Trace element partitioning between amphibole and hydrous silicate glasses at 0.6–2.6 GPa

Zhang, Bo; Hu, Xianxu; Tang, Qizhe; Zhou, Wenge

doi:10.1007/s11631-019-00322-4

Cited by 10 publications

(11 citation statements)

References 50 publications

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“…In addition, the breakdown of the amphiboles in the mantle in the island arc environment is the s main source of the H2O during the formations of the granites above the deep subduction zones [89]. The amphibole metaso-matism put an essential role in the distribution of the LILE and HFSE components in the mantle [90] due to the high partition coefficients of this mineral [90][91][92][93][94]. Nevertheless, the more recent researches show that pargasites are stable to 20.5 GPa [23].…”

Section: Comparisons With the Amphiboles Worldwidementioning

confidence: 99%

“…The melts reconstructed with the KD for the amphiboles [91,92,105] reveal very high LREE patterns and concave in the MREE part (Figure 13). The levels of the HFSE are mostly low but there are some varieties rather high in Zr which is probably evidence about the participation of the H2O rich melts/fluids in their generation.…”

Section: Pargasites Low-middle Preasuresmentioning

confidence: 99%

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Unique Amphibole Bearing Mantle Column Beneath the Leningrad Kimberlite Pipe, West Ukukit Field, NE Yakutia

Ashchepkov¹,

Babushkina²,

Mevedev³

et al. 2021

Preprint

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In the subcratonic mantle beneath Leningrad pipe, West Ukukit field, Yakutia garnet thermoba-rometry give division to 7 horizons (paleosubduction slabs). Cr-bearing amphiboles >500 reveal a broad range changing from Cr- pargasitic hornblendes to pargasites, edinites, kataforites, К-richterites with increasing pressure determined with new amphibole thermobarometer. Cr-hornblendes compiles the high-temperature branch from 3.5 GPa to Moho for basaltic melt. Amphiboles in the middle eddinites and high-pressure interval reveal different PT ranges from 35 to 40 mw/m2. Richterites near the lithosphere base both trace low –T and convective branches. The amphiboles reveal the 9 geochemical groups. The low-temperature varieties reveal Eu minima and U, Ba, Sr peaks high LILE, Sr, Rb and troughs in Nb, Pb. While high –T varieties have no Eu dips and reveal higher HFSE. Clinopyroxenes and garnets show variable trace ele-ment patterns and divisions in groups eth the plume and subduction signs. The contrasting be-haviour of Ta and Nb is regulated by the rutile partition coefficients likely for primary eclogites. Subduction and Na and K (siliceous) types of fluids percolated through the mantle with abun-dant eclogites causing amphibolization at the different levels of the mantle column. The plume melts produced hybridism and more smooth trace element patterns in reacted minerals, clino-pyroxene. monomineral thermobarometry.

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Section: Comparisons With the Amphiboles Worldwidementioning

confidence: 99%

Section: Pargasites Low-middle Preasuresmentioning

confidence: 99%

Unique Amphibole Bearing Mantle Column Beneath the Leningrad Kimberlite Pipe, West Ukukit Field, NE Yakutia

Ashchepkov¹,

Babushkina²,

Mevedev³

et al. 2021

Preprint

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“…DOI: https://doi.org/10.2138/am-2022-8536. http://www.minsocam.org/ 2020b, 2007; Hilyard et al 2000a;Zhang et al 2019). It is widely accepted that the resulting partition coefficients depend on the chemical compositions of mineral and melt phases, pressure, temperature, and H2O-content of the melt, as well as on the redox conditions (Blundy and Wood 2003;Adam and Green 2006;Aigner-Torres et al 2007;Severs et al 2009;van Kan Parker et al 2010;Hill et al 2011;Fabbrizio et al 2021).…”

Section: Introductionmentioning

confidence: 99%

“…Moreover, Blundy and Wood (1994) provided a theoretical framework based on the lattice strain model (Brice 1975) for the interpretation of trace element partitioning. So far, it has been applied successfully to trace element partitioning between pyroxene (e.g., Wood and Blundy 1997;Schmidt et al 1999;Adam and Green 2006;Liang 2012, 2013;Mollo et al 2018;Bonechi et al 2021;Fabbrizio et al 2021), olivine (e.g., Zanetti et al 2004;Liang 2013), garnet (e.g., Draper andvan Westrenen 2007;van Westrenen and Draper 2007;Sun and Liang 2013), amphibole (e.g., LaTourrette et al 1995;Adam and Green 2006;Tiepolo et al 2007;Wan et al 2009;Nandedkar et al 2016;Shimizu et al 2017;Zhang et al 2019;Cannaò et al 2022), phlogopite (e.g., LaTourrette et al 1995;Schmidt et al 1999;Fabbrizio et al 2010), leucite (e.g., Schmidt et al 1999;Fabbrizio et al 2008), feldspars (e.g., Icenhower and London 1996;Fabbrizio et al 2009) and their coexisting melts. Despite numerous investigations on the partition between crystals and melt, there are still some mineral phases, including amphibole, for which data are limited or missing.…”

Section: Introductionmentioning

confidence: 99%

“…http://www.minsocam.org/ and M4-M4' sites of amphibole. Also, we reviewed the influence of melt and amphibole compositions, temperature, and pressure on the behavior of partition coefficients between amphiboles and glasses by integrating our data with a literature data set (LEPR database and data from Nandedkar et al 2016, Zhang et al 2019, and Cannaò et al 2022) spanning a wide range of pressures (0.6-2.5 GPa), temperatures (780-1100 °C) and compositions (from basanite to rhyolite). Finally, we observed whether a composition approaching the APR16 one is able, through the crystallization of amphibole in a deep differentiation process, to produce an andesite melt with trace element abundances similar to those of the calc-alkaline volcanic products found in Parete and Castelvolturno bore-holes (NW of Campi Flegrei, Italy).…”

Section: Introductionmentioning

confidence: 99%

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Experimental investigation of trace element partitioning between amphibole and alkali basaltic melt: Toward a more general partitioning model with implications for amphibole fractionation at deep crustal levels

Bonechi,

Fabbrizio,

Perinelli

et al. 2023

American Mineralogist

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Time-series experiments were carried out in a piston cylinder apparatus conducted at 0.8 GPa and 1030-1080 °C using as starting material a hydrous K-basalt melt to determine the element partition coefficients between amphibole and silicate glass. Major, minor, and trace element compositions of This is the peer-reviewed, final accepted version for American Mineralogist, published by the Mineralogical Society of America.The published version is subject to change. Cite as Authors (Year) Title. American Mineralogist, in press.

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Constraints on the pre-eruptive magma storage conditions and magma evolution of the 56–30 ka explosive volcanism of Ciomadul (East Carpathians, Romania)

Cserép,

Szemerédi,

Harangi

et al. 2023

Contrib Mineral Petrol

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A detailed mineral-scale study was conducted on pumices of the latest, dominantly explosive eruption epoch (56–30 ka) of Ciomadul, the youngest, long-dormant volcano in eastern-central Europe for characterizing the magma storage system and for understanding better the changes in eruption style from effusive to explosive. The mineral cargo of dacitic pumices enables us to constrain the conditions of the pre-recharge crystal mush, the recharge magmas and the post-recharge magma prior to eruptions. A careful evaluation of the results yielded by various thermometers, barometers, oxybarometers, chemometers and hygrometers as well as direct comparison with experimental data were necessary to select the appropriate techniques and therefore to constrain the conditions for the Ciomadul magmatic system. Beneath the volcano, a felsic crystal mush body is inferred at 8–12 km depth comprising slightly oxidized (0.5–1.6 ∆NNO), low-temperature (680–750 °C), highly crystalline magma. This zone is underlain by a deep magma storage zone with less evolved, hot (> 900 °C) magma at 16–40 km depth. The dominantly explosive volcanism after the effusive eruptions (160–90 ka) can be explained by the ascent of distinct recharge magmas. They contained high-Mg (MgO > 18 wt%) amphibole, which could have crystallized from ultrahydrous (H2O > 8 wt%) magma at near-liquidus conditions. The rates of amphibole overgrowth and microphenocryst formation require weeks to months for the magma mixing and the eruption events. The hybridized melt became more oxidized and contained dissolved water in around 5.5 wt% at temperature of 790–830 °C calculated from the re-equilibrated Fe-Ti oxides. These magma properties along with the degree of crystallinity (27–38 vol% crystals) favored rapid magma ascent and an explosive style eruption. Thus, the strongly hydrous nature of the recharge magma in addition to the crystallinity and H2O content of the pre-eruption magma plays an important role in controlling the eruption style.

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Trace element partitioning between amphibole and hydrous silicate glasses at 0.6–2.6 GPa

Cited by 10 publications

References 50 publications

Unique Amphibole Bearing Mantle Column Beneath the Leningrad Kimberlite Pipe, West Ukukit Field, NE Yakutia

Unique Amphibole Bearing Mantle Column Beneath the Leningrad Kimberlite Pipe, West Ukukit Field, NE Yakutia

Experimental investigation of trace element partitioning between amphibole and alkali basaltic melt: Toward a more general partitioning model with implications for amphibole fractionation at deep crustal levels

Constraints on the pre-eruptive magma storage conditions and magma evolution of the 56–30 ka explosive volcanism of Ciomadul (East Carpathians, Romania)

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