1,2Lidia Pittarello,1,3Seann McKibbin,4Akira Yamaguchi,5,6Gang Ji,5Dominique Schryvers,7Vinciane Debaille,7Philippe Claeys
American Mineralogist 104, 1663-1672 Link to Article [https://doi.org/10.2138/am-2019-7001]
1Analytical, Environmental, and Geo-Chemistry (AMGC), Vrije Universiteit Brussel, Pleinlaan 2, B-1050 Brussels, Belgium
2Department of Mineralogy and Petrography, Natural History Museum Vienna, Burgring 7, A-1010 Vienna, Austria.
3Geowissenschaftliches Zentrum, Georg-August Universität, Goldschmidtstraße 1, 37073 Göttingen, Germany.
4National Institute of Polar Research, Antarctic Meteorite Research Center, 10-3 Midoricho, Tachikawa, Japan
5Electron Microscopy for Materials Science (EMAT), University of Antwerp, Groenenborgerlaan 171, B-2020 Antwerp, Belgium
6University of Lille, CNRS, INRA, ENSCL, UMR 8207, UMET, Unité Matériaux et Transformations, F-59000 Lille, France.
7Laboratoire G-Time (Géochemie: Traçage isotopique, minéralogique et élémentaire), Université Libre de Bruxelles, Av. F.D. Roosevelt 50, 1050 Brussels, Belgium B-1050 Brussels, Belgium
Copyright: The Mineralogical Society of America
Mesosiderite meteorites consist of a mixture of crustal basaltic or gabbroic material and metal. Their formation process is still debated due to their unexpected combination of crust and core materials, possibly derived from the same planetesimal parent body, and lacking an intervening mantle component. Mesosiderites have experienced an extremely slow cooling rate from ca. 550 °C, as recorded in the metal (0.25–0.5 °C/Ma). Here we present a detailed investigation of exsolution features in pyroxene from the Antarctic mesosiderite Asuka (A) 09545. Geothermobarometry calculations, lattice parameters, lamellae orientation, and the presence of clinoenstatite as the host were used in an attempt to constrain the evolution of pyroxene from 1150 to 570 °C and the formation of two generations of exsolution lamellae. After pigeonite crystallization at ca. 1150 °C, the first exsolution process generated the thick augite lamellae along (100) in the temperature interval 1000–900 °C. By further cooling, a second order of exsolution lamellae formed within augite along (001), consisting of monoclinic low-Ca pyroxene, equilibrated in the temperature range 900–800 °C. The last process, occurring in the 600–500 °C temperature range, was likely the inversion of high to low pigeonite in the host crystal, lacking evidence for nucleation of orthopyroxene.
The formation of two generations of exsolution lamellae, as well as of likely metastable pigeonite, suggest non-equilibrium conditions. Cooling was sufficiently slow to allow the formation of the lamellae, their preservation, and the transition from high to low pigeonite. In addition, the preservation of such fine-grained lamellae limits long-lasting, impact reheating to a peak temperature lower than 570 °C. These features, including the presence of monoclinic low-Ca pyroxene as the host, are reported in only a few mesosiderites. This suggests a possibly different origin and thermal history from most mesosiderites and that the crystallography (i.e., space group) of low-Ca pyroxene could be used as parameter to distinguish mesosiderite populations based on their cooling history.