Patterns of Trace-Element Distribution in Calcic Amphiboles as a Function of Metamorphic Grade

Скублов, С. Г.; Drugova, G. M.

doi:10.2113/gscanmin.41.2.383

Cited by 22 publications

(12 citation statements)

References 15 publications

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“…The observed signature can originate from the dissolution of other mineral phases present in this horizon (illite, hornblende, augite, chlorite), less abundant in the chronosequence. For example, amphiboles can contain high concentrations in REEs and negative anomalies in Eu (Skublov and Drugova, 2003). The weathering of two minerals with opposite Eu anomalies may explain the absence of change in this anomaly through time.…”

Section: Ree Evolution With Depth In Podzolic Soil Chronosequence As mentioning

confidence: 99%

Rare earth elements dynamics along pedogenesis in a chronosequence of podzolic soils

et al. 2016

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International audienceRare earth elements (REE) total concentration and signature in soils are known to be impacted by successive soil forming processes. So it be used as probe of soil processes. However, few studies focus on their behavior in Podzols. Podzols result from the combination of two main pedogenic processes: (1) the strong weathering in the surface eluvial horizon; (2) the downward transfer of dissolved organic matter (OM) and mobile AI and Fe, and their accumulation in the illuvial horizon beneath. Iron oxides and OM are known to have strong affinities with REE, and to play an important role in transfer and immobilization of REE. In order to decipher the relative importance of Fe oxide and OM in REE fate during podzolization, and to investigate whether REE can trace Podzol formation, we study here the evolution of REE signatures along five pedons, aged from 120 to 530 years, in a Cambisol-Podzol chronosequence located in the Cox Bay of Vancouver Island. Our results show that the REE content is strongly correlated to the general loss of elements and mineral weathering. Furthermore, the accumulation of secondary OM, Al and Fe-bearing phases does not impact the REE signature of the bulk soil. Both our results and the ones available in the literature indicate that the release of REE induced by weathering and,subsequent leaching in percolating water are the main pathways determining the REE fate in Podzols. Furthermore, we show that REE can be released and mobilized in very short periods of time during podzolization (330 years). (C) 2016 Elsevier B.V. All rights reserved

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Section: Ree Evolution With Depth In Podzolic Soil Chronosequence As mentioning

confidence: 99%

Rare earth elements dynamics along pedogenesis in a chronosequence of podzolic soils

et al. 2016

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“…(1) Under granulite-facies conditions, amphibole sequestrates abundant MREE and HREE (Skublov & Drugova, 2003; Storkey et al 2005; Buick et al 2006) causing depletion of REE contents in coexisting competitors (garnet, zircon and orthopyroxene), evident from the comparison of mineral compositions from amphibole-free granulites with amphibole-bearing granulites having a similar budget of REEs.…”

Section: Discussionmentioning

confidence: 99%

REE partition among zircon, orthopyroxene, amphibole and garnet in a high-grade metabasic system

et al. 2017

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A mafic amphibole-bearing granulite with porphyroblastic garnet was investigated to evaluate: (1) the rare earth element (REE) partition among garnet, zircon, orthopyroxene and amphibole during the metamorphic evolution; (2) the significance of the REE distribution along lobes and bights of reabsorbed garnet rim; and (3) REE distribution coefficient values (DREE) suggestive of chemical equilibrium, assuming garnet as a reference. The results have been compared with those deriving from an intermediate granulite containing porphyroblastic garnet, without amphibole. Porphyroblastic garnet from both samples is rimmed by a continuous corona formed during post-peak decompression characterized by REE-enriched lobes and REE-poor bights. The amphiboles from corona have various REE abundances, reflecting a different dissolution rate of original garnet rim. The initial slow rate of garnet dissolution caused high REE concentration in the new garnet rim due to intra-crystalline diffusion, leading to the formation of REE-poorer amphiboles in corona. Subsequently, under an increasing geothermal gradient and fluid-present conditions, the faster dissolution of garnet determined the formation of bights and the transfer of REEs towards the corona. The timing of garnet growth and its dissolution were checked by U–Pb zircon ages. The zircons dated from 339 Ma to 303 Ma in two rock types combined with the garnet domains (core, outer core, rim) show similar distribution of patterns relative to heavy rare earth elements for zircon and garnet (DHREEzrn/grt), suggesting chemical equilibrium. Zircons dated at c. 300 Ma do not appear in equilibrium with REE-rich garnet lobes, and younger zircons (278 Ma) show a new equilibrium with REE-poor garnet bights. On this basis, the DHREEamph/grt values obtained in specific textural sites might be interpreted as suggestive of equilibrium under granulite conditions.

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“…The composition of metamorphic magnetite changes in response to mainly temperature and oxygen fugacity (Frost, 1991). The partitioning behavior and distribution of trace elements in magnetite depends on the metamorphic grade (Van Baalen, 1993;Skublov et al, 2003). During metamorphism, elements can be activated and transferred (Lin et al, 1982).…”

Section: Indication Of Hydrothermal Overprinting For the Depositmentioning

confidence: 99%

A Textural and Mineralogical Study of the Shanzhuang Banded Iron Formation, Southeastern Margin of the North China Craton: Implications for the Overprint History of Hydrothermal Alteration and Supergenesis after Mineralization

Zhang

Peng

et al. 2020

Acta Geologica Sinica (Eng)

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Banded iron formations (BIFs) are one of the most important chemical sedimentary rocks for understanding the Precambrian evolution of the hydrosphere, atmosphere and biosphere (Klein, 2005; Bekker et al., 2010, 2014). They are mainly composed of alternating silica-rich and iron-rich bands. BIFs are broadly classified as either Algoma-type or Superior-type based on their depositional environment (Gross, 1980; Ohmoto, 2003), although it is more appropriate to treat these classifications as end members, with a wide range of intermediate varieties (Bekker et al., 2012). The former type is stratigraphically and genetically linked to submarine-emplaced maficultramafic to felsic volcanic rocks in greenstone belts, and in some cases, coupled with volcanogenic massive sulfide (VMS) deposits (Ohmoto, 2003; Bekker et al., 2010; Peng et al., 2017). In contrast, the latter type was deposited in the passive-margin setting and was typically interbedded with carbonates and black shales, but generally lacks

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Patterns of Trace-Element Distribution in Calcic Amphiboles as a Function of Metamorphic Grade

Cited by 22 publications

References 15 publications

Rare earth elements dynamics along pedogenesis in a chronosequence of podzolic soils

Rare earth elements dynamics along pedogenesis in a chronosequence of podzolic soils

REE partition among zircon, orthopyroxene, amphibole and garnet in a high-grade metabasic system

A Textural and Mineralogical Study of the Shanzhuang Banded Iron Formation, Southeastern Margin of the North China Craton: Implications for the Overprint History of Hydrothermal Alteration and Supergenesis after Mineralization

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