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Article

Petrogenesis of Eocene A-Type Granite Associated with the Yingpanshan–Damanbie Regolith-Hosted Ion-Adsorption Rare Earth Element Deposit in the Tengchong Block, Southwest China

by
Zhong Tang
1,2,3,
Zewei Pan
1,2,3,
Tianxue Ming
2,3,
Rong Li
2,3,
Xiaohu He
4,*,
Hanjie Wen
1,5,* and
Wenxiu Yu
1
1
Faculty of Land Resources Engineering, Kunming University of Science and Technology, Kunming 650093, China
2
Institute of Yunnan Geology Survey, Kunming 650051, China
3
Key Laboratory of Sanjiang Metallogeny and Resources Exploration and Utilization, Ministry of Natural Resources (MNR) of the People’s Republic of China, Kunming 650051, China
4
School of Earth Sciences, Yunnan University, Kunming 650500, China
5
School of Earth Sciences and Resources, Chang’an University, Xi’an 710064, China
*
Authors to whom correspondence should be addressed.
Minerals 2024, 14(9), 933; https://doi.org/10.3390/min14090933
Submission received: 10 July 2024 / Revised: 3 September 2024 / Accepted: 10 September 2024 / Published: 12 September 2024
(This article belongs to the Special Issue Petrogenesis of Large Igneous Province and Rare Earth–Rare Metal Deposits)
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Abstract

:
The ion-adsorption-type rare earth element (iREE) deposits dominantly supply global resources of the heavy rare earth elements (HREEs), which have a critical role in a variety of advanced technological applications. The initial enrichment of REEs in the parent granites controls the formation of iREE deposits. Many Mesozoic and Cenozoic granites are associated with iREE mineralization in the Tengchong block, Southwest China. However, it is unclear how vital the mineralogical and geochemical characteristics of these granites are to the formation of iREE mineralization. We conducted geochronology, geochemistry, and Hf isotope analyses of the Yingpanshan–Damanbie granitoids associated with the iREE deposit in the Tengchong block with the aims to discuss their petrogenesis and illustrate the process of the initial REE enrichment in the granites. The results showed that the Yingpanshan–Damanbie pluton consists of syenogranite and monzogranite, containing REE-bearing accessory minerals such as monazite, xenotime, apatite, zircon, allanite, and titanite, with a high REE concentration (210–626 ppm, mean value is 402 ppm). The parent granites have Zr + Nb + Ce + Y (333–747 ppm) contents and a high FeOT/MgO ratio (5.89–11.4), and are enriched in Th (mean value of 43.6 ppm), U (mean value of 4.57 ppm), Zr (mean value of 305 ppm), Hf (mean value of 7.94 ppm), Rb (mean value of 198 ppm), K (mean value of 48,902 ppm), and have depletions of Sr (mean value of 188 ppm), Ba (mean value of 699 ppm), P (mean value of 586 ppm), Ti (mean value of 2757 ppm). The granites plot in the A-type area in FeOT/MgO vs. Zr + Nb + Ce + Y and Zr vs. 10,000 Ga/Al diagrams, suggesting that they are A2-type granites. These granites are believed to have formed through the partial melting of amphibolites at a post-collisional extension setting when the Tethys Ocean closed. REE-bearing minerals (e.g., apatite, titanite, allanite, and fluorite) and rock-forming minerals (e.g., potassium feldspar, plagioclase, biotite, muscovite) supply rare earth elements in weathering regolith for the Yingpanshan–Damanbie iREE deposit.

1. Introduction

The ion-adsorption-type rare earth element (iREE) deposit, also named as the regolith-hosted rare earth element (REE) deposit [1,2], is the accumulation of REEs in the regolith formed by the long-term physical and chemical weathering of REE-rich rocks such as granite, syenite, rhyolite, and metamorphic rocks [3,4,5]. The iREE deposits dominantly supply global resources of the heavy rare earth elements (HREEs, USA [6]), which are known as ‘industrial vitamins’ due to their critical role in a variety of advanced technological applications. This kind of REE deposit forms in supergene environment where REE is released from the granites and subsequently mainly absorbed by clay minerals in the weathering profile [7,8,9]. However, recent studies have proved that the REE contents and mineral assemblage in the parent granites also control the formation of ion-adsorption REE deposits [10]. The ion-adsorption-type REE deposits mostly show two to six times more enrichment of REEs compared to parent granites and been shown to have inherited the REE patterns of the parent granites [2,3,11]. Probing into the initial enrichment of REEs during the genesis of the parent granites is important to understand the formation of ion-adsorption REE deposits. It has been proposed that the magmatic sources with relatively high REE contents control the REE enrichment in the granites. However, in other studies, the magmatic evolution is considered to play a more important role in the REE enrichment and fractionation in the granites and contributes to the ion-adsorption REE mineralization [12,13]. Therefore, further studies on the source and magmatic evolution of the parent granite for iREE deposits are necessary to constrain the mechanism of initial REE enrichment.
In the Tengchong block of Southwest China, numerous Mesozoic and Cenozoic granites formed during the closure of the Neo-Tethys Ocean [14,15], and they could be classified as S-type granites [16,17,18,19], I-type granites [18,20], and A-type granites [16,21]. Many of these granites are associated with iREE mineralization [22]. However, it is unclear how the mineralogical and geochemical characteristics of these granites controlled the iREE mineralization. In this study, we conducted geochronology, geochemistry, and Hf isotope analyses of the Banggunjianshan granitoids associated with the Yingpanshan–Damanbie iREE deposit in the Tengchong block with the aims to (1) discuss the petrogenesis of these granites, (2) illustrate the process of the initial REE enrichment in the granites and (3) provide additional perspectives to unravel the ore-forming mechanism of the iREE deposit.

2. Geological Setting

The Tengchong block is a segment of the eastern Tethyan tectonic domain (ETTD, Figure 1a), and bounded by the Myitkyina suture to the west and the Gaoligong–Longling–Ruili fault to the east ([23]; see Figure 1b). The high-grade metamorphic basement, the Gaoligongshan group, consists of gneiss and migmatite [24,25,26,27]. These paragneisses and orthogneisses give zircon U-Pb ages ranging with 1053–635 Ma and 490–470 Ma, respectively [28]. The Meso-Proterozoic basement is obviously different from that of the Yangtze block in rock assemblages and tectono-magmatic events, and is considered to constitute part of the basement of the Gondwana supercontinent [29,30,31,32,33,34]. The Gaoligongshan Group is an unconformity covered by late–Paleozoic and early–Mesozoic carbonate and clastic rocks, Cenozoic conglomerates, sandstones, and Quaternary alluvial and fluvial deposits. The early-Paleozoic, Jurassic, and Cretaceous stratum are absent in the stratigraphic sequence. Three stages of magmatism in the Tengchong block have been reported: (1) Early Cretaceous (130–110 Ma) magmatic activities ([14,35,36,37,38] and references therein); (2) Late Cretaceous to early Cenozoic (75–64 Ma) magmatism [18,39,40,41,42,43]; and (3) Eocene (55–47 Ma) magmatism represented by mafic rocks, monzogranites, and granodiorites with mafic enclaves [18,39,40,41,42,43]. In addition, these three-stage granitoids are closely related to Sn–polymetallic deposits [40,44], granitic-pegmatite-type rare-metal mineralization [45] and iREE deposits [22] in the region. Specifically, regolith formed from intermediate-mafic intrusive rocks (e.g., diorite and gabbro) do not host rare earth mineralization according to extensive field investigations [46].
In recent years, numerous large or medium regolith-hosted iREE deposits, such as those in Long’an, Yingpanshan–Damanbie, Yiwanshui, Xinpaoshan, Shilingka, and Tuguanzhai (see Figure 1b), have been discovered by geological surveys, suggesting a large potential reserves of rare earth metals at the Tengchong block. These iREE deposits have been preserved in the regolith profiles of a few meters to tens of meters of thickness [53]. Ore bodies of these iREE deposits mainly occur at the bottom of the completely weathered layer of the regolith profiles. The proportion of ion-adsorbed REEs ranges from 4.69 to 73.33 wt.% [22,37,54]. REE-bearing minerals are mainly bastnasite, thorite, fergusonite. More than 80% of the regolith in the area is derived from the weathering of Eocene granites, while the rest are sourced from Cretaceous and Triassic granites, Quaternary basalt and rhyolite, or Cenozoic granitic gneiss [22,55]. Most of the parent granites associated with the iREE mineralization exhibit high contents of SiO2 (68–78 wt.%), Al2O3 (12–15 wt.%), and alkali elements (K2O + Na2O contents of 7.5–10.6 wt.%, mostly greater than 8 wt.%) [49,53,54,55,56,57,58,59]. A recent drilling project showed that the Yingpanshan–Damanbie deposit is a large iREE deposit with more than 100,000 tons (separated quantities of rare earth oxide, SREO) of estimated resources, and an average grade of 0.0526% (SREO). The weathered profile ranges from 10 to 32 m in thickness, and has a 0.8–16.1 m thickness of ore bodies, which is associated with the topography and geomorphology. The parent pluton associated with this deposit consists of monzogranite and syenogranite with ages of 48.0 to 50.8 Ma [22]. The Yingpanshan–Damanbie iREE deposit is located in Longchuan County, Yunnan Province, as shown in Figure 2.

3. Samples and Petrography

To evaluate the relationship between the petrogenesis of the parent granites and the initial REE enrichment mechanism in the parent granites comprised of monzogranite and syenogranite, we have collected 23 fresh samples from the intrusive body (also named Banggunjianshan granitic batholith). In the later supergene processes, this body has been weathered into regolith where the Yingpanshan–Damanbie iREE deposit was formed. The syenogranite is light gray, shows a porphyritic texture (Figure 3a), and is mainly comprised of quartz (20–23 vol.%), K-feldspar (45–50 vol.%), plagioclase (20–22 vol.%), and biotite (3–5 vol.%) (Figure 3b). These minerals are 1–10 mm in size. REE-bearing accessory minerals are monazite, xenotime, apatite, zircon, allanite, and titanite, which are mostly smaller than 1 mm in size, as revealed by Tescan Integrated Mineral Analyzer (TIMA, Brno, Czech Republic) images (Figure 3c). Syenogranite exhibits a slight alteration, with plagioclase and biotite partially altered to sericite and chlorite, respectively.
Monzogranite exhibits a porphyritic texture (Figure 4a) with quartz (15–20 vol.%, 2–15 mm in size), plagioclase (25–35 vol.%, 1–6 mm in size), and K-feldspar (25–35 vol.%, 2–10 mm in size) as the main phenocrysts (Figure 4b). The groundmass minerals are composed of biotite (3–10 vol.%), muscovite (1–3 vol.%) and other REE-bearing accessory minerals. These minerals are apatite, magnetite, titanite, zircon, and fluorite, mostly smaller than 1 mm in size, as revealed by TIMA images (Figure 4c). TIMA images also reveal significant late-stage fluoritization and carbonate hydrothermal alteration in these rocks (Figure 4c). Overall, REE-bearing minerals of parent rocks are mainly apatite, titanite, allanite, zircon, and fluorite, supplying the rare earth in the weathering regolith.

4. Analytical Methods

4.1. Zircon U–Pb Dating

The collected granite samples were manually crushed into samples that were smaller than 200 microns in size, and zircon grains were extracted by conventional gravity and electromagnetic separation at Langfang Chengxin Geological Services Co., Ltd. (Langfang, China) Zircon grains with clean surfaces and no cracks or inclusions were handpicked under a binocular microscope and mounted in epoxy resin. To identify their internal structure and to choose potential target sites for the U–Pb analysis, cathodoluminescence (CL) images (Figure 5) were obtained using a TESCAN Mira3 scanning electron microscope (TESCAN, Brno, Czech Republic) at Nanjing Hongchuang Geological Exploration Technology Services Co., Ltd. in Nanjing, China. Zircon U–Pb dating was conducted by using an Agilent 7900 inductively coupled plasma mass spectrometer (LA–ICP–MS, Santa Clara, CA, USA) combined with a Resolution SE 193nm laser ablation system (Applied Spectra, Fremont, CA, USA) at the microanalysis laboratory of Nanjing Hongchuang Geological Exploration Technology Services Co., Ltd. The laser was set to a fluence of 3 J/cm2, with a spot size of 32 μm, a repetition rate of 6 Hz and an ablation time of 47 s. The parameters were adjusted as detailed in Thompson et al. [60], and data processing was performed using the Iolite program (ver. 3.7) [61]. Zircon 91,500 was used as a calibration standard, and reference zircon GJ–1 served as a monitoring standard. For every 10–12 sample analyses, two 91,500 and one GJ–1 standards were measured. The ages obtained for 91,500 (1061.5 ± 3.2 Ma, 2σ) and GJ–1 (604 ± 6 Ma, 2σ) were consistent with the recommended values within the uncertainty range. Measured compositions were corrected for common Pb using nonradiogenic 204Pb, and mean ages for 206Pb/238U are quoted at a 95% confidence interval. Transparent euhedral zircon crystals from syenogranite (L-1-b5) and monzogranite (L-1-b6) were selected to perform U-Pb dating. Zircon grains range from 100 to 300 μm in size and show typical oscillatory zoning in CL images (Figure 5), indicative of a magmatic origin [62,63,64]. This is also supported by the high U (149–2521 ppm) and Th (148–4200 ppm) contents with Th/U ratios of 0.41–1.77 (greater than 0.1) in all analyzed spots. After homogenization, eighteen and sixteen reliable analytical spots were obtained from L-1-B5 and L-1-B6, respectively.

4.2. Zircon Hf Isotope Analysis

Zircon Lu–Hf isotope analysis was conducted at Nanjing Hongchuang Geological Exploration Technology Services Co., Ltd., using a combination of the US Applied Spectra Inc. (West Sacramento, CA, USA) J–100 femtosecond laser and Neptune MC–ICP–MS (Thermo Finnigan, Silicon Valley, CA, USA). The sizes of laser ablation spots were 20 μm × 40 μm with 8 Hz of frequency, an energy density of 1.5 J/cm2, and an ablation time of 31 s. Given the low 176Lu/177Hf ratio in zircons (usually <0.002), the interference of 176Lu to 176Hf isotopes can be neglected. The interference of 176Yb to 176Hf was corrected by the abundance of Yb and the measured 173Yb/172Yb values. Hf isotope analysis points were selected to overlap or be within the same zone as zircon U–Pb age analysis points, ensuring correspondence between the Hf isotope and zircon U–Pb age analysis. The Hf and Yb isotope ratios were standardized using 179Hf/177Hf = 0.7325 and 173Yb/172Yb = 1.35274. The measured 176Hf/177Hf ratio for GJ1 is 0.282008 ± 20, consistent with the recommended 176Hf/177Hf ratio of 0.282000 ± 5 reported by Morel et al. [65]. Analysis methods and data processing were followed by Wu and Yang [66].

4.3. Whole-Rock Major and Trace Element Analysis

Whole-rock major and trace element analysis was also conducted at Nanjing Hongchuang Geological Exploration Technology Services Co., Ltd. AxiosMAX XRF analyzer (Malvinpanaco, Almero, The Netherlands) was used to analyze the major elements, with the precision and accuracy meeting the “Chemical Analysis Methods for Silicate Rocks-Part 28: Determination of 16 Major and Trace Elements (GB/T14506.28–2010, National Standard of the People’s Republic of China)”. Trace elements were analyzed using an Agilent 7900 ICP–MS, and were scanned five times for precision, whereas the accuracy was ensured within a relative standard deviation (1RSD) of less than 5%.

4.4. TIMA Mineral Comprehensive Analysis

Mineral content and grain size were determined using a TESCAN integrated mineral analyzer TIMA (TESCAN Integrated Mineral Analyzer, Brno, Czech Republic), hosted at Nanjing Hongchuang Geological Exploration Technology Services Co., Ltd. The instrument is a high-resolution Schottky field emission scanning electron microscope (SEM) (model TESCAN MIRA3) equipped with four energy-dispersive spectrometry probes (EDAX Element 30, Berwyn, PA, USA) and computer graphics and data software processing technology designed to perform automatic quantitative mineralogical analyses. Prior to the experiment, thin section (target) samples were carbon-coated. Mineral analyses were carried out with a 25 kV and 9 nA electron beam at a 143 nm spot and a 15 mm analysis distance. The automatic calibration of current and BSE signal intensity were carried out using a platinum Faraday cup. The energy-dispersive spectrometer (EDS) signals were calibrated using a manganese standard. The test employed a disassociation mode, simultaneously obtaining BSE images and EDS data, with 1000 X-ray counts per point. The pixel size was 2.5 μm, and the energy spectrum step size was 7.5 μm.

5. Results

5.1. Zircon U–Pb Ages

Complete results of the U-Pb isotopic data for these zircons are listed in Table 1. The 18 analysis points of zircon yield 206Pb/238U ages of 49.2 ± 1.4 to 51.6 ± 1.2 Ma, with a weighted mean age of 50.5 ± 0.3 Ma (MSWD = 1.8, 2σ) for the syenogranite (Figure 4a). The 16 analysis points of zircon yield 206Pb/238U ages ranging from 49.8 ± 0.7 to 51.7 ± 0.7 Ma, with a weighted mean age of 50.7 ± 0.3 Ma (MSWD = 2.7, 2σ) for the monzogranite (Figure 4b). We interpret these zircon U-Pb ages as the crystallization time of the Yingpanshan–Damanbie granitoids.

5.2. Major and Trace Element Geochemistry

Major and trace element compositions of granitoids are presented in Table 2. In the SiO2–(Na2O + K2O) diagram (Figure 6a), samples are plotted in the field of granite and monzogranite, respectively. According to the abundance of K-feldspar (45–50 vol.%) and plagioclase (20–22 vol.%), the granite samples are classified as syenogranite.
Syenogranites are characterized by high SiO2 (70.28–73.96 wt.%), Al2O3 (12.74–13.88 wt.%) and K2O/Na2O (1.31–3.43) contents, and relatively low Na2O (1.79–3.3 wt.%) and P2O5 (0.06–0.25 wt.%) contents and Mg# (100 × [MgO/(Mg + FeOT)] = 13.48 to 21.46). They also have A/CNK (A/CNK = mol Al2O3/(CaO + Na2O + K2O)) ratios of 0.95 to 1.17 and high K2O contents of 4.33–6.61 wt.%, suggesting they are metaluminous to weakly peraluminous (Figure 6b–d). They show significant negative δEu values (0.32–0.65) and variably negative to positive δCe values (0.66–1.13). Notably, syenogranite samples are enriched in total REE contents of 210–599 ppm (average 376 ppm), with relatively high LREE/HREE ratios of 9.53–17.71 and (La/Yb)N values of 9.82–25.95, indicating a preferential enrichment of LREEs. This feature is also exhibited by the right-inclining chondrite-normalized REE patterns (Figure 7a). They exhibit relative depletion in high-field-strength elements (HFSEs, e.g., Nb, Ta, P) and Sr, Ti, and Ba on the primitive mantle-normalized trace element spider diagram (Figure 7b). The calculation results of zircon saturation thermometry completed by Watson and Harrison (1983) [67] display that syenogranites are crystallized at relatively high temperatures ranging from 866 °C to 918 °C.
Monzogranites have relatively lower SiO2 contents (64.41–69.34 wt.%) and Mg# (14.28–22.97), elevated Al2O3 (13.81–15.79 wt.%) and high K2O (5.15–7.10 wt.%) contents, with moderately low Na2O (1.90–3.78 wt.%) and P2O5 (0.06–0.14 wt.%) contents. They have A/CNK ratios of 0.91 to 1.15 and high K2O contents of 5.15–7.10 wt.%, also suggesting that they are metaluminous to weakly peraluminous (Figure 6b–d). They show significant negative δEu values (0.37–0.67) and slightly negative to slightly positive δCe values (0.94–1.04). Notably, monzogranite samples are enriched in total REE contents of 232–626 ppm (average 431 ppm), with relatively high LREE/HREE ratios of 12.50–17.96 and (La/Yb)N values of 16.62–25.90, indicating a preferential enrichment of LREEs. This feature is also indicated by the right-inclining chondrite-normalized REE patterns (Figure 7a). They exhibit relative depletion in high-field-strength elements (HFSEs, e.g., Nb, Ta, P) and Sr, Ti, and Ba on the primitive mantle-normalized trace element spider diagram (Figure 7b). The calculation results of zircon saturation thermometry completed by Watson and Harrison (1983) [67] display that monzogranites are also crystallized at relatively high temperatures ranging from 848 °C to 929 °C.

5.3. Zircon Lu–Hf Isotopes

In situ zircon Lu–Hf isotope analyses were carried out as close as possible to the spots for zircon U–Pb dating. The εHf(t) values of a syenogranite sample (L-1-b5) and a monzogranite sample (L-1-b6) were then calculated based on their U–Pb ages. The results of the initial 176Hf/177Hf values are listed in Table 3. The εHf(t) values and two-stage model ages (TDM2) were calculated using the average zircon U-Pb ages of the samples. The initial 176Hf/177Hf values of zircon grains from syenogranite range from 0.282462 to 0.282531, and the corresponding εHf(t) values are from −9.9 to −7.5. Furthermore, the calculated two-stage model ages (TDM2, according to Griffin et al. [70]) for the zircon grains are 1598–1752 Ma. The initial 176Hf/177Hf values of zircons from monzogranite range from 0.282473 to 0.282635, and the corresponding εHf(t) values are from −9.5 to −3.9. The two-stage model ages (TDM2) of the zircons range from 1369 to 1727 Ma.

6. Discussion

6.1. Petrogenesis and Tectonic Setting of the Yingpanshan–Damanbie Pluton

Granitoids related to the Yingpanshan–Damanbie iREE deposit have relatively low loss on ignition (LOI) values (0.43–1.98; Table 2), indicating that the influence of alteration on the original chemical composition is negligible. The La/Sm ratio can be used to distinguish the process of fractional crystallization and partial melting, due to its extreme insensitivity to partial melting [71]. A positive trend between the La/Sm ratio and the La concentration (Figure 8a) and a relatively constant range of Zr/Hf ratios (Figure 8b) show that partial melting has played an important role in the formation of monzogranites and syenogranites, without intensive fractional crystallization in the magmatic evolution. We therefore suggest that they might have been directly derived from the partial melting of their source regime, which can be reflected by the major- and trace-element data of these granites. All samples are plotted in the field of A-type granites on the diagrams of FeOT/MgO vs. Zr + Nb + Ce + Yb (Figure 8c) and Zr vs. 10,000 Ga/Al (Figure 8d). The classification is also supported by the geochemical characteristic of A-type granites with enrichments in Th, U, Zr, Hf, Rb, and K, and depletions in Sr, Ba, P, and Ti [72]. They are further divided into A2 chemical subgroups in the Yb/Ta–Y/Nb and Nb–Y–Ce diagrams (Figure 8e–f, after Eby [73]). This result is also evidenced by the relatively low Nb/Y ratios (0.41–0.95, mostly smaller than 0.83, after Eby [73]) of these granites. A2-type granites are considered to be formed at convergent plate margins in an extensional environment related to a collision orogeny or a back-arc, and are similar to continental crust or island arc granite [73]. Fluids released from the subduction zone can also lead to the arc signature of A2-type granites [50,74,75]. Three models are proposed to interpret the petrogenesis of A-type granite: the (1) fractional crystallization of mantle-derived alkaline basalt [76]; the (2) partial melting of specific protoliths in the continental crust [77,78]; and the (3) mixing between anatectic magma and mantle-derived mafic magma [78,79]. Several lines of evidence, including a positive trend between the La/Sm ratio and the La concentration (Figure 8a) and relatively constant Zr/Hf ratios (Figure 8b), exclude the genesis form fractional crystallization of mantle-derived alkaline basalt. No mafic microgranular enclaves (MMEs) have been discovered in these rocks, which also rules out the mixing between anatectic magma and mantle-derived mafic magma. Monzogranites and syenogranites are enriched in large ion lithophile elements (LILEs, e.g., K and Rb), and depleted in some HFSEs (Nb, Ta), and Ti, Ba, Sr, and P, suggesting crust-derived sources. Negative εHf(t) values (ranging from −9.9 to −3.9), with T2DM ranging from 0.94 to 1.11 Ga, are higher than those of contemporaneous Xiaolonghe A–type granites (εNd(T) = −12.5 to −10.7; Figure 9) in the Tengchong block [51], and are plotted in the same area of coeval mafic rocks and granites in Tongbiguan (Figure 9a), suggesting that they have the same source region and further implying a predominantly Paleoproterozoic crustal source composed of amphibolite under low pressure (Figure 9).
According to plots of Al2O3/(Fe2O3T + MgO + TiO2) vs. Al2O3 + Fe2O3T + MgO + TiO2 (Figure 9b), (Na2O + K2O)/(FeOT + MgO + TiO2) vs. Na2O + K2O + FeOT + MgO + TiO2 (Figure 9c), and Mg# vs. SiO2 (Figure 9d), both the monzogranites and syenogranites show similar geochemical characteristics as amphibolite-derived melts at low pressures and/or crustal-derived melts at high temperatures, which is also supported by the relatively high zirconium saturation temperatures (TZr = 848–915 °C, following the calculation by Watson and Harrison, 1983 [69]). Hence, we suggested that the melts for both the syenogranites and monzogranites may have been formed by the partial melting of amphibolites at a relatively high temperature. This result is consistent with the occurrence of I and A-type granites formed in high-temperature and low-pressure conditions [40]. K-rich mafic rocks of coeval stages including gabbro, metagabbro, amphibolite, enclave, MMEs, and ultra-potassic rocks [43,80,81] in the western Tengchong block have been recognized and considered to be derived from a mid-ocean ridge basalt (MORB)-like subcontinental lithospheric mantle [42,43,80,81]. Collectively, these Eocene rocks [14,15,18,32,40,42,43,51,80,82] recorded a slab breakoff event in the early Eocene era [12]. During this event, asthenospheric melts upwelled into the lithosphere through a slab window and supplied the amount of heat to facilitate the decompression melting of the lithospheric mantle and lower crust, leading to the generation of high-K mafic and felsic magmas. Thus, we support that slab breakoff is a plausible model accounting for the Eocene magmatism in the Tengchong block [15]. Lastly, we propose that the A-type granites associated with the Yingpanshan–Damanbie iREE deposit in this study were formed by the partial melting of amphibolites at a post-collisional extension setting after the Tethys ocean had been closed.
Minerals 14 00933 g008aMinerals 14 00933 g008b
Figure 8. Plots of (a) La/Sm versus La, (b) Zr/Hf versus SiO2, (c) FeOT/MgO versus (Zr + Y + Nb + Ce), (d) Zr versus 10,000 Ga/Al) [83], (e) Nb-Y-3Ga [73]; and (f) Nb-Y-Ce [73] for monzogranite and syenogranite from the Yingpanshan–Damanbie iREE deposit. A = A-type granite; A1 = A1-type granite; A2 = A2-type granite; I = I-type granite; S = S-type granite; FG = Fractionated felsic granite; OGT = Unfractionated M-, I- and S-type granite.
Figure 8. Plots of (a) La/Sm versus La, (b) Zr/Hf versus SiO2, (c) FeOT/MgO versus (Zr + Y + Nb + Ce), (d) Zr versus 10,000 Ga/Al) [83], (e) Nb-Y-3Ga [73]; and (f) Nb-Y-Ce [73] for monzogranite and syenogranite from the Yingpanshan–Damanbie iREE deposit. A = A-type granite; A1 = A1-type granite; A2 = A2-type granite; I = I-type granite; S = S-type granite; FG = Fractionated felsic granite; OGT = Unfractionated M-, I- and S-type granite.
Minerals 14 00933 g008aMinerals 14 00933 g008b
Minerals 14 00933 g009
Figure 9. Plots of (a) Al2O3/(Fe2O3T + MgO + TiO2) versus (Al2O3 + Fe2O3T + MgO + TiO2) (after Patiňo Douce. (1999) [84]); (b) (Na2O + K2O) versus (FeOT + MgO + TiO2); (c) Mg# versus SiO2; and (d) εHf(t) versus U–Pb ages for monzogranite and syenogranite from the Yingpanshan–Damanbie iREE deposit. (b) Compositional fields of experimental melts are from Patiño Douce [84], Sylvester [85], Patiño Douce [84], and Altherr et al. [86], respectively; (c) fields shown are as follows: pure crustal partial melts obtained in experimental studies by the dehydration melting of low-K basaltic rocks at 8–16 kbar and 1000–1050 °C [87]; pure crustal melts obtained in experimental studies by the moderately hydrous (1.7–2.3 wt.% H2O) melting of medium- to high-K basaltic rocks at 7 kbar and 825–950 °C [88]; mantle melts (basalts) and Quaternary volcanic rocks from the Andean southern volcanic zone [89]; melts from meta-igneous sources under crustal pressure and temperature conditions of 0.5–1.5 GPa and 800–1000 °C, respectively, which are based on the work completed by Wolf and Wyllie [90]; (d) data for the Gangdese belt from Ji et al. [91]; data for the southern Lhasa block from Jiang et al. [92], Ji et al. [93], Hou et al. [94], Zheng et al. [95], Zhu et al. [96], and Huang et al. [97]; data for the central Lhasa block from Hou et al. [94], Gao et al. [98], Zheng et al. [99], and Wang et al. [100]; data for the eastern Himalayan syntaxis from Chui et al. [101], Gou et al. [102], and Pan et al. [103]; and data for the Tengchong block including the Guyong area from Xu et al. [18], Xie et al. [42], Chen et al. [51], and Qi et al. [104].
Figure 9. Plots of (a) Al2O3/(Fe2O3T + MgO + TiO2) versus (Al2O3 + Fe2O3T + MgO + TiO2) (after Patiňo Douce. (1999) [84]); (b) (Na2O + K2O) versus (FeOT + MgO + TiO2); (c) Mg# versus SiO2; and (d) εHf(t) versus U–Pb ages for monzogranite and syenogranite from the Yingpanshan–Damanbie iREE deposit. (b) Compositional fields of experimental melts are from Patiño Douce [84], Sylvester [85], Patiño Douce [84], and Altherr et al. [86], respectively; (c) fields shown are as follows: pure crustal partial melts obtained in experimental studies by the dehydration melting of low-K basaltic rocks at 8–16 kbar and 1000–1050 °C [87]; pure crustal melts obtained in experimental studies by the moderately hydrous (1.7–2.3 wt.% H2O) melting of medium- to high-K basaltic rocks at 7 kbar and 825–950 °C [88]; mantle melts (basalts) and Quaternary volcanic rocks from the Andean southern volcanic zone [89]; melts from meta-igneous sources under crustal pressure and temperature conditions of 0.5–1.5 GPa and 800–1000 °C, respectively, which are based on the work completed by Wolf and Wyllie [90]; (d) data for the Gangdese belt from Ji et al. [91]; data for the southern Lhasa block from Jiang et al. [92], Ji et al. [93], Hou et al. [94], Zheng et al. [95], Zhu et al. [96], and Huang et al. [97]; data for the central Lhasa block from Hou et al. [94], Gao et al. [98], Zheng et al. [99], and Wang et al. [100]; data for the eastern Himalayan syntaxis from Chui et al. [101], Gou et al. [102], and Pan et al. [103]; and data for the Tengchong block including the Guyong area from Xu et al. [18], Xie et al. [42], Chen et al. [51], and Qi et al. [104].
Minerals 14 00933 g009

6.2. The Relationship between the Initial REE Enrichment in Yingpanshan–Damanbie Granites and iREE Mineralization

Most iREE deposits in the Tengchong block are discovered in the regolith derived from Cretaceous to Paleogene granites, with a few formed from Triassic granites and Quaternary volcanic rocks [55]. Parent rocks of these iREE deposits are mostly A-type granites generated in an extensional setting and usually display relatively high REE contents (>200 ppm [22,53,55,58,59,105]) greater than the threshold for iREE mineralization (~150 ppm, Huang, 2021). The REE content in the protolith could directly affect the REE concentration in the regolith and, simply, the higher the REE content in the parent rock is, the more favorable it is for iREE mineralization under the same weathering conditions [106]. The REE concentrations (210–626 ppm) and patterns of Yingpanshan–Damanbie granite are similar to other bedrocks for the LREE-type deposits in Southern China [7,13,81,105,106], suggesting that these granites could also be potential source rocks for iREE mineralization. As the REE-bearing minerals in protolith are the main sources of REE cations in the weathering crust, mineral association greatly determines the concentration and fractionation characteristics of REEs. Under physical/chemical weathering and microbial action, the dissolution of rock-forming minerals, REE-bearing minerals, and REE minerals results in the activation and re-enrichment of REEs. The weathering of the protolith produces secondary minerals such as clay minerals and Fe-Mn oxides with a large specific surface area and high surface charge density to adsorb REE cations via ion exchange and surface adsorption/complexation [107,108]. Mineral types control the adsorption mechanism, enrichment-fractionation characteristics and the occurrence state of REEs [107]. According to the mineral assemblages of the granite in this study, most REE-bearing minerals (e.g., apatite, titanite, allanite, and fluorite) and rock-forming minerals (e.g., potassium feldspar, plagioclase, and biotite) are susceptible to weathering [109] and would steadily release the REEs they host during weathering [12,110]. Thus, these REE-bearing minerals and rock-forming minerals in A-type granite are altered into clay minerals (e.g., kaolinite, halloysite and illite) and iron–manganese oxides adsorbing more than 80% of REEs in the supergene environment [46,111]. An earlier study suggested high REE contents in parent rocks, hydrothermal alteration, climate, topography, and groundwater have controlled the formation of iREE deposits in western Yunnan [22,111]. In this paper, we focus on the parent rocks and their contribution to iREE mineralization. Thus, we propose that high REE contents, REE-bearing and rock-forming minerals in parent rocks could lead to the REE mineralization in the intense weathering of regoliths. Further studies on weathering regoliths are necessary to ascertain other control factors for the formation of iREE mineralization.

7. Conclusions

(1)
Granites associated with the Yingpanshan–Damanbie iREE deposit in the Tengchong block are A2-type granites derived from the partial melting of a lithohpheric amphibolite source at a post-collisional extension setting.
(2)
The high content of REEs in the parent rock was critical for the formation of the Yingpanshan–Damanbie iREE deposit in the Tengchong block.
(3)
REE-bearing minerals (e.g., apatite, titanite, allanite, and fluorite) and rock-forming minerals (e.g., potassium feldspar, plagioclase, and biotite) supply rare earth elements in the weathering regolith.

Author Contributions

Conceptualization, X.H.; formal analysis, X.H. and W.Y.; resources, Z.T.; writing—original draft, Z.T., X.H., T.M. and R.L.; supervision, H.W.; project administration, Z.P.; funding acquisition, H.W. and W.Y. All authors have read and agreed to the published version of the manuscript.

Funding

This study was supported by the National Natural Science Foundation of China (Grant No. 42162011), a new round of prospecting action research projects of the Yunnan Geological Exploration Fund Management Center (SI[2024]KY002), and the Xingdian Scholar Fund of Yunnan (C6213001155).

Data Availability Statement

The data presented in this study are available in this article.

Conflicts of Interest

The authors declare no conflicts of interest.

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Figure 1. (a) Tectonic map of the eastern Tethys domain (modified after Wang et al. [47]); (b) Geological map of the Tengchong block with iREE deposits (modified after Deng et al. [48]); (c) U–Pb ages histogram of zircons from magmatic rocks in the Tengchong block (date from He et al. [15], Dong et al. [16], Xu et al. [18], Yang et al. [19], Li et al. [26], Zou et al. [30], Cong et al. [35], Cao et al. [39], Xie et al. [42], Chen et al. [44], Cong et al. [49], Li et al. [50], Chen et al. [51], Zhu et al. [52]).
Figure 1. (a) Tectonic map of the eastern Tethys domain (modified after Wang et al. [47]); (b) Geological map of the Tengchong block with iREE deposits (modified after Deng et al. [48]); (c) U–Pb ages histogram of zircons from magmatic rocks in the Tengchong block (date from He et al. [15], Dong et al. [16], Xu et al. [18], Yang et al. [19], Li et al. [26], Zou et al. [30], Cong et al. [35], Cao et al. [39], Xie et al. [42], Chen et al. [44], Cong et al. [49], Li et al. [50], Chen et al. [51], Zhu et al. [52]).
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Figure 2. (a) Geological map of the Yingpanshan–Damanbie pluton with the Yingpanshan–Damanbie iREE deposit. (b) A profile of the regolith with iREE mineralization from the Yingpanshan–Damanbie iREE deposit.
Figure 2. (a) Geological map of the Yingpanshan–Damanbie pluton with the Yingpanshan–Damanbie iREE deposit. (b) A profile of the regolith with iREE mineralization from the Yingpanshan–Damanbie iREE deposit.
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Figure 3. Characteristics of petrography and REE-bearing accessory minerals of syenogranite from the Yingpanshan–Damanbie iREE deposit in western Yunnan. (a) Photograph of a sample specimen; (b) photomicrograph; and (c) TIMA images of thin section; abbreviations: Kfs = K–feldspar, Qtz = quartz, Pl = plagioclase, Bt = biotite, Ep = Epidote.
Figure 3. Characteristics of petrography and REE-bearing accessory minerals of syenogranite from the Yingpanshan–Damanbie iREE deposit in western Yunnan. (a) Photograph of a sample specimen; (b) photomicrograph; and (c) TIMA images of thin section; abbreviations: Kfs = K–feldspar, Qtz = quartz, Pl = plagioclase, Bt = biotite, Ep = Epidote.
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Figure 4. Characteristics of petrography and REE accessory minerals of monzogranite from the Yingpanshan–Damanbie iREE deposit in western Yunnan. (a) Photograph of a sample specimen; (b) photomicrograph; and (c) TIMA images of representative thin sections; abbreviations: Kfs = K–feldspar, Qtz = quartz, Pl = plagioclase, Bt = biotite, Ep = Epidote, Hb = hornblende.
Figure 4. Characteristics of petrography and REE accessory minerals of monzogranite from the Yingpanshan–Damanbie iREE deposit in western Yunnan. (a) Photograph of a sample specimen; (b) photomicrograph; and (c) TIMA images of representative thin sections; abbreviations: Kfs = K–feldspar, Qtz = quartz, Pl = plagioclase, Bt = biotite, Ep = Epidote, Hb = hornblende.
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Figure 5. U–Pb concordia diagrams for (a) monzogranite (L–1–B6) and (b) syenogranite (L–1–B5) from the Yingpanshan–Damanbie iREE deposit and CL images of representative zircon grains.
Figure 5. U–Pb concordia diagrams for (a) monzogranite (L–1–B6) and (b) syenogranite (L–1–B5) from the Yingpanshan–Damanbie iREE deposit and CL images of representative zircon grains.
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Figure 6. Plots of (a) (K2O + Na2O) versus SiO2, (b) A/NK versus A/CNK, (c) K2O versus SiO2, (d) K2O/Na2O versus SiO2 of monzogranite and syenogranite from the Yingpanshan–Damanbie iREE deposit.
Figure 6. Plots of (a) (K2O + Na2O) versus SiO2, (b) A/NK versus A/CNK, (c) K2O versus SiO2, (d) K2O/Na2O versus SiO2 of monzogranite and syenogranite from the Yingpanshan–Damanbie iREE deposit.
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Figure 7. Plots of chondrite-normalized REE patterns (a,c) and primitive mantle (PM)-normalized spider diagrams (b,d) for monzogranite and syenogranite from the Yingpanshan–Damanbie iREE deposit. Values for normalization are from Sun and McDonough [68], respectively. UCC = upper continental crust; LCC = lower continental crust; UCC and LCC data from Jahn et al. [69].
Figure 7. Plots of chondrite-normalized REE patterns (a,c) and primitive mantle (PM)-normalized spider diagrams (b,d) for monzogranite and syenogranite from the Yingpanshan–Damanbie iREE deposit. Values for normalization are from Sun and McDonough [68], respectively. UCC = upper continental crust; LCC = lower continental crust; UCC and LCC data from Jahn et al. [69].
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Table 1. LA–ICP–MS zircon U–Pb isotopic compositions and ages of the syenogranite and monzogranite from the Yingpanshan–Damanbie iREE deposit in the Tengchong block.
Table 1. LA–ICP–MS zircon U–Pb isotopic compositions and ages of the syenogranite and monzogranite from the Yingpanshan–Damanbie iREE deposit in the Tengchong block.
Spot No.PbThUTh/UIsotope RatioAge (Ma)Concordance
ppmppmppm207Pb/206Pb2σ207Pb/235U2σ206Pb/238U2σ206Pb/238U2σ207Pb/235U2σ%
Syenogranite (L–1–b5)
Lb5–12.62402790.860.04990.00610.05230.00630.007780.0002149.91.451.36.197
Lb5–214.5122815140.810.04710.00230.05040.00220.007980.0001151.20.749.92.197
Lb5–34.86654211.580.04970.00390.05140.00390.007660.0001749.21.150.63.797
Lb5–42.12222111.050.04450.00560.04530.00540.007660.0002149.21.344.55.290
Lb5–55.85255940.880.04940.00410.05240.00440.00790.0001750.71.151.74.298
Lb5–61.51481490.990.05260.00760.05360.00770.007740.0002749.71.752.47.395
Lb5–75.23165880.540.04960.00410.05160.00410.007830.0001650.31.050.93.999
Lb5–83.54583151.450.04970.00640.05310.00680.007810.000250.21.252.06.596
Lb5–92.72432780.870.04410.00450.04730.00510.007860.0002150.51.346.64.992
Lb5–1020.997323490.410.04790.00190.05150.00180.007950.000151.10.751.11.8100
Lb5–115.23865460.710.05110.00390.05340.00380.007830.0001750.31.152.63.696
Lb5–121.71801681.070.04920.00640.05020.00630.007660.0002249.21.449.06.1100
Lb5–135.54495670.790.04960.00350.05230.00340.007760.0001449.80.952.03.496
Lb5–1414.995015880.60.04760.00220.05260.00230.00780.0001250.10.752.02.296
Lb5–154.73864770.810.04720.0040.05360.00440.008040.0001951.61.252.84.298
Lb5–165.93726360.590.04650.00360.05170.00380.007950.00015511.051.03.7100
Lb5–173.43573361.060.0490.00540.05390.00580.007950.0002511.352.95.696
Lb5–184.53844590.840.04760.00360.05330.00380.00790.0001650.71.052.53.797
Monzogranite (L–1–b6)
Lb6–120.6271017231.570.04720.0020.0540.00210.008060.0001151.70.753.42.097
Lb6–229.7420025211.670.04860.0020.05440.00210.008030.0001151.50.753.82.096
Lb6–310.212039301.290.04850.00320.05440.00370.007880.0001550.61.053.63.594
Lb6–422.6317218541.710.04810.00240.05410.00250.008040.0001251.60.853.52.496
Lb6–52.11911970.970.04990.00740.05650.00810.008040.0002851.61.855.17.793
Lb6–613155211921.30.05430.00310.05930.00310.007910.0001250.80.858.43.086
Lb6–722.8327020061.630.04680.00260.0490.00260.00780.0001350.10.848.52.597
Lb6–825.3354721381.660.04860.00190.05230.00190.007930.0001150.90.751.71.898
Lb6–97.69107061.290.04950.00450.0540.00510.007980.0001551.21.053.14.896
Lb6–108.210777131.510.0460.00370.04950.0040.007990.0001651.31.048.93.995
Lb6–1118.1270915321.770.04940.00230.05250.00240.007760.0001149.80.751.82.396
Lb6–128.36168690.710.05220.00330.05510.00340.00790.0001450.70.954.33.293
Lb6–1324336221641.550.04740.00220.04940.00230.007770.0001249.90.848.92.298
Lb6–1418.8239017131.40.04980.00240.05280.00240.00780.0001250.10.752.22.396
Lb6–156.94777660.620.0490.00310.05150.00320.007770.0001549.91.050.93.198
Lb6–161278413200.590.04920.0030.05310.00290.007750.0001249.80.852.42.895
Table 2. Major and trace element compositions of syenogranite and monzogranite from the Yingpanshan–Damanbie iREE deposit in the Tengchong block.
Table 2. Major and trace element compositions of syenogranite and monzogranite from the Yingpanshan–Damanbie iREE deposit in the Tengchong block.
LithologyMonzograniteSyenogranite
Sample No.D–2–b1D–2–b2L–1–b2L–1–b3L–1–b6L–1–b7N–1–b3N–2–b1N–2–b2N–2–b3N–2–b4D–2–b3D–2–b4L–1–b1L–1–b4L–1–b5L–1–b8L–2–b09L–2–b10N–1–b2N–1–b4N–1–b5N–2–b6
Major element oxides (wt.%)
SiO269.3468.7165.0964.4165.4565.3867.2568.7468.3768.6268.3973.4372.0172.9071.2973.9672.2272.5870.9070.9070.7870.2870.31
TiO20.370.320.670.650.680.660.550.500.530.460.360.440.380.490.450.490.300.350.310.470.410.310.43
Al2O314.4414.6715.0715.5915.2615.7914.5813.9013.8113.9514.2212.7913.6612.7413.4412.8013.5113.5913.7913.2813.2413.8813.38
Fe2O32.742.504.724.694.814.754.063.603.923.432.772.832.612.963.352.972.382.702.513.353.172.413.34
FeO1.802.013.743.704.021.372.872.412.592.481.761.871.581.942.872.441.372.051.982.301.801.902.37
MnO0.090.090.090.100.110.120.090.060.060.060.050.080.080.070.080.080.060.080.060.080.050.040.06
MgO0.450.401.080.931.120.940.970.871.000.950.700.680.530.690.790.690.330.590.370.810.680.590.79
CaO1.451.172.942.373.012.401.941.252.352.381.361.631.511.231.031.241.471.911.591.381.351.681.02
Na2O2.892.983.333.763.383.782.691.902.802.762.202.432.692.451.802.452.983.313.102.062.482.691.79
K2O6.737.105.225.795.325.856.376.185.155.576.805.686.484.876.154.876.144.336.026.106.026.616.14
P2O50.090.060.240.220.250.220.170.150.180.150.120.140.120.080.110.080.060.120.060.140.130.100.10
LOI0.670.860.650.300.720.441.021.930.780.771.470.710.641.070.570.560.580.470.431.580.980.581.98
Total99.2698.8699.0998.80100.11100.3399.6799.0898.9599.1198.44100.85100.7199.5599.05100.18100.02100.0399.14100.1399.2999.1799.34
K2O + Na2O9.6210.088.559.558.79.639.068.087.958.3398.119.177.327.957.329.127.649.128.168.59.37.93
K2O/Na2O2.332.391.571.541.571.552.373.261.842.023.092.332.411.993.421.992.061.311.942.962.432.453.44
A/NK1.201.171.361.251.351.261.291.421.361.321.301.261.191.371.401.381.171.341.191.331.251.201.40
A/CNK0.981.000.920.930.910.930.981.150.960.941.060.980.961.111.171.110.951.000.951.061.020.951.17
Mg#15.6814.2819.3817.2419.2822.9720.8621.6222.5823.2522.7821.4619.4220.9819.2819.2714.4819.0813.4821.3020.7920.5120.66
Trace elements (ppm)
Li31.735.331.929.422.433.245.942.536.332.629.721.428.727.824.939.531.977.230.838.133.231.140.2
Be4.584.574.185.614.325.284.574.214.424.253.522.873.842.905.014.644.725.934.823.993.904.073.57
B6.176.976.446.966.176.466.266.947.046.356.326.416.215.437.537.266.397.214.925.946.166.396.02
Sc4.072.947.004.5511.981.525.334.716.055.783.563.433.123.785.063.972.281.442.104.533.573.054.40
V16.113.046.429.8113.29.833.929.936.033.224.125.321.526.430.625.510.324.811.629.322.419.227.6
Cr3.022.522.462.261.722.066.687.086.646.065.372.671.533.962.104.851.781.522.426.656.113.746.18
Co1.781.345.864.1213.481.185.034.395.104.483.233.302.484.164.364.121.213.151.524.183.212.634.21
Ni0.930.671.260.941.770.581.951.931.981.811.411.300.702.100.832.060.600.850.632.611.551.422.07
Cu1.350.451.490.864.330.551.932.682.672.451.512.111.542.631.021.540.650.660.671.531.431.711.33
Zn22.716.253.844.276.218.846.639.647.737.925.531.123.938.648.746.716.843.224.240.434.326.938.1
Ga17.217.418.618.020.016.719.517.518.218.017.514.114.517.118.617.916.417.217.417.217.217.217.3
Rb223250153140128209251214202183223144195158162185209179201231224236266
Sr1251103273595061072001281981881681661671133731528416398147122190125
Y44.342.342.645.844.532.834.831.440.234.024.522.056.229.445.360.940.332.539.032.231.729.332.5
Zr383344397379304277405342332251230250213270382337289194381297238216304
Nb29.629.628.838.231.725.426.223.026.222.017.220.823.022.037.430.830.120.327.823.923.717.424.0
Sn5.5813.05.906.784.615.656.435.295.373.2911.97.284.984.467.596.565.7212.010.35.195.033.665.35
Cs6.756.737.769.034.206.148.517.076.775.406.684.354.273.609.897.965.5313.345.187.208.246.688.33
Ba6465661131128613543998347015686498534504344831374605363227285719564799783
La11010714115711784.599.910095.685.955.373.017174.813094.786.147.710699.098.263.479.6
Ce19219524428422316918518118015999.313921113222717518886.4184178174110136
Pr22.121.427.430.424.618.019.919.619.718.111.513.934.415.426.119.518.710.322.119.318.812.615.5
Nd76.373.093.0102.587.462.167.065.267.961.839.947.111852.388.667.266.036.975.264.261.042.851.2
Sm12.912.315.116.615.110.611.410.612.211.07.297.7220.38.7814.912.012.17.2212.510.69.867.438.79
Eu1.571.362.252.622.781.101.391.221.301.401.201.322.271.302.691.381.081.021.111.130.971.191.01
Gd9.859.2010.7711.6310.777.618.447.799.438.275.585.5614.786.5410.739.689.135.758.797.837.395.706.62
Tb1.421.411.481.591.481.091.211.101.371.200.820.792.140.961.471.421.390.901.281.121.060.850.99
Dy7.767.727.968.517.995.936.465.887.526.454.604.2211.255.477.888.277.615.116.966.045.814.705.48
Ho1.531.511.531.641.591.161.241.131.431.230.880.802.081.071.541.751.471.021.361.171.120.931.10
Er4.054.034.084.344.213.113.323.033.813.232.372.095.282.824.034.973.932.883.623.082.982.492.98
Tm0.5930.6040.6020.6490.6280.4740.4840.4460.5550.4640.3530.3020.7530.4140.6040.7590.5780.4680.5320.4540.4400.3650.447
Yb3.653.773.674.073.933.013.032.753.402.832.241.904.732.533.694.603.633.283.242.832.702.222.75
Lu0.5400.5320.5390.5980.5790.4410.4460.4090.4930.4050.3240.2890.6650.3610.5510.6980.5140.5010.4600.4090.3960.3320.412
Hf9.698.709.739.207.617.6810.508.978.716.666.176.805.676.608.988.928.165.7810.007.786.325.728.18
Ta1.932.521.492.091.682.081.711.691.701.461.201.271.471.412.002.092.252.451.911.791.681.371.92
W0.2670.3540.8250.4230.4940.2221.0070.2900.2670.9310.4600.1890.2870.3780.5080.4330.2410.2460.1790.3720.6680.7811.906
Tl1.351.491.241.241.031.311.651.531.401.291.390.821.111.031.371.291.401.501.271.521.461.471.82
Pb29.3231.7429.3124.8927.7828.3134.1031.6830.0128.7835.5123.8529.0028.4034.1629.2226.0237.1827.8934.0730.7437.1131.87
Bi0.1710.1580.1670.1260.1310.2200.0850.1210.1090.0630.1040.1130.2250.2500.4550.1210.1340.2400.1550.0740.0870.0710.067
Th43.1435.4252.5753.6035.0756.9159.1442.7155.2643.7041.9525.1043.8422.8636.5738.9542.0727.3245.6246.6469.3436.0449.56
U3.803.414.214.385.055.735.433.936.105.014.953.264.703.683.503.993.532.838.303.967.283.075.03
ΣREE444439553626501368409400405361232298599304521402401210427395384255313
LREE414410523593470346384377377337215283557284490370372190401372362237292
HREE29.428.830.633.031.222.824.622.528.024.117.216.041.720.230.532.228.319.926.222.921.917.620.8
LREE/HREE14.114.317.118.015.115.215.616.813.514.012.517.713.414.116.111.513.29.515.316.216.613.514.1
(La/Yb)N20.319.225.926.120.218.922.224.619.020.516.626.024.419.923.813.916.09.822.123.624.519.219.5
δEu0.430.390.540.580.670.380.430.410.370.450.570.620.40.530.650.390.320.480.320.380.350.560.41
δCe0.940.980.940.991.001.041.000.981.000.970.951.050.660.930.940.981.130.940.910.980.970.940.93
(Gd/Yb)N2.181.972.372.312.212.042.252.292.242.362.012.372.522.092.351.702.031.422.192.232.212.071.94
TZr (°C)915904907903878871918915897866867873854890929914885848913895869854904
Rb/Sr1.782.280.470.390.251.961.261.671.020.971.330.871.171.400.431.222.501.102.041.571.841.252.13
Rb/Ba0.350.440.140.110.090.520.300.310.360.280.260.320.450.330.120.310.580.790.700.320.400.300.34
Notes: Mg# = 100 × molar MgO/(Mg + FeOT). FeOT = 0.9 × Fe2O3T; δEu = EuN/SQRT (SmN × GdN); δCe = CeN/SQRT (LaN × PrN); TZr is calculated from zircon saturation thermometry according to the word of Watson and Harrison, 1983 [67].
Table 3. Hf isotopic compositions of zircons from granitoids from the Yingpanshan–Damanbie iREE deposit in the Tengchong block.
Table 3. Hf isotopic compositions of zircons from granitoids from the Yingpanshan–Damanbie iREE deposit in the Tengchong block.
Spot No.Age176Hf/177Hf2σ176Yb/177Hf2σ176Lu/177Hf2σεHf(0)εHf(t)TDM1 (Ma)fLu/HfTDM2 (Ma)
Syenogranite (L-1-b5)
LB5–150.50.2824810.0000190.024680.000230.00094970.000009−10.3−9.21089−0.971710
LB5–250.50.2825100.0000190.03830.000320.0014710.000011−9.3−8.21063−0.961646
LB5–350.50.2824920.0000240.02580.000530.000970.000018−9.9−8.81074−0.971685
LB5–450.50.2824940.0000240.01690.000390.0006670.000014−9.8−8.71063−0.981680
LB5–550.50.2824620.000020.018520.000420.0007170.000015−11.0−9.91108−0.981752
LB5–650.50.2824840.0000230.017710.000170.00069430.0000069−10.2−9.11077−0.981702
LB5–750.50.2824800.0000160.0168730.0000650.00068940.0000018−10.3−9.21083−0.981711
LB5–850.50.2824780.0000250.02890.000720.001090.000025−10.4−9.31097−0.971717
LB5–950.50.2825020.0000220.0169050.0000870.00065520.0000027−9.5−8.51051−0.981662
LB5–1050.50.2825310.000020.026390.000440.0010280.000016−8.5−7.51021−0.971598
LB5–1150.50.2824880.0000220.019480.000710.0007550.000025−10.0−9.01073−0.981694
LB5–1250.50.2825030.0000180.018470.000270.0007180.00001−9.5−8.41051−0.981660
LB5–1350.50.2825290.0000240.019810.000340.0007780.000012−8.6−7.51017−0.981602
LB5–1450.50.2825020.0000180.033880.000870.0013450.000032−9.5−8.51070−0.961663
LB5–1550.50.2825100.0000190.017130.000630.0006720.000023−9.3−8.21040−0.981644
LB5–1650.50.2824920.0000190.018710.00050.0007270.000019−9.9−8.81067−0.981685
LB5–1750.50.2825160.0000210.036230.000530.0013480.000018−9.1−8.01051−0.961632
LB5–1850.50.2824900.0000220.017810.000620.0006980.000022−10.0−8.91069−0.981689
Monzogranite (L-1-b6)
LB6–150.70.2825830.0000270.07940.0010.0029860.000037−6.7−5.7999−0.911485
LB6–250.70.2825840.0000270.08440.00190.0031880.000077−6.6−5.61004−0.901483
LB6–350.70.2825530.0000240.059470.000490.0022350.000018−7.7−6.71022−0.931550
LB6–450.70.2826350.0000360.09210.00130.003520.000046−4.8−3.9936−0.891369
LB6–550.70.2824840.0000210.018440.000120.00071820.0000044−10.2−9.11078−0.981702
LB6–650.70.2825550.0000250.059850.000720.0022920.000025−7.7−6.61021−0.931546
LB6–750.70.2826080.0000250.06510.00110.0024530.000036−5.8−4.8948−0.931427
LB6–850.70.2825930.0000270.054290.000490.0020650.000015−6.3−5.3960−0.941460
LB6–950.70.2825120.0000220.03930.00250.0014960.000091−9.2−8.11061−0.951641
LB6–1050.70.2825440.0000240.051790.000730.0019550.000024−8.1−7.01028−0.941570
LB6–1150.70.2824730.0000230.0125870.0000410.00049950.000001−10.6−9.51087−0.981727
LB6–1250.70.2825280.0000230.022170.000110.00086080.0000036−8.6−7.51020−0.971604
LB6–1350.70.2825310.0000230.020240.00020.00080490.000007−8.5−7.41015−0.981597
LB6–1450.70.2825800.0000280.11170.00210.0041720.000083−6.8−5.81038−0.871494
LB6–1550.70.2825750.0000210.054730.000650.0020610.000023−7.0−5.9986−0.941501
LB6–1650.70.2825400.0000220.018010.000220.00070610.0000092−8.2−7.11000−0.981577
LB6–1750.70.2825820.0000260.10760.00140.0040240.000056−6.7−5.71031−0.881489
LB6–1850.70.2825840.0000210.047360.000650.0017910.000025−6.6−5.6966−0.951480
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Tang, Z.; Pan, Z.; Ming, T.; Li, R.; He, X.; Wen, H.; Yu, W. Petrogenesis of Eocene A-Type Granite Associated with the Yingpanshan–Damanbie Regolith-Hosted Ion-Adsorption Rare Earth Element Deposit in the Tengchong Block, Southwest China. Minerals 2024, 14, 933. https://doi.org/10.3390/min14090933

AMA Style

Tang Z, Pan Z, Ming T, Li R, He X, Wen H, Yu W. Petrogenesis of Eocene A-Type Granite Associated with the Yingpanshan–Damanbie Regolith-Hosted Ion-Adsorption Rare Earth Element Deposit in the Tengchong Block, Southwest China. Minerals. 2024; 14(9):933. https://doi.org/10.3390/min14090933

Chicago/Turabian Style

Tang, Zhong, Zewei Pan, Tianxue Ming, Rong Li, Xiaohu He, Hanjie Wen, and Wenxiu Yu. 2024. "Petrogenesis of Eocene A-Type Granite Associated with the Yingpanshan–Damanbie Regolith-Hosted Ion-Adsorption Rare Earth Element Deposit in the Tengchong Block, Southwest China" Minerals 14, no. 9: 933. https://doi.org/10.3390/min14090933

APA Style

Tang, Z., Pan, Z., Ming, T., Li, R., He, X., Wen, H., & Yu, W. (2024). Petrogenesis of Eocene A-Type Granite Associated with the Yingpanshan–Damanbie Regolith-Hosted Ion-Adsorption Rare Earth Element Deposit in the Tengchong Block, Southwest China. Minerals, 14(9), 933. https://doi.org/10.3390/min14090933

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