Structure-Magnetism Correlations and Chemical Order-Disorder Transformations in Ferrous L10-Structured Compounds

Total Page:16

File Type:pdf, Size:1020Kb

Structure-Magnetism Correlations and Chemical Order-Disorder Transformations in Ferrous L10-Structured Compounds STRUCTURE-MAGNETISM CORRELATIONS AND CHEMICAL ORDER-DISORDER TRANSFORMATIONS IN FERROUS L10-STRUCTURED COMPOUNDS A Dissertation Presented By Nina Cathryn Bordeaux to The Department of Chemical Engineering in partial fulfillment of the requirements for the degree of Doctor of Philosophy in the field of Chemical Engineering Northeastern University Boston, Massachusetts April 15, 2015 ACKNOWLEDGMENTS There are so many people I am grateful to for getting me to this point. First and foremost, I would like to thank my advisor, Professor Laura H. Lewis for taking me on and teaching me so much. You’ve challenged me to “ask the right questions” and I am a better scientist for it. Thank you for believing in me and for all of the ways you’ve gone beyond the expected for me, from taking me to the Taj Mahal to attending my wedding! Many thanks to my committee members, Professor Sunho Choi, Professor Teiichi Ando, and Professor Katayun Barmak, for taking the time to read my Dissertation and to serve on my committee. Thanks to Dr. Ando for teaching such a wonderful kinetics course that provided me with the foundational knowledge for much of this Dissertation. Special thanks to Dr. Barmak for being a collaborator in this research and for all of the time you’ve invested in discussing results and analysis methods. Thank you for your patience and your guidance. I want to thank Professor Joseph Goldstein for serving on my proposal committee. You provided invaluable guidance in this project and I am so grateful for all that you taught me about meteorites and scientific research. Thank you to Dr. Peter Stephens and Dr. Jean Jordan-Sweet at the NSLS for all of their help with synchrotron experiments. To all of my labmates, thank you for your comradery and commiseration. Thank you to Felix, Radhika, Melissa, Pegah, Luke, Ana, Ian, and Mahboobeh. You’ve been so great to work with! Thank you Luke for helping to get me to the finish line. Special acknowledgement goes to Radhika, who has been a great friend to me and a source of support since the beginning. Many thanks to Ana for long talks on FeNi and L10, afternoon coffee and chocolate breaks, and always being willing to lend an ear. I need to thank my husband, Eric Mueller, for loving and supporting me, especially through the Dissertation writing process. I love you. Most importantly, thanks to my mom, Margaret Ho, for being my role model. You’ve exemplified strength, independence, and intelligence. Thank you for encouraging me to pursue a career in engineering. Everything I’ve accomplished is because of you. Lastly, thank you to Northeastern University, especially for the Dissertation Completion Fellowship that has enabled me to finish this work. ii ABSTRACT Understanding chemical order-disorder transformations and their effects on structure and magnetic properties of ferrous L10 intermetallic systems has been a longstanding problem in materials science and solid state chemistry. Herein, the kinetics of ordering and disordering of the L10 structure in the FePd and FeNi systems are explored in correlation with their structure and magnetic properties. In many systems, the chemically ordered L10 structure forms through an ordering transformation from a chemically disordered parent phase, which is often a face-centered cubic (fcc, A1) solid solution of the two elements (see unit cells of both structures in Figure 1). L10 FeNi (a.k.a. tetrataenite) is only found naturally in meteorites that form over 4.5 billion years; to date, it has not been produced in bulk by laboratory methods. The challenge for manufacturing L10 FeNi is that it has a critical temperature of 320 °C, below which the fcc chemically disordered phase transforms into the L10 chemically ordered phase [1]. Below this critical temperature, the atomic mobilities of Fe and Ni are extremely low (1 atomic jump per 2,600 years [2]) therefore the atomic movement necessary for chemical ordering is limited. On the other hand, the L10 structure forms readily in FePd making it a useful model system in which to study the order-disorder transformation [3] (it is noted, however, that the high cost of palladium makes FePd an impractical material for bulk industrial applications). In this dissertation, laboratory-synthesized L10 FePd was used as a test-bed system while a variety of meteorites were used as natural sources of L10- structured FeNi. The effect of the cooling rate on the A1→L10 chemical ordering transformation in FePd is investigated to elucidate the mechanism of chemical ordering. The effect of the heating rate on the L10→A1 chemical disordering transformation in iii FeNi is investigated to gain understanding of the phase’s stability and order-disorder transformation mechanism. Analysis of the magnetic properties of L10 FeNi and L10 FePd indicates that the materials have theoretical magnetic energy products comparable to those of today’s best permanent magnets; thus, results from this work may aid future synthesis efforts for advanced permanent magnet applications. L1 structure A1 structure 0 Figure 1: Unit cells of binary alloy AB with (a) the chemically disordered fcc (A1) structure and (b) the chemically ordered L10 structure. iv TABLE OF CONTENTS 1 Introduction ...................................................................................................... 1 1.1 Motivation ................................................................................................. 1 1.2 Overview of Research ............................................................................... 3 1.3 Organization of Dissertation ..................................................................... 6 2 Formalism and Critical Literature Review ....................................................... 8 2.1 General Overview of Phase Transformations ........................................... 9 2.1.1 Thermodynamics of Phase Transformations ....................................... 9 2.1.2 Kinetics of Structural Phase Transformations ................................... 17 2.2 Order-Disorder Transformations ............................................................. 26 2.2.1 Chemical Order and Disorder ........................................................... 26 2.2.2 Magnetic Phase Transitions .............................................................. 30 2.3 Critical Literature Review ....................................................................... 39 2.3.1 Overview of L10 FePd ....................................................................... 39 2.3.2 Overview of L10 FeNi (Tetrataenite)................................................. 47 3 Experimental Methods and Techniques ......................................................... 55 3.1 FePd Synthesis and Processing ............................................................... 55 3.2 Meteorite Sample Preparation ................................................................. 56 3.3 Composition and Homogeneity Determination Using Scanning Electron Microscope Energy-Dispersive X-ray Spectroscopy (SEM-EDS) ........... 57 3.4 Characterization of Microstructure and Structure Using Optical Microscopy and X-ray Diffraction (XRD) ............................................... 59 3.5 Methods of Magnetic Domain and Bulk Magnetism Characterization... 66 3.5.1 Magnetic Domain Characterization Using Magnetic Force Microscopy (MFM) ........................................................................... 66 3.5.2 Bulk Magnetic Characterization Using Vibrating Sample Magnetometry (VSM) ....................................................................... 68 3.6 Calorimetric Methods .............................................................................. 71 4 FePd Results and Discussion .......................................................................... 73 4.1 Characterization of the Structure, Magnetism, and Thermal Stability of L10 FePd.................................................................................................... 74 4.1.1 Results from the Characterization of Structure, Magnetism, and Thermal Stability of L10 FePd .......................................................... 76 v 4.1.2 Discussion from the Characterization of Structure, Magnetism, and Thermal Stability of L10 FePd .......................................................... 83 4.1.3 Significance of Work from the Characterization of Structure, Magnetism, and Thermal Stability of L10 FePd ................................ 89 4.2 The Effect of Cooling Rate on the A1→L10 Chemical Ordering Transformation in FePd ............................................................................ 90 4.2.1 Results from the Effect of Cooling Rate on the A1→L10 Chemical Ordering Transformation in FePd ..................................................... 91 4.2.2 Discussion from the Effect of Cooling Rate on the A1→L10 Chemical Ordering Transformation in FePd ................................... 101 4.2.3 Significance of Work from the Effect of Cooling Rate on the A1→L10 Chemical Ordering Transformation in FePd ................... 120 5 FeNi Results and Discussion ........................................................................ 123 5.1 Correlations of Structure and Magnetism of L10 FeNi ......................... 123 5.1.1 Results on the Correlations of Structure and Magnetism of L10 FeNi.. ......................................................................................................... 124 5.1.2 Discussion on the Correlations of Structure and Magnetism of L10 FeNi ................................................................................................
Recommended publications
  • Podiform Chromite Deposits—Database and Grade and Tonnage Models
    Podiform Chromite Deposits—Database and Grade and Tonnage Models Scientific Investigations Report 2012–5157 U.S. Department of the Interior U.S. Geological Survey COVER View of the abandoned Chrome Concentrating Company mill, opened in 1917, near the No. 5 chromite mine in Del Puerto Canyon, Stanislaus County, California (USGS photograph by Dan Mosier, 1972). Insets show (upper right) specimen of massive chromite ore from the Pillikin mine, El Dorado County, California, and (lower left) specimen showing disseminated layers of chromite in dunite from the No. 5 mine, Stanislaus County, California (USGS photographs by Dan Mosier, 2012). Podiform Chromite Deposits—Database and Grade and Tonnage Models By Dan L. Mosier, Donald A. Singer, Barry C. Moring, and John P. Galloway Scientific Investigations Report 2012-5157 U.S. Department of the Interior U.S. Geological Survey U.S. Department of the Interior KEN SALAZAR, Secretary U.S. Geological Survey Marcia K. McNutt, Director U.S. Geological Survey, Reston, Virginia: 2012 This report and any updates to it are available online at: http://pubs.usgs.gov/sir/2012/5157/ For more information on the USGS—the Federal source for science about the Earth, its natural and living resources, natural hazards, and the environment—visit http://www.usgs.gov or call 1–888–ASK–USGS For an overview of USGS information products, including maps, imagery, and publications, visit http://www.usgs.gov/pubprod To order this and other USGS information products, visit http://store.usgs.gov Suggested citation: Mosier, D.L., Singer, D.A., Moring, B.C., and Galloway, J.P., 2012, Podiform chromite deposits—database and grade and tonnage models: U.S.
    [Show full text]
  • A New Occurrence of Terrestrial Native Iron in the Earth's Surface
    geosciences Article A New Occurrence of Terrestrial Native Iron in the Earth’s Surface: The Ilia Thermogenic Travertine Case, Northwestern Euboea, Greece Christos Kanellopoulos 1,2,* ID , Eugenia Valsami-Jones 3,4, Panagiotis Voudouris 1, Christina Stouraiti 1 ID , Robert Moritz 2, Constantinos Mavrogonatos 1 ID and Panagiotis Mitropoulos 1,† 1 Department of Geology and Geoenvironment, National and Kapodistrian University of Athens, Panepistimioupolis Zografou, 15784 Athens, Greece; [email protected] (P.V.); [email protected] (C.S.); [email protected] (C.M.); [email protected] (P.M.) 2 Section of Earth and Environmental Sciences, University of Geneva, Rue des Maraichers 13, 1205 Geneva, Switzerland; [email protected] 3 School of Geography, Earth & Environmental Sciences, University of Birmingham, Edgbaston, Birmingham B15 2TT, UK; [email protected] 4 Department of Earth Sciences, Natural History Museum London, Cromwell Road, London SW7 5BD, UK * Correspondence: [email protected] † Professor Panagiotis Mitropoulos has passed away in 2017. Received: 6 April 2018; Accepted: 23 July 2018; Published: 31 July 2018 Abstract: Native iron has been identified in an active thermogenic travertine deposit, located at Ilia area (Euboea Island, Greece). The deposit is forming around a hot spring, which is part of a large active metallogenetic hydrothermal system depositing ore-bearing travertines. The native iron occurs in two shapes: nodules with diameter 0.4 and 0.45 cm, and angular grains with length up to tens of µm. The travertine laminae around the spherical/ovoid nodules grow smoothly, and the angular grains are trapped inside the pores of the travertine.
    [Show full text]
  • Heazlewooditeand Awaruite in Serpentinites of The
    HEAZLEWOODITEANDAWARUITE IN SERPENTINITESOF THE EASTERN TOWNSHIPS,QUEBEC J. A. CnaUBERLATN Geological,Suraey of Canail,a,Ottawa Awaruite of composition approximately NiaFe was shown by Nickel (1959) to be a common accessory phase in most serpentinites of the asbestos-producing belt in the Eastern Townships, Quebec. Nickel demonstrated that awaruite developed during the serpentinization process from nickel and iron already present in these rocks. Work on the distribution and genesis of native metals in the Muskox intrusion (Chamberlain, et aI, 1965) indicated that native metals could form by the decomposition of earlier-formed sulphides. For example, pentlandite was shown to decomposeto form avraruite plus iron sulphide, and chalcopyrite to native copper plus pyrrhotite. Some native iron may have been formed by the reduction of magnetite. Such reactions suggested that awaruite in the Eastern Townships could also have been formed by the decomposition of primary sulphides. This theory was checked by examination of 44 polished sections made from samples donated by A. S. Maclaren of the Geological Survey, and from samples collected during the 1965 field season*. The observed distribution of awaruite, heazle- woodite and magnetite in these sections is summarized in Table 1. Magnetite is present in g4 per cent of the sections in amounts exceeding 0.1 per cent. Most sections contain 1 per cent or more. It occurs as threads between ghost olivine or pyroxene crystals, as discrete, weakly euhedral grains, or as rims around primary chromite crystals. It is invariably in contact with serpentine. Magnetite is believed to have formed by reaction of magnesium-iron olivine or pyroxene with water to give magnesium serpentine plus magnetite at temperatures below 550o C.
    [Show full text]
  • Washington State Minerals Checklist
    Division of Geology and Earth Resources MS 47007; Olympia, WA 98504-7007 Washington State 360-902-1450; 360-902-1785 fax E-mail: [email protected] Website: http://www.dnr.wa.gov/geology Minerals Checklist Note: Mineral names in parentheses are the preferred species names. Compiled by Raymond Lasmanis o Acanthite o Arsenopalladinite o Bustamite o Clinohumite o Enstatite o Harmotome o Actinolite o Arsenopyrite o Bytownite o Clinoptilolite o Epidesmine (Stilbite) o Hastingsite o Adularia o Arsenosulvanite (Plagioclase) o Clinozoisite o Epidote o Hausmannite (Orthoclase) o Arsenpolybasite o Cairngorm (Quartz) o Cobaltite o Epistilbite o Hedenbergite o Aegirine o Astrophyllite o Calamine o Cochromite o Epsomite o Hedleyite o Aenigmatite o Atacamite (Hemimorphite) o Coffinite o Erionite o Hematite o Aeschynite o Atokite o Calaverite o Columbite o Erythrite o Hemimorphite o Agardite-Y o Augite o Calciohilairite (Ferrocolumbite) o Euchroite o Hercynite o Agate (Quartz) o Aurostibite o Calcite, see also o Conichalcite o Euxenite o Hessite o Aguilarite o Austinite Manganocalcite o Connellite o Euxenite-Y o Heulandite o Aktashite o Onyx o Copiapite o o Autunite o Fairchildite Hexahydrite o Alabandite o Caledonite o Copper o o Awaruite o Famatinite Hibschite o Albite o Cancrinite o Copper-zinc o o Axinite group o Fayalite Hillebrandite o Algodonite o Carnelian (Quartz) o Coquandite o o Azurite o Feldspar group Hisingerite o Allanite o Cassiterite o Cordierite o o Barite o Ferberite Hongshiite o Allanite-Ce o Catapleiite o Corrensite o o Bastnäsite
    [Show full text]
  • Nanomagnetic Properties of the Meteorite Cloudy Zone
    Nanomagnetic properties of the meteorite cloudy zone Joshua F. Einslea,b,1, Alexander S. Eggemanc, Ben H. Martineaub, Zineb Saghid, Sean M. Collinsb, Roberts Blukisa, Paul A. J. Bagote, Paul A. Midgleyb, and Richard J. Harrisona aDepartment of Earth Sciences, University of Cambridge, Cambridge, CB2 3EQ, United Kingdom; bDepartment of Materials Science and Metallurgy, University of Cambridge, Cambridge, CB3 0FS, United Kingdom; cSchool of Materials, University of Manchester, Manchester, M13 9PL, United Kingdom; dCommissariat a` l’Energie Atomique et aux Energies Alternatives, Laboratoire d’electronique´ des Technologies de l’Information, MINATEC Campus, Grenoble, F-38054, France; and eDepartment of Materials, University of Oxford, Oxford, OX1 3PH, United Kingdom Edited by Lisa Tauxe, University of California, San Diego, La Jolla, CA, and approved October 3, 2018 (received for review June 1, 2018) Meteorites contain a record of their thermal and magnetic history, field, it has been proposed that the cloudy zone preserves a written in the intergrowths of iron-rich and nickel-rich phases record of the field’s intensity and polarity (5, 6). The ability that formed during slow cooling. Of intense interest from a mag- to extract this paleomagnetic information only recently became netic perspective is the “cloudy zone,” a nanoscale intergrowth possible with the advent of high-resolution X-ray magnetic imag- containing tetrataenite—a naturally occurring hard ferromagnetic ing methods, which are capable of quantifying the magnetic state mineral that
    [Show full text]
  • Sulfide Dissolution and Awaruite Formation in 10.1029/2021JB021758 Continental Serpentinization Environments and Its
    RESEARCH ARTICLE Sulfide Dissolution and Awaruite Formation in 10.1029/2021JB021758 Continental Serpentinization Environments and Its Special Section: Implications to Supporting Life Ophiolites and Oceanic Lith- 1 1 1 1 1 osphere, with a focus on the E. M. Schwarzenbach , J. C. Vrijmoed , J. M. Engelmann , M. Liesegang , U. Wiechert , Samail ophiolite in Oman R. Rohne1, and O. Plümper2 1 2 Key Points: Institute of Geological Sciences, Freie Universität Berlin, Berlin, Germany, Department of Earth Sciences, Utrecht • High disequilibrium conditions University, Utrecht, The Netherlands induce skeletal awaruite growth during continental serpentinization • Pentlandite dissolution creates fluid Abstract Serpentinization environments are key locations that support microbial communities by pathways and nutrients for microbial the abiogenic formation of reduced species associated with peridotite alteration. Here we studied partially life • Sulfur isotope compositions serpentinized peridotites from the Chimaera seeps (Turkey), an active continental serpentinization system document ocean floor and that vents highly methane-rich fluids, to investigate the impact of water-rock interaction on the sulfide subsequent continental and metal mineralogy and its implications on supporting microbial communities. Using high-resolution serpentinization processes scanning electron microscopy, electron microprobe analysis, and transmission electron microscopy we found diverse pentlandite decomposition features with precipitation of secondary sulfides including Supporting Information: millerite, heazlewoodite, as well as Cu-bearing sulfides, native Cu, and awaruite (Ni3Fe). Awaruite forms Supporting Information may be found in the online version of this article. dense veinlets to single crystal platelets tens of nanometers in size, which is formed by desulphurization of pentlandite. In addition, the nanometer-sized awaruite platelets are intimately intergrown with serpentine suggesting its growth during peridotite alteration by a dissolution-precipitation process, Correspondence to: E.
    [Show full text]
  • Occurrence of Graphite-Like Carbon in Podiform Chromitites of Greece and Its Genetic Significance
    minerals Article Occurrence of Graphite-Like Carbon in Podiform Chromitites of Greece and Its Genetic Significance Maria Economou-Eliopoulos *, George Tsoupas and Vasilis Skounakis Department of Geology and Geoenvironment, University of Athens, Athens 15784, Greece; [email protected] (G.T.); [email protected] (V.S.) * Correspondence: [email protected]; Tel.: +30-2107274214 Received: 21 December 2018; Accepted: 26 February 2019; Published: 3 March 2019 Abstract: The role of post-magmatic processes in the composition of chromitites hosted in ophiolite complexes, the origin of super-reduced phases, and factors controlling the carbon recycling in a supra-subduction zone environment are still unclear. The present contribution compiles the first scanning electron microscope/energy-dispersive (SEM/EDS) data on graphite-like amorphous carbon, with geochemical and mineral chemistry data, from chromitites of the Skyros, Othrys, Pindos, and Veria ophiolites (Greece). The aim of this study was the delineation of potential relationships between the modified composition of chromite and the role of redox conditions, during the long-term evolution of chromitites in a supra-subduction zone environment. Chromitites are characterized by a strong brittle (cataclastic) texture and the presence of phases indicative of super-reducing phases, such as Fe–Ni–Cr-alloys, awaruite (Ni3Fe), and heazlewoodite (Ni3S2). Carbon-bearing assemblages are better revealed on Au-coated unpolished sections. Graphite occurs in association with hydrous silicates (chlorite, serpentine) and Fe2+-chromite, as inclusions in chromite, filling cracks within chromite, or as nodule-like graphite aggregates. X-ray spectra of graphite–silicate aggregates showed the presence of C, Si, Mg, Al, O in variable proportions, and occasionally K and Ca.
    [Show full text]
  • Cais CAI AOA AOA AOA
    50th Lunar and Planetary Science Conference 2019 (LPI Contrib. No. 2132) 1033.pdf THE FORMATION CONDITIONS OF CHONDRITES: INSIGHTS FROM NORTHWEST AFRICA 10850 – AN OXIDIZED CV3 CHONDRITE. M. M. Jean1,2, A. Patchen1, M. B. Sueilem3, L. A. Taylor1, 1Planetary Ge- osciences Institute, Dept. Earth and Planetary Sciences, University of Tennessee Knoxville. 2University of Alaska- Anchorage, Dept. of Geological Sciences, Anchorage, AK 99508. 3Smara Refugee Camps of Western Sahara, Tin- douf, Algeria. ([email protected]) Introduction: For the first time, data are presented lected from Algeria, in the Tindouf province. Approx- from a detailed investigation of all components of the imately 50.3 g were recovered on August 2015, and Northwest Africa (NWA) 10850 carbonaceous chon- acquired by us shortly thereafter. Its classification as a drite. NWA 10850 is a newly classified meteorite col- carbonaceous chondrite was recently approved [1]. chondrules matrix chondrule matrix AOA chondrule CAI AOA matrix CAIs matrix AOA chondrules matrix AOA 2 mm Figure 1. Combined Mg Kα (blue) + Al Kα (green) + Ca Kα (red) X-ray maps showing chondrules, CAIs (cal- cium-aluminum inclusions), amoeboidal olivine aggregates (AOA), and other features found in NWA 10850 50th Lunar and Planetary Science Conference 2019 (LPI Contrib. No. 2132) 1033.pdf We have undertaken a comprehensive study to pro- Di Hd vide an overview of the petrography and geochemistry of this meteorite. Based on these results, we add NWA 10850 to the Allende-like subgroup (CV3oxA), which typically contains approximately 40 vol % matrix ma- terial (with little phyllosilicate), 40–50 vol % intact En Fs chondrules, and ~ 0.2 vol % metallic FeNi.
    [Show full text]
  • Highly Reducing Conditions During Alpine Metamorphism of The
    Contrib Mineral Petrol (1992) 112:329-340 Contributions to Mineralogy and Petrology 9 Springer-Verlag 1992 Highly reducing conditions during Alpine metamorphism of the Malenco peridotite (Sondrio, northern Italy) indicated by mineral paragenesis and H 2 in fluid inclusions Adolf Peretti 1 *, Jean Dubessy 2, Josef Mnllis 3, B. Ronald Frost 4, and V. Trommsdorff 5 1 Institut ffir Mineralogie und Petrographie, ETH, Sonneggstrasse 5, CH-8092 Zurich, Switzerland 2 CREGU, GS CNRS 077, BP 23, F-54501 Vandoeuvre-Les-Nancy Cedex, France 3 Mineralogisch Petrographisches Institut der Universit/it, Bernoullistrasse 30, CH-4056 Basel, Switzerland 4 Department of Geology and Geophysics, University of Wyoming, Laramie, WY 82071, USA 5 Institut fiir Mineralogie und Petrographie, ETH, Sonneggstrasse 5, CH-8092 Zurich, Switzerland Received April 12, 1991 / Accepted June 19, 1992 Abstract. During regional metamorphism of the Malen- has evidenced mineral parageneses (formation of awar- co serpentinized peridotite (Sondrio, northern Italy), the uite) indicative of highly reducing conditions during the mineral assemblage pentlandite-awaruite-magnetite-na- prograde alpine metamorphism. The aim of this study tive copper-antigorite-brucite-olivine-diopside is formed. is to obtain information about the prograde metamor- The opaque assemblage indicates very reduced fluids phic fluids at the site of dehydration reactions of serpen- with fO2 values 4 log units below QFM. Primary fluid tinite (olivine-in isograd) and the contemperaneous for- inclusions were trapped in diopside overgrowth, contem- mation of awaruite. poraneous with the opaque assemblage. These metamor- phic fluids are saline aqueous solutions (about 10.4 mol% NaC1 equivalent) and contain molecular H2 Geological setting of approximately 1 mol%, as shown by micro-Raman analysis and microthermometry.
    [Show full text]
  • Crystal-Structure of a Natural Nickel-Iron Alloy. by Professor E
    415 Crystal-structure of a natural nickel-iron alloy. By Professor E. A. OWEN, M.A., Sc.D., and B. D. BURNS, M.Sc. University College of North Wales, Bangor. [Read June 8, 1939 ; communicated by the editor.] 1. Introduction. ATU,RAL nickel-iron alloys have been found in several places on the N earth s surface. In addition to alloys containing a low percentage of nickel (about 3%), there are others which contain much higher per- centages of nickel (about 70o/o). To alloys of the latter group the name awaruite is now generally given and it may include josephinite, souesite, and other alloys possessing high nickel content so long as they belong to the same phase and possess identical crystal-structures. It is of interest to the mineralogist to know whether these alloys con- form to the structure of nickel-iron alloys prepared in the laboratory and whether they fit into the accepted phase diagram of the nickel-iron system. It is of interest also to the physicist and the metallurgist to obtain information concerning these natural alloys, because some nickel- iron alloys made in the laboratory are difficult to prepare in a state of true equilibrium. Data derived from the study of the natural alloys may help to throw light upon the structure of these artificial alloys. 2. Previous Work on Natural Nickel-iron Alloys. Several investigations of natural nickel-iron alloys have been de- scribed. W. H. MelvillO records the examination of magnetic pebbles discovered in large quantities in the gravel of a stream in Josephine and Jackson Counties in Oregon.
    [Show full text]
  • Eliopoulosite, V7S8, a New Sulfide from the Podiform Chromitite of The
    minerals Article Eliopoulosite, V7S8, A New Sulfide from the Podiform Chromitite of the Othrys Ophiolite, Greece Luca Bindi 1,* , Federica Zaccarini 2, Paola Bonazzi 1, Tassos Grammatikopoulos 3, Basilios Tsikouras 4 , Chris Stanley 5 and Giorgio Garuti 2 1 Dipartimento di Scienze della Terra, Università degli Studi di Firenze, I-50121 Florence, Italy; paola.bonazzi@unifi.it 2 Department of Applied Geological Sciences and Geophysics, University of Leoben, A-8700 Leoben, Austria; [email protected] (F.Z.); [email protected] (G.G.) 3 SGS Canada Inc., 185 Concession Street, PO 4300, Lakefield, ON K0L 2H0, Canada; [email protected] 4 Faculty of Science, Physical and Geological Sciences, Universiti Brunei Darussalam, BE 1410 Gadong, Brunei Darussalam; [email protected] 5 Department of Earth Sciences, Natural History Museum, London SW7 5BD, UK; [email protected] * Correspondence: luca.bindi@unifi.it; Tel.: +39-055-275-7532 Received: 22 February 2020; Accepted: 6 March 2020; Published: 8 March 2020 Abstract: The new mineral species, eliopoulosite, V7S8, was discovered in the abandoned chromium mine of Agios Stefanos of the Othrys ophiolite, located in central Greece. The investigated samples consist of massive chromitite hosted in a strongly altered mantle tectonite, and are associated with nickelphosphide, awaruite, tsikourasite, and grammatikopoulosite. Eliopoulosite is brittle and has a metallic luster. In plane-reflected polarized light, it is grayish-brown and shows no internal reflections, bireflectance, and pleochroism. It is weakly anisotropic, with colors varying from light to dark greenish. Reflectance values of mineral in air (Ro, Re’ in %) are: 34.8–35.7 at 470 nm, 38–39 at 546 nm, 40–41.3 at 589 nm, and 42.5–44.2 at 650 nm.
    [Show full text]
  • Occurrence, Formation and Destruction of Magnetite in Chondritic Meteorites
    51st Lunar and Planetary Science Conference (2020) 1092.pdf OCCURRENCE, FORMATION AND DESTRUCTION OF MAGNETITE IN CHONDRITIC METEORITES. Alan E. Rubin1 and Ye Li2, 1Dept. Earth, Planet. Space Sci., UCLA, Los Angeles, CA 90095-1567, USA. 2Key Lab. Planet. Sci., Purple Mount. Observ., Chinese Academy of Sciences, Nanjing, 210034, China. Occurrence: Magnetite with low Cr2O3 is present in chondritic asteroids. CO3.1 chondrites also contain aqueously altered carbonaceous chondrites (CI1, veins of fayalite as well as fayalitic overgrowths on CM2.0-2.2, CR1, CV3OxA, CV3OxB, CO3.00-3.1) [1-6], magnesian olivine grains; these occurrences of ferroan type 3.00-3.4 ordinary chondrites [7,8] and type 3.5 R olivine are alteration products (as is magnetite). chondrites [9]. Magnetite in CI Orgueil averages 0.04 Carbide-magnetite assemblages may have formed wt.% Cr2O3 [10]; magnetite in CO3 chondrites averages from metallic Fe by a C-O-H-bearing fluid in a process 0.27 wt.% Cr2O3 [11]; magnetite in LL3.00 Semarkona involving carbidization by CO(g) and oxidation by is nearly pure Fe3O4 (with ~0.1 wt.% Co) [7]. Magnetite H2O(g) [8]. Textural evidence indicates that magnetite is rare to absent in less-altered, more-metamorphosed also replaces iron carbide and troilite in type-3 OC [8]. CM, CR, CO, OC and R chondrites; in addition, mag- This is consistent with the apparent replacement of pyr- netite is rare in CV3Red chondrites and less abundant in rhotite by framboidal magnetite in CM chondrites [22] type-3.6 Allende (CVOxA) than in type-3.1 Kaba and in the Kaidun ungrouped polymict carbonaceous (CVOxB).
    [Show full text]