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Interaction of model peridotite with H2O-KCl fluid: Experiment at 1.9 GPa and its implications for upper mantle metasomatism

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Abstract

Mineralogical and geochemical data suggest that chloride components play an important role in the transformation and partial melting of upper mantle peridotites. The effect of KCl on the transformation of hydrous peridotite rich in Al2O3, CaO, and Na2O was examined in experiments aimed at studying interaction between model NCMAS peridotite with H2O-KCl fluid under a pressure of 1.9 GPa, temperatures of 900–1200°C, and various initial H2O/KCl ratios. The experimental results indicate that KCl depresses the solidus temperature of the hydrous peridotite: this temperature is <900°C at 1.9 GPa, which is more than 100°C lower than the solidus temperature (1000–1025°C) of hydrous peridotite in equilibrium with KCl-free fluid. The reason for the decrease in the melting temperature is that the interaction of KCl with silicates prevails over the effect of chloride on the water activity in the fluid. Experimental data highlight the key role of Al2O3 as a component controlling the whole interaction process between peridotite and H2O-KCl fluid. Garnet, spinel, and pargasite-edenite amphibole in association with aluminous orthopyroxene are unstable in the presence of H2O-KCl fluid at a chloride concentration in the fluid as low as approximately 2 wt % and are replaced by Cl-bearing phlogopite (0.4–1.1 wt % Cl). Interaction with H2O-KCl fluid does not, however, affect clinopyroxene and forsterite, which are the Al poorest phases of the system. Chlorine stabilizes phlogopite at relatively high temperatures in equilibrium with melt at temperatures much higher than the solidus (>1200°C). The compositional evolution of melt generated during the melting of model peridotite in the presence of H2O-KCl fluid is controlled, on the one hand, by the solubility of the H2O-KCl fluid in the melt and, on the other hand, by phlogopite stability above the solidus. At temperatures below 1050°C, at which phlogopite does not actively participate in melting reactions, fluid dissolution results in SiO2-undersaturated (35–40 wt %) and MgO-enriched (up to 45 wt %) melts containing up to 4–5 wt % K2O and 2–3 wt % Cl. At higher temperatures, active phlogopite dissolution and, perhaps, also the separation of immiscible aqueous chloride liquid give rise to melts containing >10 wt % K2O and 0.3–0.5 wt % Cl. Our experimental results corroborate literature data on the transformation of upper mantle peridotites into phlogopite-bearing associations and the formation of ultrapotassic and highly magnesian melts.

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Abbreviations

Amph :

amphibole

Ca-Ts :

Ca-Tschermak molecule

Cpx :

clinopyroxene

Di :

diopside

En :

enstatite

Fo :

forsterite

Grs :

grossular

Grt :

garnet

Jd :

jadeite

L :

melt

Mg-Ts :

Mg-Tschermak molecule

Ol :

olivine

Opx :

orthopyroxene

Phl :

phlogopite

Prg :

pargasite

Prp :

pyrope

Spl :

spinel

X KCl = KCl/(KCl + H2O):

KCl mole fraction in aqueous salt fluid

\(X_{H_2 O} = {{H_2 O} \mathord{\left/ {\vphantom {{H_2 O} {\left( {KCl + H_2 O} \right)}}} \right. \kern-\nulldelimiterspace} {\left( {KCl + H_2 O} \right)}}\) :

H2O mole fraction in aqueous salt fluid

\(a_{H_2 O}\) :

H2O activity in aqueous salt fluid

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Authors and Affiliations

  1. Institute of Experimental Mineralogy, Russian Academy of Sciences, ul. Akademika Ossipyana 4, Chernogolovka, Moscow oblast, 142432, Russia

    O. G. Safonov & V. G. Butvina

  2. Geological Faculty, Moscow State University, Moscow, 119899, Russia

    O. G. Safonov

  3. Department of Geology, University of Johannesburg, Auckland Park, Johannesburg, 2006, South Africa

    O. G. Safonov

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  1. O. G. Safonov
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  2. V. G. Butvina
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Correspondence to O. G. Safonov.

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Original Russian Text © O.G. Safonov, V.G. Butvina, 2013, published in Petrologiya, 2013, Vol. 21, No. 6, pp. 654–672.

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Safonov, O.G., Butvina, V.G. Interaction of model peridotite with H2O-KCl fluid: Experiment at 1.9 GPa and its implications for upper mantle metasomatism. Petrology 21, 599–615 (2013). https://doi.org/10.1134/S0869591113060076

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