphibolite facies) in the study area. Therefore, no Pegmatite-Alaskite similar to the Luoxin (Namibia) and Guangshigou (China) uranium deposits were formed. This can be demonstrated by the formation of euhedral dark minerals in the felsic vein. The dark euhedral minerals formed by plagioclase gneisses on both sides of metasomatic felsic veins during emplacement are mainly plagioclase and pyroxene. The corresponding metamorphic lithofacies is hornblende, indicating that the dark minerals were formed at medium—high temperatures (about 500 °C) and medium—high pressure. This is consistent with the Guo et al. [24] result showing that the homogenization temperature of the inclusions in the felsic veins was concentrated at 380–540 °C. The homogenization temperature of some primary inclusions in quartz veins tested by Guo et al. [24] was concentrated at 140–220 °C in addition to high-temperature inclusions. This is inconsistent with the higher mineralization temperature reflected by the UrC geochemical characteristics. In contrast, we believe that the formation temperature of such inclusions may represent the lower limit of the formation temperature of uraninite. Thus, the formation of coarse-grained uraninite occurs during a slow decline from medium to high temperatures (about 500 °C) to medium-low temperatures (140–220 °C).
The symbiotes closely related to uraninite in the felsic vein and quartz vein are apatite, sphene, and molybdenite, which may imply that the felsic and quartz veins have a certain genetic relationship. UrA, UrB, and UrC have the same REE distribution patterns, indicating that the felsic and quartz veins have the same genesis. By comparing the ThO2 content of uraninite in different veins (Figure 6b), it was found that the ThO2 content of UrC was significantly higher than that of UrA and UrB, which may indicate that the quartz vein was formed at a lower temperature resulting from the evolution of the felsic magma. The biggest limiting factor for the formation of large grained uraninite is the slow decrease in temperature [36]. The particle size of UrB formed in the quartz vein is relatively small (Figure 2g,h), while the particle size of UrC formed in the quartz vein can reach more than 1 cm (Figure 3b,d), which indicates that the formation of large grain uraninite is facilitated by the slow decrease of temperature during simple fractional crystallization combine the evidence mentioned above.

5.3. Discussion on Genesis of Uraninite

Because U in a silicate magma has a large ionic radius and high valence, it cannot easily enter the structure of the main rock-forming minerals. This leads to the preferential existence of U in the silicate melt during the partial melting and crystal differentiation processes [37]. Theoretically, there are two methods to produce uranium-rich silicate rock masses. One method is the extreme differentiation of highly differentiated silicate magma, which is often regarded as Uranium-rich granite. Its uranium minerals exist in the form of accessory minerals and have small particles. Therefore, there are few reports on the formation of large-grained uraninite [18,38]. Another way to make silicate melts rich in uranium is by low-degree partial melting of the parent rock [39,40]. Mercadier et al. [40] proved that under very low partial melting (<5%) conditions, the concentration of U in a silicate melt can reach 300 ppm. Kukkonen and Lauri [41] used model calculations to prove that uranium can be enriched dozens of times in the parent rock under low-degree partial melting conditions. Therefore, even if the U content in the parent rock is normal, partial melting will cause the U content in the melt to increase. Because of the similar geochemical properties of Th and U, similar Th enrichment behavior also occurs under low-degree partial melting conditions [38,41].
Qu [28] studied the petrological and geochemical characteristics of major and trace elements, and the diagenetic ages of the main rock mass (Dingzhen rock mass) in the Haita area and classified these rock masses as hyper aluminous high-K calc-alkaline potassic basalt series of highly differentiated A2 granites. The Hf content in zircon has a positive correlation with magma evolution [42]. That is, the highly differentiated granite zircon is rich in Hf. By collecting the Hf content of zircons from different veins tested by the research team (unpublished data), it was discovered that the Hf content of zircon in the quartz vein is 8019.56–15,215.86 ppm (mean = 11,139.80 ppm), while that in the felsic vein is 7546.19–13,563.58 ppm (mean = 10,067.95 ppm). The Hf contents of zircons in the two veins are low, indicating that the magma had a low degree of evolution. The euhedral dark minerals in the felsic vein led to the metamorphic facies in the study area being defined as hornblende facies. Chen et al. [38] studied the Guangshigou uranium deposit and found that the hornblende facies is the key to the formation of uranium-rich pegmatitic magma, which is also applicable to the study area. The low Hf content of zircon indicates that the two veins were unrelated to the Dingzhen rock mass during genesis. Amphibolite facies limited by dark minerals indicate uranium mineralization in the study area during migmatization. Therefore, it is speculated that uranium mineralization in the study area is closely related to the partial melting of felsic material caused by migmatization. The combined research team found in previous research that the mica quartz schist and gneiss components of migmatite veins in the study area are para-metamorphic rocks formed by the metamorphism of sedimentary rocks. The U concentrations ranged from 5.64 to 12.90 ppm, with an average of 8.89 ppm. The average Th/U ratio of 2.97 falls within the range of values reported for U-rich rocks [22]. After the onset of migmatization, the U concentrations of the granites formed by in situ anatexis of metamorphic rocks varied from 12.90 to 29.50 ppm, with an average of 21.30 ppm. The average Th concentration and average Th/U ratio were 59.13 ppm and 3.20, respectively. These rocks, which belong to the U-rich granite body, reflect the completion of preliminary U enrichment during the migmatization process. The U-rich granite body is one of the most likely U sources linked to ore-forming fluid evolution in the study area. This is consistent with the conclusion of partial melting reflected in the geochemical characteristics of uraninite [22].
The low degree of partial melting of feldspathic materials during the migmatization may be the most important mechanism for uranium mineralization in the study area and even in the western margin of the Yangtze Block. Further simple fractional crystallization may be another important mechanism for the formation of megacrystalline uraninite.

6. Conclusions

The REE distribution patterns, the variation of ThO2 content, particle size, and the syngenetic assemblage of megacrystalline uraninite indicate that the quartz vein and felsic vein are related in genesis, and that the quartz vein may have formed by simple evolutionary differentiation of felsic magma.
We suggest that genesis of megacrystalline uraninite can be classified into the subtype of Pegmatite-Alaskite under intrusive type, which is formed by partial melting in high-temperature and low-pressure environments.
This study enriches the REE database of uraninite in uranium deposits worldwide, which is meaningful for studying the genesis of megacrystalline uraninite.

Supplementary Materials

The following are available online at https://www.mdpi.com/article/10.3390/min11111173/s1, Table S1: Chemical composition of megacrystalline uraninite.

Author Contributions

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

Funding

This study was financially supported by the Everest Scientific Research Program of Chengdu University of Technology (No. 2021ZF11413), The National Natural Science Foundation Program of China (No. 41872079, 42072096), The Applied Basic Research Program of Sichuan Province, China (No. 20YYJC2305), the Program of China National Uranium Company Limited (No. 20217).

Institutional Review Board Statement

Not applicable.

Informed Consent Statement

Not applicable.

Data Availability Statement

Data is contained within the article and Supplementary Materials.

Acknowledgments

We greatly appreciate the help of Jiaming Qi, Zhibo Zhang, Guangwen Huang, and Pengfei Fan during daily discussion work.

Conflicts of Interest

The authors declare no conflict of interest.

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Minerals 11 01173 g001 550
Figure 1. (a) Location of the Kangdian region in China, (b) geological map of the Kangdian region, and (c) geological map of the Haita area (modified after Wang et al. [20]).
Figure 1. (a) Location of the Kangdian region in China, (b) geological map of the Kangdian region, and (c) geological map of the Haita area (modified after Wang et al. [20]).
Minerals 11 01173 g001
Minerals 11 01173 g002 550
Figure 2. (a) Felsic vein (Fv), (b) Molybdenite in felsic vein, (c) Dark idiomorphic mineral in felsic vein, (d) Uraninite in dark idiomorphic mineral, (e) Megacrystalline uraninite in dark idiomorphic mineral, and (f–h) Megacrystalline uraninite in felsic vein. Abbreviations: Pl, Plagioclase gneiss; Mo, Molybdenite; Py, Pyroxene; Am, Amphibole; Ap, Apatite; Sp, Sphene.
Figure 2. (a) Felsic vein (Fv), (b) Molybdenite in felsic vein, (c) Dark idiomorphic mineral in felsic vein, (d) Uraninite in dark idiomorphic mineral, (e) Megacrystalline uraninite in dark idiomorphic mineral, and (f–h) Megacrystalline uraninite in felsic vein. Abbreviations: Pl, Plagioclase gneiss; Mo, Molybdenite; Py, Pyroxene; Am, Amphibole; Ap, Apatite; Sp, Sphene.
Minerals 11 01173 g002
Minerals 11 01173 g003 550
Figure 3. (a) Quartz vein (Qv), (b,c) Megacrystalline uraninite in quartz vein, (d) BSE of megacrystalline uraninite, (e) Apatite and sphene in quartz vein.
Figure 3. (a) Quartz vein (Qv), (b,c) Megacrystalline uraninite in quartz vein, (d) BSE of megacrystalline uraninite, (e) Apatite and sphene in quartz vein.
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Minerals 11 01173 g004 550
Figure 4. (a–d) Chondrite-normalised rare earth element patterns for uranium oxides from six different types of uranium occurrences (data from Mercadier et al. [17]), (e) Chondrite-normalized rare earth element patterns of UrA/UrB/UrC (Chondrite values are from Anders and Grevesse [35]), and (f) Rare earth element abundance (ΣREE) vs. REE fractionation ((ΣLREE/ΣHREE) N) from six different types of uranium occurrences and UrA/UrB/UrC
Figure 4. (a–d) Chondrite-normalised rare earth element patterns for uranium oxides from six different types of uranium occurrences (data from Mercadier et al. [17]), (e) Chondrite-normalized rare earth element patterns of UrA/UrB/UrC (Chondrite values are from Anders and Grevesse [35]), and (f) Rare earth element abundance (ΣREE) vs. REE fractionation ((ΣLREE/ΣHREE) N) from six different types of uranium occurrences and UrA/UrB/UrC
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Minerals 11 01173 g005 550
Figure 5. (a) Th versus U content in uraninite from various types of deposits and UrA/UrB/UrC, and (b) REE versus Y content in uraninite from various types of deposits and UrA/UrB/UrC (data from Frimmel et al. [7] and this study). Abbreviations: Vt., Vein-type; In., Intrusive.
Figure 5. (a) Th versus U content in uraninite from various types of deposits and UrA/UrB/UrC, and (b) REE versus Y content in uraninite from various types of deposits and UrA/UrB/UrC (data from Frimmel et al. [7] and this study). Abbreviations: Vt., Vein-type; In., Intrusive.
Minerals 11 01173 g005
Minerals 11 01173 g006 550
Figure 6. (a) V versus Zr content in uraninite from various types of deposit and UrA/UrB/UrC (data from Frimmel et al. [7] and this study), and (b) ThO2 versus UO2 content in uraninite from UrA/UrB/UrC.
Figure 6. (a) V versus Zr content in uraninite from various types of deposit and UrA/UrB/UrC (data from Frimmel et al. [7] and this study), and (b) ThO2 versus UO2 content in uraninite from UrA/UrB/UrC.
Minerals 11 01173 g006
Table
Table 1. Oxide concentrations (wt %) of megacrystalline uraninite.
Table 1. Oxide concentrations (wt %) of megacrystalline uraninite.
NO.Na2OMgOAl2O3SiO2PbOThO2UO2K2OCaOTiO2FeOTotal
UrA1/0.013/0.0122.7592.72288.7470.1590.2330.0360.08094.761
UrA20.0140.002/0.022.8773.16489.0670.1610.2720.030/95.607
UrA3///0.0382.7593.00789.9400.1510.2770.0140.06596.251
UrA40.009//0.0202.7733.18989.1860.1560.2380.0730.03395.677
UrA50.022//0.0152.9392.67189.3270.1480.2540.019/95.395
UrA6///0.0182.8532.65388.9930.1620.2440.005/94.928
UrA70.0060.006/0.0222.9052.55589.8900.1620.2610.0060.02995.842
UrA8///0.0222.932.91288.8610.150.2350.0490.02795.186
UrA90.002//0.0282.8332.3789.0910.1450.1510.0620.17294.854
UrA100.0050.01/0.6222.6522.49889.4330.1650.3050.0090.07495.773
UrB10.0030.017/0.0223.0563.42788.4960.1590.3310.039/95.55
UrB20.0220.019/0.0192.9762.93889.9090.1610.3540.083/96.481
UrB30.0290.004/0.0353.0963.33589.3870.1390.3160.037/96.378
UrB40.0030.015/0.0352.9453.45589.3970.1740.3770.001/96.402
UrB50.010.018/0.0532.8183.41288.9850.1690.3540.022/95.841
UrB60.0010.0050.0080.7202.8513.42088.9570.1780.3040.0490.05096.543
UrB7/0.003/0.0352.9693.87089.0510.1560.3120.0550.04096.491
UrB80.0260.011/0.0262.9613.63889.4370.1670.2600.0520.00796.585
UrB9/0.023/0.0402.8533.57088.6830.1660.4020.033/95.77
UrB10/0.005/0.0012.9383.84188.8450.1520.3340.061/96.177
UrC10.020.004/0.0603.2384.67984.9960.2520.3010.027/93.577
UrC20.0050.0050.0460.0502.9764.72684.4400.2290.4140.0140.03492.939
UrC30.004//0.0172.8065.21785.5830.1710.3690.0820.04794.296
UrC40.0120.013/0.0702.9385.23385.5520.2110.3500.059/94.438
UrC50.007//0.0842.9946.14784.3960.1850.2620.043/94.118
UrC6///0.0953.0315.67284.5890.2270.3130.0260.01893.971
UrC7/0.011/0.0953.0635.63984.7580.1910.4820.0150.06494.318
UrC80.009//0.0453.2245.26185.4390.2050.2790.0280.01094.500
UrC90.0170.009/0.0703.0514.97785.8280.2390.4130.014/94.618
UrC100.009/0.8160.1563.0935.24784.8150.1700.4900.0280.00494.828
UrC110.013//0.0623.0955.39986.0660.2070.3440.0290.00295.217
UrC120.0060.0160.0320.0612.8575.42985.1650.2050.4630.044/94.278
UrC130.022//0.0672.9985.77285.1250.2000.3240.050/94.558
Note: / =below detectable limit
Table
Table 2. Trace element composition of megacrystalline uraninite.
Table 2. Trace element composition of megacrystalline uraninite.
NO.VYZrLaCePrNdSmEuGdTbDyHoErTmYbLuHf
UrA13.78 13,361.93 122.12 81.36 1925.00 528.19 3599.89 1934.33 179.20 2193.33 402.89 2987.46 694.52 1996.01 295.10 1963.88 218.99 0.49
UrA22.53 10,847.38 95.59 25.63 1220.05 400.80 2922.62 1566.42 154.02 1797.94 323.29 2336.55 560.95 1607.01 230.82 1572.98 179.02 0.33
UrA32.60 6751.92 91.55 16.89 789.21 262.58 2048.07 1012.02 139.45 1133.26 199.62 1430.58 335.83 983.84 143.71 1007.52 123.36 0.24
UrA42.81 11,089.65 89.55 27.15 1207.74 386.20 2866.49 1552.08 173.87 1840.48 331.87 2383.82 557.59 1635.11 245.47 1602.79 186.62 0.28
UrA53.20 14,364.34 85.57 35.02 1516.55 473.73 3454.72 1838.54 177.63 2206.75 427.65 3150.71 721.65 2143.83 310.74 2125.68 238.39 0.41
UrA63.91 12,002.10 163.70 309.63 4238.08 844.89 4595.41 1773.90 185.18 1898.67 353.99 2502.39 593.11 1722.55 252.00 1757.59 197.49 0.74
UrA75.06 12,322.04 158.78 313.81 4007.86 796.15 4512.94 1745.23 186.17 1985.75 363.67 2543.86 608.03 1771.57 252.68 1784.60 199.93 0.90
UrA84.03 15,164.90 94.15 26.69 1394.84 435.16 3316.43 1942.52 164.84 2376.74 446.57 3331.00 778.19 2287.38 329.25 2234.14 244.75 0.44
UrA95.29 12,593.88 78.17 73.52 1672.30 464.30 3161.90 1610.78 223.97 1899.41 356.77 2622.23 629.77 1829.92 264.46 1894.10 215.16 0.35
UrA104.74 12379.11 96.66 127.28 2365.67 554.79 3631.23 1656.62 182.74 1876.94 353.86 2551.39 610.82 1767.58 263.67 1780.48 209.41 0.53
UrB10.11 11,043.63 104.01 218.24 2510.62 551.69 3389.77 1538.18 165.82 1805.19 333.18 2440.02 572.39 1695.01 243.00 1660.22 189.75 0.76
UrB20.05 10,707.16 98.91 186.84 2490.20 544.70 3246.34 1484.17 214.83 1736.41 325.25 2396.59 565.28 1672.90 237.94 1636.68 190.85 1.11
UrB30.10 11,348.09 147.70 259.27 2903.89 598.11 3463.29 1571.05 200.65 1832.11 339.11 2455.77 593.48 1718.50 246.80 1688.02 194.60 1.49
UrB40.04 11,275.54 152.07 256.06 2887.86 609.73 3528.70 1590.68 211.82 1818.41 332.57 2484.59 578.35 1715.22 244.23 1686.15 197.06 1.30
UrB50.02 11,098.00 151.00 256.66 2869.11 590.55 3487.95 1552.83 199.32 1761.91 330.95 2448.63 572.09 1670.86 243.02 1641.45 196.16 1.13
UrB60.51 9677.55 138.54 169.79 2331.16 506.77 3010.07 1362.88 197.42 1532.27 281.97 2072.87 494.05 1423.35 207.68 1474.83 172.37 0.61
UrB70.37 10,448.28 166.89 316.64 3063.05 626.92 3462.49 1510.98 203.16 1691.28 314.37 2302.84 538.10 1582.47 229.24 1573.23 184.33 1.61
UrB80.20 11,149.91 132.13 248.35 2694.28 569.86 3314.47 1534.65 216.13 1748.59 328.83 2431.49 575.31 1686.16 245.04 1685.18 197.76 1.12
UrB90.25 9027.06 121.18 238.15 2747.04 542.16 3057.23 1318.82 186.48 1438.90 268.07 1903.85 457.34 1356.20 196.54 1339.53 162.94 0.48
UrB100.34 10,494.09 126.37 201.13 2536.71 535.48 3160.21 1484.23 192.73 1675.22 311.15 2328.38 534.05 1592.50 231.82 1585.89 181.08 0.79
UrC11.54 7706.36 141.83 174.92 2016.67 411.08 2406.91 1013.54 133.53 1136.31 207.01 1537.51 383.49 1161.50 170.34 1217.54 143.90 0.57
UrC20.47 8471.67 115.06 210.35 2164.55 432.97 2483.67 1080.87 140.75 1228.42 223.12 1674.94 426.69 1299.89 191.19 1360.06 163.98 0.48
UrC31.89 8948.43 114.58 193.72 2202.64 448.04 2626.37 1110.83 145.92 1267.47 232.85 1736.58 442.23 1334.32 196.45 1391.19 169.38 0.57
UrC40.34 8742.42 175.81 191.47 2188.19 445.13 2574.38 1099.36 143.38 1261.68 228.98 1718.85 436.62 1333.54 195.69 1396.17 168.93 0.91
UrC50.78 8587.08 110.09 210.68 2394.16 464.08 2641.75 1083.51 137.43 1230.43 220.66 1662.78 419.98 1302.81 191.55 1385.97 166.14 0.57
UrC60.47 8347.09 101.05 209.24 2261.53 440.70 2477.16 1028.83 133.01 1189.24 218.17 1604.92 411.60 1261.34 187.82 1361.88 167.02 0.42
UrC70.79 9278.59 141.05 255.57 2420.54 476.92 2729.45 1153.95 149.84 1333.76 245.77 1803.37 462.93 1431.22 209.96 1490.12 183.35 0.81
UrC80.45 9266.14 213.52 205.00 2303.11 466.39 2698.70 1152.92 144.48 1305.24 236.98 1795.78 458.58 1434.80 211.44 1543.30 186.75 0.87
UrC92.38 7884.69 163.64 179.95 2079.02 425.71 2388.00 1035.53 137.54 1162.74 210.41 1558.65 400.04 1222.28 176.10 1265.46 150.88 0.64
UrC105.57 9634.39 194.74 241.43 2499.32 487.35 2745.06 1143.07 153.87 1331.84 246.47 1853.03 474.07 1477.31 213.45 1546.54 189.30 1.11
UrC110.15 9114.62 186.27 220.14 2356.95 477.90 2712.03 1136.25 140.57 1311.25 239.59 1778.94 458.05 1411.81 208.65 1499.53 182.50 0.60
UrC120.83 10,141.08 156.43 254.57 2621.67 511.55 2875.30 1227.34 169.02 1437.10 258.98 1952.98 485.20 1517.44 218.37 1563.90 185.90 0.62
UrC130.67 8446.43 123.17 208.92 2328.10 459.82 2564.20 1079.40 134.62 1249.46 224.93 1686.31 424.54 1296.42 189.51 1364.84 162.39 0.64
Note: content unit is ppm.
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Xu, Z.; Yin, M.; Chen, Y.; Xiang, L.; Song, H.; Zhang, C.; Yao, J.; Guo, H. Genesis of Megacrystalline Uraninite: A Case Study of the Haita Area of the Western Margin of the Yangtze Block, China. Minerals 2021, 11, 1173. https://doi.org/10.3390/min11111173

AMA Style

Xu Z, Yin M, Chen Y, Xiang L, Song H, Zhang C, Yao J, Guo H. Genesis of Megacrystalline Uraninite: A Case Study of the Haita Area of the Western Margin of the Yangtze Block, China. Minerals. 2021; 11(11):1173. https://doi.org/10.3390/min11111173

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Xu, Zhengqi, Minghui Yin, Youliang Chen, Lu Xiang, Hao Song, Chengjiang Zhang, Jian Yao, and Hu Guo. 2021. "Genesis of Megacrystalline Uraninite: A Case Study of the Haita Area of the Western Margin of the Yangtze Block, China" Minerals 11, no. 11: 1173. https://doi.org/10.3390/min11111173

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