^1,2Lu Feng, ^3,4Masaaki Miyahara, ⁵Toshiro Nagase, ³Eiji Ohtani, ¹Sen Hu, ⁶Ahmed El Goresy, ¹Yangting Lin
American Mineralogist 102, 1254-1262 Link to Article [DOI: 10.2138/am-2017-5905]
¹Key Laboratory of Earth and Planetary Physics, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing, 100029,China
²Guangzhou Institute of Geochemistry, Chinese Academy of Sciences, Guangzhou, 510640, China
³Institute of Mineralogy, Petrology, and Economic Geology, Tohoku University, Sendai, 980-8578, Japan
⁴Department of Earth and Planetary Systems Science, Graduate School of Science, Hiroshima University, Higashi-Hiroshima, 739-8526, Japan
⁵Center for Academic Resources and Archives, Tohoku University, Sendai, 980-8578, Japan
⁶Bayerisches Geoinstitut, Universität Bayreuth, Bayreuth, 95447, Germany
Copyright: The Mineralogical Society of America

Akimotoite [(Mg,Fe)SiO₃-ilmenite] was encountered in shock-induced melt veins of Grove Mountains (GRV) 052082, a highly equilibrated low iron ordinary chondritic meteorite (L6). Coexistence of ringwoodite, majorite, and majorite-pyrope solid solution indicates the shock pressure at 18–23 GPa and temperature of 2000–2300 °C during the natural dynamic event. Most low-Ca pyroxene clasts entrained in the melt veins have been partially or entirely transformed into akimotoite-pyroxene glass assemblages, which contain micrometer-sized areas with various brightness in the backscattered electron images, different from the chemically homogeneous grains in the host-rock (Fs_20.5–21.3). The transmission electron microscopy study of a focused ion beam (FIB) slice from the heterogeneous areas shows that the assemblages are composed of FeO-depleted and heterogeneous akimotoite (Fs_6–19) crystals (100 nm up to 400 nm in size) scattered in FeO-enriched and relatively homogeneous pyroxene glass (Fs_31–39). All analyses of the akimotoite-pyroxene glass assemblages plot on a fractionation line in FeO-MgO diagram, with the host-rock pyroxene at the middle between the compositions of FeO-depleted akimotoite and the FeO-enriched pyroxene glass. These observations are different from previous reports of almost identical compositions of akimotoite, bridgmanite [(Mg,Fe)SiO₃-perovskite], or pyroxene glass to the host rock pyroxene (Chen et al. 2004; Ferroir et al. 2008; Ohtani et al. 2004; Tomioka and Fujino 1997), which is consistent with solid-state transformation from pyroxene to akimotoite and preexisting bridgmanite that could be vitrified. The observed fractionation trend and the granular shapes of akimotoite suggest crystallization from liquid produced by shock melting of the host-rock pyroxene, and the pyroxene glass matrix was probably quenched from the residual melt. However, this interpretation is inconsistent with the static experiments that expect crystallization of majorite [(Mg,Fe)SiO₃-garnet], instead of akimotoite, from pyroxene liquid (Sawamoto 1987). Our discovery raises the issue on formation mechanisms of the high-pressure polymorphs of pyroxene and places additional constraints on the post-shock high-pressure and high-temperature conditions of asteroids.

¹Danika F.Wellington et al. (>10)*
American Mineralogist 102, 1202-1217 Link to Article [DOI: 10.2138/am-2017-5760CCBY]
¹School of Earth and Space Exploration, Arizona State University, Tempe, Arizona 85287, U.S.A.
*Find the extensive, full author and affiliation list on the publishers website
Copyright: The Mineralogical Society of America

The Mastcam CCD cameras on the Mars Science Laboratory Curiosity Rover each use an 8-position filter wheel in acquiring up to 1600 × 1200 pixel images. The filter set includes a broadband near-infrared cutoff filter for RGB Bayer imaging on each camera and 12 narrow-band geology filters distributed between the two cameras, spanning the wavelength range 445–1013 nm. This wavelength region includes the relatively broad charge-transfer and crystal-field absorption bands that are most commonly due to the presence of iron-bearing minerals. To identify such spectral features, sequences of images taken with identical pointings through different filters have been calibrated to relative reflectance using pre-flight calibration coefficients and in-flight measurements of an onboard calibration target. Within the first 1000 sols of the mission, Mastcam observed a spectrally diverse set of materials displaying absorption features consistent with the presence of iron-bearing silicate, iron oxide, and iron sulfate minerals. Dust-coated surfaces as well as soils possess a strong positive reflectance slope in the visible, consistent with the presence of nanophase iron oxides, which have long been considered the dominant visible-wavelength pigmenting agent in weathered martian surface materials. Fresh surfaces, such as tailings produced by the drill tool and the interiors of rocks broken by the rover wheels, are grayer in visible wavelengths than their reddish, dust-coated surfaces but possess reflectance spectra that vary considerably between sites. To understand the mineralogical basis of observed Mastcam reflectance spectra, we focus on a subset of the multispectral data set for which additional constraints on the composition of surface materials are available from other rover instruments, with an emphasis on sample sites for which detailed mineralogy is provided by the results of CheMin X-ray diffraction analyses. We also discuss the results of coordinated observations with the ChemCam instrument, whose passive mode of operation is capable of acquiring reflectance spectra over wavelengths that considerably overlap the range spanned by the Mastcam filter set (Johnson et al. 2016). Materials that show a distinct 430 nm band in ChemCam data also are observed to have a strong near-infrared absorption band in Mastcam spectral data, consistent with the presence of a ferric sulfate mineral. Long-distance Mastcam observations targeted toward the flanks of the Gale crater central mound are in agreement with both ChemCam spectra and orbital results, and in particular exhibit the spectral features of a crystalline hematite layer identified in MRO/CRISM data. Variations observed in Mastcam multi-filter images acquired to date have shown that multispectral observations can discriminate between compositionally different materials within Gale Crater and are in qualitative agreement with mineralogies from measured samples and orbital data.

¹Ryoji Tanaka, ¹Eizo Nakamura
Nature Astronomy 1, 0137 Link to Article [doi:10.1038/s41550-017-0137]
¹The Pheasant Memorial Laboratory for Geochemistry and Cosmochemistry, Institute for Planetary Materials, Okayama University, Misasa, Tottori 682-0193, Japan

We currently do not have a copyright agreement with this publisher and cannot display the abstract here

Peter J. MOUGINIS-MARK¹, Joseph BOYCE¹, Virgil L. SHARPTON², and Harold GARBEIL¹
Meteoritics & Planetary Science (in Press) Link to Article [DOI: 10.1111/maps.12895]
¹Hawaii Institute of Geophysics and Planetology, University of Hawaii, Honolulu, Hawaii 96822, USA
²Lunar and Planetary Institute, Houston, Texas 77058, USA
Published by arrangement with John Wiley & Sons

We review the methods and data sets used to determine morphometric parameters related to the depth (e.g., rim height and cavity depth) and diameter of Martian craters over the past ~45 yr, and discuss the limitations of shadow length measurements, photoclinometry, Earth-based radar, and laser altimetry. We demonstrate that substantial errors are introduced into crater depth and diameter measurements that are inherent in the use of 128th-degree gridded Mars Orbiter Laser Altimeter (MOLA) topography. We also show that even the use of the raw MOLA Precision Engineering Data Record (PEDR) data can introduce errors in the measurement of craters a few kilometers in diameter. These errors are related to the longitudinal spacing of the MOLA profiles, the along-track spacing of the individual laser shots, and the MOLA spot size. Stereophotogrammetry provides an intrinsically more accurate method for measuring depth and diameter of craters on Mars when applied to high-resolution image pairs. Here, we use 20 stereo Context Camera (CTX) image pairs to create digital elevation models (DEMs) for 25 craters in the diameter range 1.5–25.6 km and cover the latitude range of 25^° S to 42^° N. These DEMs have a spatial scale of ~24 m per pixel. Six additional craters, 1.5–3.1 km in diameter, were studied using publically available DEMs produced from High-Resolution Imaging Science Experiment (HiRISE) image pairs. Depth/diameter and rim height were determined for each crater, as well as the azimuthal variation of crater rim height in 1-degree increments. These data indicate that morphologically fresh Martian craters at these diameters are significantly deeper for a given size than previously reported using Viking and MOLA data, most likely due to the improvement in spatial resolution provided by the CTX and HiRISE data.

Hamed POURKHORSANDI¹, Massimo D’ORAZIO¹, Pierre ROCHETTE¹, Millarca VALENZUELA³, Jérôme GATTACCECA¹, Hassan MIRNEJAD^4,5, Brad SUTTER⁶, Aurore HUTZLER⁷, and Maria ABOULAHRIS^1,8

Meteoritics & Planetary Science (in Press) Link to Article [DOI: 10.1111/maps.12894]

¹CNRS, Aix-Marseille Univ., IRD, Coll. France, CEREGE, Aix-en-Provence, France
²Dipartimento di Scienze della Terra, Universit a di Pisa, Via S. Maria 53, I-56126 Pisa, Italy
³Instituto de Astrof ısica, Pontificia Universidad Cato lica de Chile, Vicun~a Mackena 4860, Macul, Santiago, Chile
⁴Department of Geology, Faculty of Sciences, University of Tehran, Tehran 14155-64155, Iran
⁵Department of Geology and Environmental Earth Sciences, Miami University, Oxford, Ohio 45056, USA
⁶Jacobs-NASA, Johnson Space Center, Houston, Texas 77058, USA
⁷Natural History Museum, Burgring 7, A-1010 Vienna, Austria
⁸D epartement de G eologie, Facult e des Sciences, Universit e Hassan II Casablanca, Casablanca, Morocco
Published by arrangement with John Wiley & Sons

The behavior of rare earth elements (REEs) during hot desert weathering of meteorites is investigated. Ordinary chondrites (OCs) from Atacama (Chile) and Lut (Iran) deserts show different variations in REE composition during this process. Inductively coupled plasma–mass spectrometry (ICP-MS) data reveal that hot desert OCs tend to show elevated light REE concentrations, relative to OC falls. Chondrites from Atacama are by far the most enriched in REEs and this enrichment is not necessarily related to their degree of weathering. Positive Ce anomaly of fresh chondrites from Atacama and the successive formation of a negative Ce anomaly with the addition of trivalent REEs are similar to the process reported from Antarctic eucrites. In addition to REEs, Sr and Ba also show different concentrations when comparing OCs from different hot deserts. The stability of Atacama surfaces and the associated old terrestrial ages of meteorites from this region give the samples the necessary time to interact with the terrestrial environment and to be chemically modified. Higher REE contents and LREE-enriched composition are evidence of contamination by terrestrial soil. Despite their low degrees of weathering, special care must be taken into account while working on the REE composition of Atacama meteorites for cosmochemistry applications. In contrast, chondrites from the Lut desert show lower degrees of REE modification, despite significant weathering signed by Sr content. This is explained by the relatively rapid weathering rate of the meteorites occurring in the Lut desert, which hampers the penetration of terrestrial material by forming voluminous Fe oxide/oxyhydroxides shortly after the meteorite fall.

Shinsuke KATO¹, Tomokatsu MOROTA¹, Yasushi YAMAGUCHI¹, Sei-ichiro WATANABE¹, Hisashi OTAKE², and Makiko OHTAKE²
Meteoritics & Planetary Science (in Press) Link to Article [DOI: 10.1111/maps.12896]

¹Graduate School of Environmental Studies, Nagoya University, Furo-cho, Chikusa-ku, Nagoya 464–8602, Japan
²Japan Aerospace Exploration Agency, 3-1-1 Yoshinodai, Sagamihara, Kanagawa 229-8510, Japan
Published by arrangement with John Wiley & Sons

Mare basalts provide insights into the composition and thermal history of the lunar mantle. The ages of mare basalts suggest a first peak of magma activity at 3.2–3.8 Ga and a second peak at ~2 Ga. In this study, we reassess the correlation between the titanium contents and the eruption ages of mare basalt units using the compositional and chronological data updated by SELENE (Kaguya). Using morphological and geological criteria, we calculated the titanium content of 261 mare units across a representative area of each mare unit. In the Procellarum KREEP Terrane, where the latest eruptions are located, an increase in the mean titanium content is observed during the Eratosthenian period, as reported by previous studies. We found that the increase in the mean titanium content occurred within a relatively short period near approximately 2.3 Ga, suggesting that the magma source of the mare basalts changed at this particular age. Moreover, the high-titanium basaltic eruptions are correlated with a second peak in volcanic activity near ~2 Ga. The high-titanium basaltic eruptions occurring during the last volcanic activity period can be explained by the three possible scenarios (1) the ilmenite-bearing cumulate rich layer in the core-mantle boundary formed after the mantle overturn, (2) the basaltic material layers beneath the lunar crust formed through upwelling magmas, and (3) ilmenite-bearing cumulate blocks remained in the upper mantle after the mantle overturn.

Noriyuki Kawasaki^a,b, Steven B. Simon^c, Lawrence Grossman^c,d, Naoya Sakamoto^e, Hisayoshi Yurimoto^b,a,e

Geochimica et Cosmochimica Acta (in Press) Link to Article [https://doi.org/10.1016/j.gca.2017.05.035]
^aInstitute of Space and Astronautical Science, Japan Aerospace Exploration Agency, Sagamihara 252-5210, Japan
^bDepartment of Natural History Sciences, Hokkaido University, Sapporo 060-0810, Japan
^cDepartment of Geophysical Sciences, The University of Chicago, 5734 S. Ellis Ave., Chicago, Illinois 60637, USA
^dThe Enrico Fermi Institute, The University of Chicago, 5640 S. Ellis Ave., Chicago, Illinois 60637, USA
^eIsotope Imaging Laboratory, Creative Research Institution, Hokkaido University, Sapporo 001-0021, Japan
Copyright Elsevier

Toni Schulz^a, Christian Koeberl^a,b, Ambre Luguet^c, David Van Acken^c,d, Tanja Mohr-Westheide^e,f, Seda Ozdemir^a, Wolf Uwe Reimold^e,g,h

Geochimica et Cosmochimica Acta (in Press) Link to Article [https://doi.org/10.1016/j.gca.2017.05.040]
^aDepartment of Lithospheric Research, University Vienna, Althanstrasse 14, 1090 Vienna, Austria
^bNatural History Museum, Burgring 7, A-1010 Vienna, Austria
^cSteinmann-Institut of Geology, Mineralogy and Palaeontology, University of Bonn, Poppelsdorfer Schloss, 53115 Bonn, Germany
^dIrish Centre for Research in Applied Geosciences (iCRAG), University College Dublin, Belfield, Dublin 4, Ireland
^eMuseum für Naturkunde, Leibniz Institute for Evolution and Biodiversity Science, Invalidenstrasse 43, 10115 Berlin, Germany
^fFreie Universität Berlin (FU Berlin), Institut für Geologische Wissenschaften, Malteserstrasse 74-100, 12249 Berlin, Germany
^gHumboldt Universität zu Berlin, Unter den Linden 6, 10099 Berlin, Germany
^hGeochronology Laboratory, University of Brasília, Brazil
Copyright Elsevier

E.S. Steenstra^a, A.B. Sitabi^a, Y.H. Lin^a, N. Rai^b,c, J.S. Knibbe^a, J. Berndt^d, S. Matveev^e, W. van Westrenen^a

Geochimica et Cosmochimica Acta (in Press) Link to Article [https://doi.org/10.1016/j.gca.2017.05.034]
^aFaculty of Earth and Life Sciences, VU University Amsterdam, Amsterdam, The Netherlands
^bCentre for Planetary Sciences, Birkbeck University of London, London, UK
^cDepartment of Earth Sciences, Mineral and Planetary Sciences Division, Natural History Museum, London, UK
^dDepartment of Mineralogy, University of Münster, Germany
^eDepartment of Petrology, Utrecht University, The Netherlands
Copyright Elsevier

Franz A. Weis^a,b, Jeremy J. Bellucci^a, Henrik Skogby^a, Roland Stalder^c, Alexander A. Nemchin^a,d, Martin J. Whitehouse^a

Geochimica et Cosmochimica Acta (in Press) Link to Article [https://doi.org/10.1016/j.gca.2017.05.041]
^aSwedish Museum of Natural History, Dept. of Geosciences, Box 50007, SE-104 05 Stockholm, Sweden
^bUppsala University, Dept. of Earth Sciences, Center of Experimental Mineralogy, Petrology and Geochemistry (CEMPEG), SE-752 36 Uppsala, Sweden
^cInnsbruck University, Inst. for Mineralogy and Petrography, A-6020 Innsbruck, Austria
^dCurtin University, Dept. of Applied Geology, Perth, WA 6845, Australia
Copyright Elsevier