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Pargasite at high pressure and temperature

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Abstract

The P–T phase stability field, the thermoelastic behavior and the P-induced deformation mechanisms at the atomic scale of pargasite crystals, from the “phlogopite peridotite unit” of the Finero mafic–ultramafic complex (Ivrea-Verbano Formation, Italy), have been investigated by a series of in situ experiments: (a) at high pressure (up to 20.1 GPa), by single-crystal synchrotron X-ray diffraction with a diamond anvil cell, (b) at high temperature (up to 823 K), by powder synchrotron X-ray diffraction using a hot air blower device, and (c) at simultaneous HP–HT conditions, by single-crystal synchrotron X-ray diffraction with a resistive-heated diamond anvil cell (P max = 16.5 GPa, T max = 1200 K). No phase transition has been observed within the P–T range investigated. At ambient T, the refined compressional parameters, calculated by fitting a second-order Birch–Murnaghan Equation of State (BM-EoS), are: V 0 = 915.2(8) Å3 and K P0,T0 = 95(2) GPa (β P0,T0 = 0.0121(2) GPa−1) for the unit-cell volume; a 0 = 9.909(4) Å and K(a) P0,T0 = 76(2) GPa for the a-axis; b 0 = 18.066(7) Å and K(b) P0,T0 = 111(2) GPa for the b-axis; c 0 = 5.299(5) Å and K(c) P0,T0 = 122(12) GPa for the c-axis [K(c) P0,T0 ~ K(b) P0,T0 > K(a) P0,T0]. The high-pressure structure refinements (at ambient T) show a moderate contraction of the TO4 double chain and a decrease of its bending in response to the hydrostatic compression, along with a pronounced compressibility of the A- and M(4)-polyhedra [K P0, T0(A) = 38(2) GPa, K P0, T0(M4) = 79(5) GPa] if compared to the M(1)-, M(2)-, M(3)-octahedra [K P0, T0(M1,2,3) ≤ 120 GPa] and to the rigid tetrahedra [K P0, T0(T1,T2) ~ 300 GPa]. The thermal behavior, at ambient pressure up to 823 K, was modelled with Berman’s formalism, which gives: V 0 = 909.1(2) Å3, α0 = 2.7(2)·10−5 K−1 and α1 = 1.4(6)·10−9 K−2 [with α0(a) = 0.47(6)·10−5 K−1, α0(b) = 1.07(4)·10−5 K−1, and α0(c) = 0.97(7)·10−5 K−1]. The petrological implications for the experimental findings of this study are discussed.

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Acknowledgements

Mario Tribaudino and Wilson Crichton are gratefully thanked for the useful and fruitful comments and suggestions. The Editor, Milan Rieder is acknowledged for handling the manuscript. PETRA-III synchrotron facility (Hamburg, Germany) is acknowledged for provision of beamtime at P02.2 beamline. ELETTRA (Trieste, Italy) synchrotron facility is acknowledged for beamtime at MCX beamline. J. Plaisier is thanked for the support during the experiment at ELETTRA. The authors acknowledge the University of Milano, the Doctoral School of Earth Science of the University of Milano, and the DCO (Deep Carbon Observatory) for supporting the research.

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Authors and Affiliations

  1. Dipartimento di Scienze della Terra, Università degli Studi di Milano, Via Botticelli 23, 20133, Milan, Italy

    Davide Comboni, Paolo Lotti, G. Diego Gatta & Marco Merlini

  2. ELETTRA Sincrotrone Trieste S.c.P.A, Strada Statale 14, km. 163.5, 34149, Basovizza, Trieste, Italy

    Paolo Lotti

  3. CNR-Istituto di Cristallografia, Sede di Bari, Via G. Amendola 122/O, Bari, Italy

    G. Diego Gatta

  4. Photon Sciences, DESY, Notkestrasse 85, 22607, Hamburg, Germany

    Hanns-Peter Liermann

  5. Bayerisches Geoinstitute, University of Bayreuth, 95440, Bayreuth, Germany

    Daniel J. Frost

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  1. Davide Comboni
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Comboni, D., Lotti, P., Gatta, G.D. et al. Pargasite at high pressure and temperature. Phys Chem Minerals 45, 259–278 (2018). https://doi.org/10.1007/s00269-017-0915-0

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