Stable isotope constraints on the origin of kaolin deposits from Variscan granitoids of Galicia (NW Spain)

Clauer, Norbert; Fallick, Anthony E.; Galán, E.; Aparicio, Patricia; Miras, A.; Fernández-Caliani, Juan Carlos; Aubert, Amélie

doi:10.1016/j.chemgeo.2015.09.022

Cited by 16 publications

(13 citation statements)

References 33 publications

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“…Kaolins of weathering origin generally have higher δ 18 O (from 17 to 23 ) and δD (from −80 to 40 ) values. This is supported by data of the following kaolins of weathering origin: Nuevo Montecastelo kaolins in Spain [43], Variscan kaolins in Spain [16], Burela kaolin in Spain [45], Lastarria kaolin in Chile [17] and La Espingarda kaolin in Patagonia [46].…”

Section: Paleotemperaturessupporting

confidence: 56%

“…The temperature of kaolinitisation (T) of the studied kaolins were calculated using Equation (5) [16] and is presented in Table 8. The Lwamondo kaolin deposit had a mean temperature of 26.9 ± 3.6 • C whereas the Zebediela kaolin had a mean temperature of 36.6 ± 4.2 • C. Kaolinite in equilibrium with the global meteoric water line, kaolinitisation temperatures in the Lwamondo kaolins (26.9 • C), whereas the Zebediela kaolins kaolinitisation temperature was 36.6 • C. The Makoro and Kgwakgwe kaolins formed at around 40 • C [39].…”

Section: Paleotemperaturesmentioning

confidence: 99%

“…The stable isotopic composition of kaolins can provide paleoenvironmental information on the isotopic composition of soil and meteoric waters, as well as paleotemperatures during the formation of the kaolins [11]. The stable isotope geochemistry of clay minerals has been applied in geothermometry, clay mineral genesis and diagenesis and paleoenvironments, amongst other disciplines [12][13][14][15][16][17].…”

Section: Introductionmentioning

confidence: 99%

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Trace Element and Stable Isotope Geochemistry of Lwamondo and Zebediela Kaolins, Limpopo Province, South Africa: Implication for Paleoenvironmental Reconstruction

et al. 2019

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The aim of the present study was the paleoenvironmental reconstruction of the prevailing environment under which the Lwamondo and Zebediela kaolin deposits were formed. Hence, this study reports deuterium and oxygen stable isotope values and trace and rare earth element concentrations for two samples of kaolin. Upper continental crust-normalised trace-element patterns reveal that large ion lithophile elements and high-field-strength elements are generally depleted in Lwamondo and Zebediela kaolins, whereas transition trace elements are generally enriched in these kaolins. Upper continental crust-normalised rare earth element (REE) patterns show that there is a slight enrichment of heavy REEs (HREEs) compared to light REEs (LREEs) in these kaolins. The δ18O and δD stable isotope values for kaolinite from Lwamondo ranged from 17.4‰ to 19.1‰ and from −54‰ to 84‰, respectively, whereas those values for kaolinite from Zebediela varied from 15.6‰ to 17.7‰ and from −61‰ to –68‰ for δ18O and δD, respectively. The REE patterns and the content of other trace elements indicate ongoing kaolinitisation in the Lwamondo and Zebediela kaolins with minimum mineral sorting. The sources of the kaolins varied from basic to acidic and these were derived from an active margin tectonic setting. Lwamondo kaolin was deposited in an oxic environment whereas Zebediela kaolin was deposited under suboxic/anoxic conditions. Based on the δ18O and δD values of the kaolinite, they formed in a supergene environment at temperatures generally below 40 °C.

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Section: Paleotemperaturessupporting

confidence: 56%

Section: Paleotemperaturesmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Trace Element and Stable Isotope Geochemistry of Lwamondo and Zebediela Kaolins, Limpopo Province, South Africa: Implication for Paleoenvironmental Reconstruction

et al. 2019

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“…The Penouta albite granite is similar in composition to other albite granites in the Iberian Massif, most of them located in the innermost part of the Iberian Variscan Belt, namely, in the Central Iberian Zone. Most of these albite leucogranites were affected by an intense albitization, kaolinitization and greisenization (Mangas and Arribas, 1991; Clauer et al ., 2015), probably related to fluid saturation in the apical zone of the leucogranite (López Moro et al ., 2017).…”

Section: Geological Settingmentioning

confidence: 99%

Textural and mineral-chemistry constraints on columbite-group minerals in the Penouta deposit: evidence from magmatic and fluid-related processes

et al. 2018

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The Penouta Sn-Ta deposit, in the northwest of Spain, is a greisenized granitic cupola where Ta minerals occur mainly as disseminations in a leucogranite body intruded in Precambrian–Lower Cambrian gneisses and mica-schists. This leucogranite is a medium- to fine-grained inequigranular rock consisting mainly of quartz, albite, K-feldspar and muscovite. Accessory minerals are mainly of spessartine, zircon, cassiterite, Nb-Ta oxides, monazite, xenotime, native bismuth and pyrite. The alteration processes were mainly albitization, muscovitization and kaolinitization.This leucogranite is peraluminous and P-poor, with 0.03–0.07 wt.% P2O5, 900–1500 ppm Rb, 30–65 ppm Cs, 120–533 ppm Li, 80–140 ppm Ta, 51–81 ppm Nb and up to 569 ppm of Sn.Mineralogical characterization of Nb-Ta oxide minerals was determined by X-ray diffraction, scanning electron microscopy, electron microprobe analysis and mineral liberation analysis. Mn-rich members of the columbite-group minerals (CGM) are the most common Ta-bearing phases, but microlite, wodginite, tapiolite and Ta-rich cassiterite occur also. CGM crystals are commonly zoned concentrically, with a Nb-rich core surrounded by a Ta-rich rim, with a sharp boundary between them. Convoluted zoning occurs also. Dissolution textures resulting from the corrosion of columbite and tantalite rims, in particular, are common. The Mn/(Mn + Fe) ratio varies between 0.33 and 0.97 and the Ta/(Ta + Nb) ratio between 0.07 and 0.93. Wodginite and microlite formed as late replacements of CGM and occur associated with tantalite and cassiterite. Subhedral to anhedral cassiterite crystals, usually up to 200 μm across, occur in two generations: the earlier one is Nb,Ta-poor whereas in the later generation, the Ta content can reach >9 wt.% of Ta2O5 and 1.7 wt.% of Nb. The presence of a fluid phase in the apical zone of the granite, probably related to the separation of a fluid/vapour of the melt, could explain the sponge-like textures, the Ta enrichment associated with these textures, the occurrence of Ta-enriched mineral phases (microlite and wodginite) and their common interstitial character.

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“…Traditional isotope ratio mass spectrometry (IRMS) is commonly used for δ 18 O and δD measurements of clay separates in bulk (e.g., Fernández-Caliani et al, 2010;Mix and Chamberlain, 2014;Clauer et al, 2015).…”

Section: Introductionmentioning

confidence: 99%

NanoSIMS as an analytical tool for measuring oxygen and hydrogen isotopes in clay minerals from palaeosols: Analytical procedure and preliminary results

Laita

Subirana²,

Schaumlöffel³

et al. 2023

Chemical Geology

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Stable isotope constraints on the origin of kaolin deposits from Variscan granitoids of Galicia (NW Spain)

Cited by 16 publications

References 33 publications

Trace Element and Stable Isotope Geochemistry of Lwamondo and Zebediela Kaolins, Limpopo Province, South Africa: Implication for Paleoenvironmental Reconstruction

Trace Element and Stable Isotope Geochemistry of Lwamondo and Zebediela Kaolins, Limpopo Province, South Africa: Implication for Paleoenvironmental Reconstruction

Textural and mineral-chemistry constraints on columbite-group minerals in the Penouta deposit: evidence from magmatic and fluid-related processes

NanoSIMS as an analytical tool for measuring oxygen and hydrogen isotopes in clay minerals from palaeosols: Analytical procedure and preliminary results

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