Magmatic evolution and controls on rare metal-enrichment of the Strange Lake A-type peralkaline granitic pluton, Québec-Labrador

Siegel, Karin; Vasyukova, O. V.; Williams‐Jones, Anthony E.

doi:10.1016/j.lithos.2018.03.003

Cited by 57 publications

(29 citation statements)

References 42 publications

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“…Primary pyrochlore, with high Na and F concentrations and low Ca, is of special interest and can be classified as fluornatropyrochlore. The latter has been rarely found in natural occurrence [4][5][6][13][14][15][16][17] and became a registered mineral species as late as in 2013 [18]. In this respect, it is pertinent to compare the Katugin pyrochlore with its counterparts that are known from other places.…”

Section: Discussionmentioning

confidence: 99%

“…Fluorcalciopyrochlore (Ca,Na) 2 Nb 2 O 6 F is the most widespread phase in the group [3,10,12]. Findings of pyrochlore with prominent Na enrichment over Ca and other cations at the A-site are very few and are limited to several rare-metal deposits hosted by the Nechalacho syenite and nepheline syenite (Canada) [13,14], the Mariupol nepheline syenite (Ukraine) [15], the Strange Lake granite (Canada) [16], and the Halzdan-Buregteg alkaline granite (West Mongolia) [17]. Fluornatropyrochlore (Na,Pb,Ca,REE,U) 2 Nb 2 O 6 F was reported as a mineral species from the Boziguoer granites (China) only in 2013 [18].…”

Section: Introductionmentioning

confidence: 99%

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Pyrochlore-Group Minerals in the Granite-Hosted Katugin Rare-Metal Deposit, Transbaikalia, Russia

et al. 2019

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Pyrochlore group minerals are the main raw phases in granitic rocks of the Katugin complex-ore deposit that stores Nb, Ta, Y, REE, U, Th, Zr, and cryolite. There are three main types: Primary magmatic, early postmagmatic (secondary-I), and late hydrothermal (secondary-II) pyrochlores. The primary magmatic phase is fluornatropyrochlore, which has high concentrations of Na2O (to 10.5 wt.%), F (to 5.4 wt.%), and REE2O3 (to 17.3 wt.%) but also low CaO (0.6–4.3 wt.%), UO2 (to 2.6 wt.%), ThO2 (to 1.8 wt.%), and PbO (to 1.4 wt.%). Pyrochlore of this type is very rare in nature and is limited to a few occurrences: Rare-metal deposits of Nechalacho in syenite and nepheline syenite (Canada) and Mariupol in nepheline syenite (Ukraine). It may have crystallized synchronously with or slightly later than melanocratic minerals (aegirine, biotite, and arfvedsonite) at the late magmatic stage when Fe from the melt became bound, which hindered the crystallization of columbite. Secondary-I pyrochlore follows cracks or replaces primary pyrochlore in grain rims and is compositionally similar to the early phase, except for lower Na2O concentrations (2.8 wt.%), relatively low F (4 wt.%), and less complete A- and Y-sites occupancy. Secondary-II pyrochlore is a product of late hydrothermal alteration, which postdated the formation of the Katugin deposit. It differs in large ranges of elements and contains minor K, Ba, Pb, Fe, and significant Si concentrations but also low Na and F. Its composition mostly falls within the field of hydro- and keno-pyrochlore.

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Section: Discussionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

Pyrochlore-Group Minerals in the Granite-Hosted Katugin Rare-Metal Deposit, Transbaikalia, Russia

et al. 2019

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“…For example, numerous studies have shown that the Nb and rare earth elements are enriched in carbonatite and alkaline rock complexes originated from the mantle, while highly differentiated granites in the crust and the LCT-type pegmatite are enriched in rare metals like Li, Be, Rb, Cs, Nb and Ta, and crust-mantle mixed-source alkaline granite and the NYFtype pegmatite have high abundances of Nb, Ta, Zr, Hf and Y. The possible formation of alkaline granite includes the differentiation of basaltic magma, partial melting of deep crustal materials, or the mixing of crust-derived magma and mantle-derived mafic magma (Dostal and Shellnutt, 2015;Siegel et al, 2018). The genetic mechanism of the NYF-type pegmatite includes lowdegree partial melting of the lower crustal material, such as granulite, granite, quartz diorite, the extreme fractionation of mantle-sourced magma, such as basaltic, tonalitic magma, the magma generated in the lower crust and upper mantle transition zone, and the anataxis of the depleted granulite source zone (McCauley and Bradley, 2014;London, 2018;Siegel et al, 2018).…”

Section: Source Of Rare Metal Elementsmentioning

confidence: 99%

“…In general, in the process of rare metal element mobilization, transportation and enrichment during magmatism and crust-mantle interaction, the following factors place major constraints on the formation of largescale rare metal deposits (Jiang et al, 2019). First, the abundance of rare metal elements in the magma source regions, second, whether these elements can be efficiently mobilized from the source rock into the magma, and the third is the rare metal element behavior that is controlled by the magma differentiation crystallization and fluid exsolution process (López-Moro et al, 2017;Siegel et al, 2018).…”

Section: Magmatic Fractionation and Its Role For Rare Metal Enrichmentmentioning

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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“…In recent decades, due to the wide application of high‐field‐strength elements (HFSE) and rare earth elements (REEs) in modern high‐tech industries, there has been a sharp increase in the demand for many of these elements. Previous studies widely suggest that Nb and the REEs are spatially associated with alkaline igneous rocks worldwide, such as the nepheline syenite‐hosted Khaldzan Buregte Zr–Nb–REE deposit in Mongolia (Kempe, Götze, Dandar, & Habermann, 1999; Kovalenko et al, 1995), the peralkaline granite‐hosted Strange Lake REE–Zr–Nb deposit in Canada (Gysi, Williams‐Jones, & Collins, 2016; Salvi & Williams‐Jones, 1990, 1996, 2006; Siegel, Vasyukova, & Williams‐Jones, 2018; Vasyukova & Williams‐Jones, 2014), and the sole trachytic volcanic rock‐hosted Toongi and Brockman rare metal (Nb, Zr, Y, and REE) deposits of significance, both in Australia (Ramsden, French, & Chalmers, 1993; Spandler & Morris, 2016; Taylor, Esslemont, & Sun, 1995; Taylor, Page, Esslemont, Rock, & Chalmers, 1995). In the volcanic rock‐hosted rare metal deposit, rare metal enrichment can be regarded as a multi‐stage process, which includes variable primary enrichment and secondary upgrading processes.…”

Section: Introductionmentioning

confidence: 99%

Trachytic magmatism and Nb–rare earth element mineralization in the Pingli area, North Daba Mountain: Insights from geochronology and geochemistry

et al. 2020

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North Daba Mountain of South Qinling. These trachytic rocks contain relatively large quantities of Nb-and rare earth element (REE)-bearing minerals. This study presents the zircon U-Pb ages, REE content, Hf isotope data, and whole-rock compositions of the Nb-REE mineralized trachytes from the Pingli area. U-Pb geochronological data reveal the ages of zircon grains can be divided into three groups: 431-395, 270-255, and 241-240 Ma. Cathodoluminescence images and REE compositions confirm a magmatic origin for the zircons with age of 431-395 and 270-255 Ma. Zircon grains with ages of 431-395 Ma have the characteristics similar to relict zircons. The 270-255 Ma age group is interpreted to represent the diagenetic age of the trachyte. Zircon grains with a younger age (241-240 Ma) are distinguishable from magmatic zircons with regards to their cathodoluminescence patterns and REE signatures, indicating a hydrothermal origin. The 241-240 Ma age group reflects the Nb-REE mineralization age in the trachyte. Geochemically, the trachytes have high SiO 2 contents but low MgO contents and Mg# values. They can be classified as alkaline-series and belong to the metaluminous-peraluminous rocks, with A/CNK ratios between 0.81 and 1.11. The trachytes are characterized by enrichments in the light rare earth elements (LREEs) and large-ion lithophile elements (LILEs), but are depleted in the heavy REEs (HREEs), Ti, Sr, and P, with negligible Eu. These geochemical features, together with the highly negative εHf(t) (−8.25 to −11.25) values of the zircon grains, indicate that the primary magma associated with these trachytes likely originated from the partial melting of ancient lower crust. The presence of a positive εHf(t) (4.12) value suggests that this process may have involved a small amount of juvenile basaltic crust material. This is different from other rare metal-hosting trachytes worldwide, whose parental magmas are mantle-derived, analogous to basalts generated in an intraplate setting. Nevertheless, trachytes are specifically Nb-REE mineralized by primary enrichment processes (fractional crystallization) or secondary upgrading processes (hydrothermal alteration). The Nb-REE mineralization is closely related to Early

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Magmatic evolution and controls on rare metal-enrichment of the Strange Lake A-type peralkaline granitic pluton, Québec-Labrador

Cited by 57 publications

References 42 publications

Pyrochlore-Group Minerals in the Granite-Hosted Katugin Rare-Metal Deposit, Transbaikalia, Russia

Pyrochlore-Group Minerals in the Granite-Hosted Katugin Rare-Metal Deposit, Transbaikalia, Russia

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

Trachytic magmatism and Nb–rare earth element mineralization in the Pingli area, North Daba Mountain: Insights from geochronology and geochemistry

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