Petrogenesis of the Lijiagou spodumene pegmatites in Songpan-Garze Fold Belt, West Sichuan, China: Evidence from geochemistry, zircon, cassiterite and coltan U-Pb geochronology and Hf isotopic compositions

Fei, Guangchun; Menuge, Julian F.; Li, Yunqiang; Yang, Jingyi; Deng, Yun; Chen, Changsheng; Yufan, Yang; Yang, Zheng; Liye, Qin; Luo, Zheng; Tang, Wenchun

doi:10.1016/j.lithos.2020.105555

Cited by 36 publications

(18 citation statements)

References 59 publications

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“…Fractionation of the accessory minerals (i.e., apatite and monazite) in parental granite can cause the depletion of LREE in the residual magma, and fractionation of garnet result in the depletion HREE. As for the lack of an Eu anomaly, this phenomenon can be also observed in some other rare metal-bearing pegmatites [8,78,79]. Previous study pointed out that oxidation of Eu 2+ to Eu 3+ can make it less compatible in the Ca sites of plagioclase [80][81][82].…”

Section: Relationship Between the Pegmatites And Granitesmentioning

confidence: 84%

Geochemical Contrasts between Late Triassic Rb-Rich and Barren Pegmatites from Ningshan Pegmatite District, South Qinling Orogen, China: Implications for Petrogenesis and Rare Metal Exploration

et al. 2020

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The Ningshan pegmatite district in the South Qinling Orogen hosts numerous Rb-(Be) mineralized pegmatites. In this study, whole-rock geochemistry, mineral geochemistry, and zircon U–Pb isotopes of the Rb-rich and barren pegmatites were determined. The barren pegmatites consist mainly of muscovite, microcline, albite, quartz, and garnet, whereas the Rb-rich pegmatites are mainly composed of muscovite, albite, quartz, and beryl, with minor chrysoberyl, cassiterite and columbite-group mineral. The muscovite and albite are the main Rb-bearing minerals. The U–Pb zircon dating of the Rb-rich and barren pegmatites yielding an age of 212–203 Ma, which is similar to that of the neighboring two-mica monzogranites distributed in the Ningshan area. Compared with the two-mica monzogranites, geochemical features, such as the Zr/Hf, Rb/Sr and Nb/Ta ratios and trace element contents indicated that the Rb-rich and barren pegmatites derived from fractionation of the two-mica monzogranites. In combination, the current and previous results suggest that the fractionation of the two-mica monzogranites caused the generation of the affinitive residual melts that, finally, crystallized to form the pegmatites. Compared to those from the barren pegmatites, the apatite from the Rb-rich pegmatites have higher MnO (14.51–19.12 wt.%) and Cl (0.12–0.16 wt.%) contents and lower F/Cl rartios (20–29). We conclude that these differences reflect unique geochemical signatures, and the geochemical composition of the apatite can be used as exploration guidance for rare metal-rich pegmatites.

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Section: Relationship Between the Pegmatites And Granitesmentioning

confidence: 84%

Geochemical Contrasts between Late Triassic Rb-Rich and Barren Pegmatites from Ningshan Pegmatite District, South Qinling Orogen, China: Implications for Petrogenesis and Rare Metal Exploration

et al. 2020

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“…38 in Fig. 1), and 0.51 Mt in the Keéryin ore field (Wang et al, 2005(Wang et al, , 2016Fu et al, 2017;Li et al, 2019;Fei et al, 2020). Another significant discovery in the KSGOB is the Bailongshan-Dahongliutan pegmatite-type rare metal deposits in the West Kunlun orogenic belt, Xinjiang (Yan et al, 2018;Wang et al, 2020), where 14 rare metal deposits along the 600-kmlong belt have been discovered, including the Huoshikashi, Kalawala, Xiaoerbulong, Dabudaer, Sansu, Tatulugou, Kangxiwa, Zhongfulugou, No.…”

Section: Spatial-temporal Distribution Of Rare Metal Mineral Depositsmentioning

confidence: 97%

“…A series of more than 110 rare metal granitic pegmatite dykes are derived around the internal and external contact zones of the granite, forming a super-large Li-and large-scale Be-deposits, as well as significant amounts of Nb, Ta and Rb Fu et al, 2017). In the Lijiagou deposit, the pegmatite dykes also surround a granite pluton, and with increasing distance include microcline (0-800 m), microcline-albite (800-1500 m), albite-(1500-2300 m), albite-spodumene (2300-5000 m), and lepidolite pegmatites (Fei et al, 2020).…”

Section: Pegmatite Typementioning

confidence: 99%

Spatial‐Temporal Distribution, Geological Characteristics and Ore‐Formation Controlling Factors of Major Types of Rare Metal Mineral Deposits in China

Jiang

Xiong

et al. 2020

Acta Geologica Sinica (Eng)

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Rare metals including Lithium (Li), Beryllium (Be), Rubidium (Rb), Cesium (Cs), Zirconium (Zr), Hafnium (Hf), Niobium (Nb), Tantalum (Ta), Tungsten (W) and Tin (Sn) are important critical mineral resources. In China, rare metal mineral deposits are spatially distributed mainly in the Altay and Southern Great Xingán Range regions in the Central Asian orogenic belt; in the Middle Qilian, South Qinling and East Qinling mountains regions in the Qilian–Qinling–Dabie orogenic belt; in the Western Sichuan and Bailongshan–Dahongliutan regions in the Kunlun–Songpan–Garze orogenic belt, and in the Northeastern Jiangxi, Northwestern Jiangxi, and Southern Hunan regions in South China. Major ore‐forming epochs include Indosinian (mostly 200–240 Ma, in particular in western China) and the Yanshanian (mostly 120–160 Ma, in particular in South China). In addition, Bayan Obo, Inner Mongolia, northeastern China, with a complex formation history, hosts the largest REE and Nb deposits in China. There are six major rare metal mineral deposit types in China: Highly fractionated granite; Pegmatite; Alkaline granite; Carbonatite and alkaline rock; Volcanic; and Hydrothermal types. Two further types, namely the Leptynite type and Breccia pipe type, have recently been discovered in China, and are represented by the Yushishan Nb–Ta– (Zr–Hf–REE) and the Weilasituo Li–Rb–Sn–W–Zn–Pb deposits. Several most important controlling factors for rare metal mineral deposits are discussed, including geochemical behaviors and sources of the rare metals, highly evolved magmatic fractionation, and structural controls such as the metamorphic core complex setting, with a revised conceptual model for the latter.

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“…There is, however, an increasing number of case studies yielding contrasting ages for pegmatites and spatially associated granites and, thus, showing that there are rare-element pegmatites without an associated source granite (e.g. Smeds 1994, 1996;Fuchsloch et al 2018;Konzett et al 2018;Müller et al 2015Müller et al , 2017Schuster et al 2017;Barros and Menuge 2016;Ilickovic et al 2017;Knoll et al 2018;Simmons et al 1996Simmons et al , 2016Webber et al 2019;Fei et al 2020). These studies imply that not all chemically evolved pegmatites form from residual melts of chemically evolved plutons.…”

Section: Introductionmentioning

confidence: 99%

Two-stage regional rare-element pegmatite formation at Tysfjord, Norway: implications for the timing of late Svecofennian and late Caledonian high-temperature events

Müller

Romer

Augland

et al. 2022

Int J Earth Sci (Geol Rundsch)

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Pegmatite fields within granite plutons are commonly considered to have formed from residual melts of their host. This is not always true as demonstrated by the Tysfjord granite gneiss and its two groups of pegmatites. The Tysfjord granite gneiss, exposed in a tectonic window of the Caledonides of northern Norway, is part of the transscandinavian igneous belt (TIB) that includes several phases of granitic magmatism. In the northern Hamarøy area (Drag-Finnøy), where most rare-element pegmatites occur, Paleoproterozoic and metamorphosed Group 1 allanite–(Ce)–fluorite metapegmatites have similar bulk rock chemical composition as the TIB granite gneiss rocks, indicating that these pegmatites are residual melts. Group 1 metapegmatites, which are up to 400 m in size, are among the largest known intra-plutonic pegmatites with Nb–Y–F (NYF) signature. The formation of these unusually large granite-hosted NYF pegmatites may have been facilitated by the overall high F content of TIB granite gneisses. Undeformed Group 2 amazonite–tourmaline pegmatites yield columbite and zircon U–Pb ages in the range 400–379 Ma. These pegmatites are interpreted to be anatectic melts that formed from the partial melting of Tysfjord granite gneiss. Group 2 pegmatites, including those from Træna Island and the Sjona tectonic window (400 and 414 Ma), formed during late Caledonian ductile shearing and incipient unroofing of the central Scandinavian Caledonides and record progressively younger ages of this event from SW to NE.

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Petrogenesis of the Lijiagou spodumene pegmatites in Songpan-Garze Fold Belt, West Sichuan, China: Evidence from geochemistry, zircon, cassiterite and coltan U-Pb geochronology and Hf isotopic compositions

Cited by 36 publications

References 59 publications

Geochemical Contrasts between Late Triassic Rb-Rich and Barren Pegmatites from Ningshan Pegmatite District, South Qinling Orogen, China: Implications for Petrogenesis and Rare Metal Exploration

Geochemical Contrasts between Late Triassic Rb-Rich and Barren Pegmatites from Ningshan Pegmatite District, South Qinling Orogen, China: Implications for Petrogenesis and Rare Metal Exploration

Spatial‐Temporal Distribution, Geological Characteristics and Ore‐Formation Controlling Factors of Major Types of Rare Metal Mineral Deposits in China

Two-stage regional rare-element pegmatite formation at Tysfjord, Norway: implications for the timing of late Svecofennian and late Caledonian high-temperature events

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