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A Review of the Structural Architecture of Tellurium Oxycompounds
Mineralogical Magazine, May 2016, Vol. 80(3), pp. 415–545 REVIEW OPEN ACCESS A review of the structural architecture of tellurium oxycompounds 1 2,* 3 A. G. CHRISTY ,S.J.MILLS AND A. R. KAMPF 1 Research School of Earth Sciences and Department of Applied Mathematics, Research School of Physics and Engineering, Australian National University, Canberra, ACT 2601, Australia 2 Geosciences, Museum Victoria, GPO Box 666, Melbourne, Victoria 3001, Australia 3 Mineral Sciences Department, Natural History Museum of Los Angeles County, 900 Exposition Boulevard, Los Angeles, CA 90007, USA [Received 24 November 2015; Accepted 23 February 2016; Associate Editor: Mark Welch] ABSTRACT Relative to its extremely low abundance in the Earth’s crust, tellurium is the most mineralogically diverse chemical element, with over 160 mineral species known that contain essential Te, many of them with unique crystal structures. We review the crystal structures of 703 tellurium oxysalts for which good refinements exist, including 55 that are known to occur as minerals. The dataset is restricted to compounds where oxygen is the only ligand that is strongly bound to Te, but most of the Periodic Table is represented in the compounds that are reviewed. The dataset contains 375 structures that contain only Te4+ cations and 302 with only Te6+, with 26 of the compounds containing Te in both valence states. Te6+ was almost exclusively in rather regular octahedral coordination by oxygen ligands, with only two instances each of 4- and 5-coordination. Conversely, the lone-pair cation Te4+ displayed irregular coordination, with a broad range of coordination numbers and bond distances. -
By Michael Fleischer and Constance M. Schafer Open-File Report 81
U.S. DEPARTMENT OF THE INTERIOR GEOLOGICAL SURVEY THE FORD-FLEISCHER FILE OF MINERALOGICAL REFERENCES, 1978-1980 INCLUSIVE by Michael Fleischer and Constance M. Schafer Open-File Report 81-1174 This report is preliminary and has not been reviewed for conformity with U.S. Geological Survey editorial standards 1981 The Ford-Fleischer File of Mineralogical References 1978-1980 Inclusive by Michael Fleischer and Constance M. Schafer In 1916, Prof. W.E. Ford of Yale University, having just published the third Appendix to Dana's System of Mineralogy, 6th Edition, began to plan for the 7th Edition. He decided to create a file, with a separate folder for each mineral (or for each mineral group) into which he would place a citation to any paper that seemed to contain data that should be considered in the revision of the 6th Edition. He maintained the file in duplicate, with one copy going to Harvard University, when it was agreed in the early 1930's that Palache, Berman, and Fronde! there would have the main burden of the revision. A number of assistants were hired for the project, including C.W. Wolfe and M.A. Peacock to gather crystallographic data at Harvard, and Michael Fleischer to collect and evaluate chemical data at Yale. After Prof. Ford's death in March 1939, the second set of his files came to the U.S. Geological Survey and the literature has been covered since then by Michael Fleischer. Copies are now at the U.S. Geological Survey at Reston, Va., Denver, Colo., and Menlo Park, Cal., and at the U.S. -
Cambridge University Press 978-1-107-10626-0 — Minerals 2Nd Edition Index More Information
Cambridge University Press 978-1-107-10626-0 — Minerals 2nd Edition Index More Information Index Bold entries are mineral names. Page numbers in bold refer to minerals with detailed descriptions. Page numbers in italics refer to pictures. Abbe refractometer, 170, 191 American Mineralogist Crystal Structure Database, 143 aberrations in lenses, 172 amethyst, 50, 308, Plate 2c absorption, 217 amosite, 529 absorption of light, 186 optical micrograph, 532 absorption spectra, supernovae, 537 TEM image, 532 abundance of elements, 16 amphibole, 445 acetic acid, structure, 474 extinction angle, 212 acetone, structure, 474 minerals and composition, 439 acid mine drainage, 533 optical orientation, 211 actinolite, 449, 529 optical properties, 209 acute bisectrix, 199 quadrilateral, 444 adularia, 309 structure, 438 from Alps, Plate 21a amphibolite facies, 415 African Copper Belt, 374 analcime, 469 agate, 308 from Italy, SEM image, 465 aggregate, 518 analyzer, 173, 176 aggregation, 127 anatase, 392 of crystals, 127 from Swiss Alps, Plate 28d Agricola, 5, 481 structure and symmetry, 104 Airy’s spiral, 202 andalusite, 408 Al2SiO5, phase diagram, 276 optical orientation, 214 alabandite, 539 optical properties, 215 albite, 301, 310 porphyroblast, Plate 5c from New Mexico, Plate 21d andesine, 301 Albite twin law, 112, 311 anglesite, 355 Algoma-type iron deposits, 491 anhedral shape, 49 alite, 519 anhydrite, 355 alkali feldspars, 301, 309 animal nutrition, zeolites, 471 optical indicatrix, 205 aniom, 19 phase diagram, 306, 314 anisotropy, 149 alkali–silica -
Kunatite, Cufe (PO) (OR) °4R 0, a New Member of The
Kunatite, CuFe (PO) (OR) °4R 0, a new 2 4 2 2 2 member ofthe whitmoreite group, from Lake Boga, Victoria, Australia. Stuart J. Mills Department of Earth and Ocean Sciences, University of British Columbia, Vancouver Be, Canada, V6T 1Z4 email: [email protected] Uwe Kolitsch Mineralogisch-Petrographische Abteilung, Naturhistorisches Museum, Burgring 7, A-10lO, Wien, Austria William D. Birch Department of Geosciences, Museum Victoria, GPO Box 666, Melbourne, Victoria 3001, Australia Jifi Sejkora Department of Mineralogy and Petrology, National Museum, Vaclavske nam. 68, CZ-1l5 79 Praha 1, Czech Republic ABSTRACT Kunatite, CuFe2(P04)2(OH)2'4HP, (IMA 2007--(57), is a newly defined mineral from a quarry in Late Devonian granite near Lake Boga, northern Victoria, Australia. The mineral occurs as acicular to lath-like microcrystals forming compact to slightly open spheres, hemispheres and flattened sprays up to about 0.25 mm across, with individual fibrous crystals up to 30 flm long and 5 flm thick. Kunatite is associated only with chalcosiderite-turquoise. The crystals are yellow-green with a pale yellow streak and are transparent; the lustre of the aggregates is silky and the estimated Mohs hardness is 3. Kunatite is monoclinic, P2/c, with a = 9.863(10), b = 9.661(6), c = 5.476(6) A, ~ = 92.45(3)°, V = 521.3(3) A3 and Z = 2. The calculated density, based on the empirical formula, is 3.063 3 • = ~ = = = g/cm Crystals are biaxial (-), with a 1.703(3), 1.742(4) and y 1.762(3), and 2Vca1c 70°. Orientation: Z-c, with straight extinction and slight pleochroism: X = very pale yellow (almost colourless), Y = pale yellowish, Z = yellowish. -
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American Mineralogist, Volume 65, pages 599-623, 1980 Microstructures and reaction mechanismsin biopyriboles Devro R. VnnreN AND PETERR. BusEcK Departmentsof Geologysnd Chemistry,Arizona State University Tempe,Arizona 85281 Abstract High-resolution transmission electron microscopy of ferromagnesian chain and sheet sili- cates from a metamorphosed ultramafic body at Chester, Vermont has revealed a wide vari- ety of structural defects.Images of thesemicrostructures have been interpreted by analogy with images of ordered chain silicates and with the aid of dynamical diflraction and imaging calculations.Most of the defectsare concentratedin regionsof chain-width disorder;they ap- parently result from retrogradereaction ofanthophyllite to talc and from deformation of the ultramafic body. The most common defects are the terminations of (010) slabs having a given chain width. Theseslabs, referred to as "zippers," in most casesterminate coherently,with no displacive planar defects associated with the termination. Two theoretically-derived rules must be obeyedfor coherenttermination. Rule l: the terminating zipper must have the samenumber of subchains as the material it replaces.Rule 2: the numbers of silicate chains in the zipper and in the material it replacesmust both be even, or they must both be odd. Where these rules are disobeyed, zipper terminations are usually associatedwith planar faults having dis- placementsprojected on (001) of either % [010] or t/+[fi)], referred to an anthophyllite cell. In rare cases,violation of the replacement rules results in severestructural distortion, rather than the creation of displacive planar faults. These replacement rules hold for all pyriboles and may [s s6ahqlling factors not only in reactionsinvolving amFhib,ole,but in pyroxene hydration reactions as well. -
References Cited in the Database (Asbestos Sites.Xls)
References Cited in the Database (asbestos_sites.xls) Adams, J.H., 1870, Notice of asbestus and corundum with other minerals at Pelham, Mass.: American Journal of Science and Arts, v. 49, no. 146, p. 271-272. Allen, R.M., Jr., 1963, Geology and mineral resources of Greene and Madison Counties: Virginia Division of Mineral Resources Bulletin 78, 102 p., 1 plate, scale 1:62,500. Allen, R.M., Jr., 1967, Geology and mineral resources of Page County: Virginia Division of Mineral Resources Bulletin 81, 78 p., 1 plate, scale 1:62,500. Anonymous, 1944, Mad River talc mine, Washington County, Vt.: U.S. Bureau of Mines War Minerals Report 222, 22 p. Anonymous, 1970, World asbestos industry—United States: Industrial Minerals, no. 28 (January 1970), p. 22-23. Bain, G.W., 1942, Vermont talc and asbestos deposits, in Newhouse, W.H., ed., Ore deposits as related to structural features: Princeton, N.J., Princeton University Press, p. 255-258. Bangs, Herbert, 1946, Asbestos in Maryland: Baltimore, Md., Natural History Society of Maryland, Maryland Journal of Natural History, v. 16, no. 4, p. 67-73. Baum, J.L., 1962, The Franklin ore body, in Northern Field Excursion Guidebook, International Mineralogical Association, Third General Congress, Washington, D.C.: International Mineralogical Association, p. 19-21. Beard, M.E., Crankshaw, O.S., Ennis, J.T., and Moore, C.E., 2001, Analysis of crayons for asbestos and other fibrous materials, and recommendations for improved analytical definitions—Executive summary: Research Triangle Park, N.C., Research Triangle Institute, Center for Environmental Measurements and Quality Assurance, Earth and Mineral Sciences Department, [informal report], 8 p. -
New Mineral Names
American Mineralogist, Volume 80, pages 630-635, 1995 NEW MINERAL NAMES. JOHN L. JAMBOR Departmentof Earth Sciences,Universityof Waterloo,Waterloo,OntarioN2L 3Gl, Canada VLADIMIR A. KOVALENKER IGREM RAN, Russian Academy of Sciences, Moscow 10917, Staromonetnii 35, Russia ANDREW C. ROBERTS Geological Survey of Canada, 601 Booth Street, Ottawa, Ontario KIA OE8, Canada Briziite* Co and increased Ni content in conireite, the name allud- F. Olmi, C. Sabelli (1994) Briziite, NaSb03, a new min- ing to the principal cations Co-Ni-Fe. eral from the Cetine mine (Tuscany, Italy): Description Discussion. An unapproved name for an incompletely and crystal structure. Eur. Jour. MineraL, 6, 667-672. described mineral. J.L.J. The mineral occurs as light pink to yellow, compact aggregates of platy to thin tabular crystals that encrust Grossite* weathered waste material and slag at the Cetine antimony D. Weber, A Bischoff(1994) Grossite (CaAl.O,)-a rare (stibnite) mine near Siena, Tuscany, Italy. Electron mi- phase in terrestrial rocks and meteorites. Eur. Jour. croprobe analysis gave Na20 15.98, Sb20s 83.28 wt%, Mineral., 6,591-594. corresponding to NaSb03. Platy crystals are hexagonal in D. Weber, A Bischoff (1994) The occurrence of grossite outline, up to 0.2 mm across, colorless, transparent, white (CaAl.O,) in chondrites. Geochim. Cosmochim. Acta, streak, pearly luster, perfect {001} cleavage, flexible, 58,3855-3817. VHNIS = 57 (41-70), nonfluorescent, polysynthetically twinned on (100), Dmeas= 4.8(2), Deale= 4.95 g/cm3 for Z Electron microprobe analysis gave CaO 21.4, A1203 = 6. Optically uniaxial negative, E= 1.631(1), w = 1.84 17.8, FeO 0.31, Ti02 0.15, Si02 0.11, MgO 0.06, sum (calculated). -
High-Resolution TEM Study of Jimthompsonite, Chesterite, and Chain-Width Disorder in Archean Ultramafic Rocks from Isua, West Greenland
American Mineralogist, Volume 95, pages 73–80, 2010 High-resolution TEM study of jimthompsonite, chesterite, and chain-width disorder in Archean ultramafic rocks from Isua, West Greenland HIROMI KONIS H I ,1 HUIFANG XU,1,* AND ROBERT F. DYME K 2 1Department of Geoscience, University of Wisconsin, Madison, Wisconsin 53706, U.S.A. 2Department of Earth and Planetary Sciences, Washington University in St. Louis, Saint Louis, Missouri 63130, U.S.A. ABSTRACT Jimthompsonite and chesterite occur as intergrowths within anthophyllite up to a few millimeters across in talc-magnesite schist from the ~3800 Ma Isua Supracrustal Belt, West Greenland. Pyribole lamellae span the entire intergrowth width and have their own crystal faces. The schist is strongly foliated and pyribole intergrowths are aligned with this foliation indicating broad synchronicity among metamorphic deformation, recrystallization, and pyribole formation. Chain-width errors, polytypic disorder, zipper terminations, displacive planar faults, replacement products by sheet silicates, polygon-shaped cavities, cavity-filling materials, and low-angle grain boundaries were revealed by HRTEM. Based on cross-cutting relationships, the order of the forma- tion of these defects was determined. Pyribole intergrowths formed prior to displacive planar faults and cavity-filling materials. Fine sheet silicates replaced pyriboles or filled cracks after the pyribole intergrowth formation. No obvious reaction or replacement products by talc or chlorite were confirmed at the interface between pyriboles and optically recognizable large sheet silicates, suggesting that fine sheet silicates replacing pyriboles formed later than talc and chlorite. Polysomatic and polytypic lamellae may have grown simultaneously because the lamellae cross cut each other and one does not affect the formation of the other. -
Mineralogical Transformations in Serpentinites from the Mt
PLINIUS n. 37, 2011 MINERALOGICAL TRANSFORMATIONS IN SERPENTINITES FROM THE MT. CAPANNE THERMOMETAMORPHIC AUREOLE (ELBA ISLAND, ITALY) MARCO FERRARI Dipartimento di Scienze della Terra, Università degli Studi di Siena, Via Laterina 8, 53100 Siena INTRODUCTION Following the collisional phase of the early Miocene, which led to the basic structure of the Apennines, Elba Island was affected by extensional tectonics related to the opening of the Tyrrhenian Sea and by the emplacement of the monzogranitic pluton of Mount Capanne 6.9 Ma ago with three pulses of magma (Dini et al., 2002; Farina et al., 2010). The monzogranitic intrusion caused the contact metamorphism and the formation of a clear thermometamorphic aureole that involved ultramafic rocks. In eastern and central Elba Island, massive serpentinites consist of typical retrograde pseudomorphic textures, i.e. mesh rims/cores and bastites, resulting from olivine and pyroxene serpentinization, respectively. Mesh rims, representing early hydration, are formed by isoriented sectors of crystalline 1T lizardite, whereas bastites and mesh cores, corresponding to late fast serpentinization, are formed by poorly crystalline assemblages of tiny lizardite lamellae, chrysotile, and polygonal serpentine fibers, in random orientation (Viti & Mellini, 1998). Relics of peridotitic olivine and pyroxene are rare, indicating advanced serpentinization (Rumori et al., 2004; Viti et al., 2005). On the contrary, the thermometamorphic serpentinites of the aureole of Mt. Capanne show rare traces of pseudomorphic textures with preserved serpentine; they are abundantly composed by talc, chlorite, anthophyllite, tremolite and olivine (thermometamorphic minerals). This research is aimed at characterizing the mineralogical and micro/nanostructural transformations, as well as the reaction mechanisms (both prograde and retrograde) of the serpentinites from the thermometamorphic aureole of Mt. -
Chemistry of the Rockforming Silicates Multiplechain, Sheet, And
REVIEWS OF GEOPHYSICS, VOL. 26, NO. 3, PAGES 407-444, AUGUST 1988 Chemistry of the Rock-Forming Silicates' Multiple-Chain, Sheet, and Framework Structures J. J. PAPIKE Institutefor the Studyof Mineral Deposits,South Dakota Schoolof Mines and Technology,Rapid City The crystal chemistry of 16 groups of multiple-chain, sheet, and framework silicates is reviewed. Crystal structuredrawings are presentedto illustrate crystal chemicalfeatures necessary to interpret chemicaldata for eachmineral group. The 16 silicategroups considered in this revieware the amphibole; nonclassical,ordered pyriboles; mica; pyrophyllite-talc;chlorite; greenalite;minnesotaite; stilpnomel- ane; prehnite;silica polymorphs; feldspar; nepheline-kalsilite; leucite-analcite; sodalite group; cancrinite group; and scapolite.Electron microprobe analyses should be augmentedby independentdeterminations of Fe2+/Fe3+ and H20 for manyof the silicategroups discussed and by determinationsof CO32-, SO42-, S2-, and Li in someof the others.However, microprobe data augmentedas suggestedwill still be ambiguousfor someof the silicategroups considered here because the structuresare not completely determinedor are variable,with disparatedomains and/or structuralmodulations, e.g., pyriboles, greena- lite, minnesotaite,and stilpnomelane.Nevertheless, the most rigorousway to interpretsilicate mineral chemicaldata is basedon the crystal structuresinvolved. CONTENTS Deer et al. [-1963a, 1962, 1963b] for mutiple-chain, sheet, and Introduction ............................................. 407 frameworksilicates, -
New Biopyriboles from Chester, Vermont
AmericanMineralogist, Volume63, pages 100A-1009, 1978 Newbiopyriboles from Chester,Vermont: I. Descriptivemineralogy Dnvn R. VnsLeNllNo CHlnr-rsW. BunNHenr Departmentof GeologicalSciences, Haruard Uniuersity Cambridge,M assachusetts02 I 38 Abstract Four new magnesium-ironchain-silicate minerals have beenidentified from a metamor- phosedultramafic body near Chester,Vermont. They occur with anthophyllite,cummingto- nite,and talcbetween the chloriteand actinolite zones at theboundary ofthe body.The cell parametersof the mineralsare diagnostic:(l) jimthompsoniteis orthorhombic,Pbca, a : 18.6,b:27.2,c:5.30A;(2)clinojimthompsoniteismonoclinic,C2/c,a:9.87,b--27.2,c : 5.32A,0: 109.5";(3)chesteriteis orthorhombic,A2,ma,a:18.6,b:45.3,c:5.30A; (4) an unnamedmineral is monoclinic,A2/m, Am, or A2, a : 9.87,b : 45.3,c : 5.294,B : 109.7o.The physicaland opticalproperties are closeto thoseof low-Caamphiboles. The cleavageangles (37.8' and44.7")are lower than those of amphiboles,and intergrowths of the mineralswith anthophylliteand cummingtonite are petrographically distinctive. The minerals are biopyribolesand are chemicallyintermediate between anthophyllite and talc.The ideal chemicalcomposition for jimthompsoniteand clinojimthompsonite is(Mg,Fe),oSi,roor(OH)n, and that of chesteriteis (Mg,Fe),rSiroOEl(OH)6.The new mineralsmight easilybe confused with amphibolesif theirelectron microprobe analyses were considered alone. Introduction Veblenet al., 1977).Physical and opticaldata, unit- Physical similaritiesamong pyroxenes,amphi- cellparameters, electron microprobe chemical analy- boles,and micasled Johannsen(1911) to call these ses,and X-ray powderdiffraction patterns calculated mineralgroups collectively the "biopyriboles."Solu- from the refinedcrystal structuresare reportedfor tion of the major biopyribolestructure types later three of the new minerals.Nomenclature for these showedthat the similaritieswere not fortuitous,but three well-characterizedminerals is also presented. -
Crystals and Crystal Structures
Crystals and Crystal Structures Crystals and Crystal Structures Richard J. D. Tilley Emeritus Professor, University of Cardiff Copyright # 2006 John Wiley & Sons Ltd, The Atrium, Southern Gate, Chichester, West Sussex PO19 8SQ, England Telephone (+44) 1243 779777 Email (for orders and customer service enquiries): [email protected] Visit our Home Page on www.wileyeurope.com or www.wiley.com All Rights Reserved. No part of this publication may be reproduced, stored in a retrieval system or transmitted in any form or by any means, electronic, mechanical, photocopying, recording, scanning or otherwise, except under the terms of the Copyright, Designs and Patents Act 1988 or under the terms of a licence issued by the Copyright Licensing Agency Ltd, 90 Tottenham Court Road, London W1T 4LP, UK, without the permission in writing of the Publisher. Requests to the Publisher should be addressed to the Permissions Department, John Wiley & Sons Ltd, The Atrium, Southern Gate, Chichester, West Sussex PO19 8SQ, England, or emailed to [email protected], or faxed to (þ44) 1243 770620. This publication is designed to provide accurate and authoritative information in regard to the subject matter covered. It is sold on the understanding that the Publisher is not engaged in rendering professional services. If professional advice or other expert assistance is required, the services of a competent professional should be sought. Other Wiley Editorial Offices John Wiley & Sons Inc., 111 River Street, Hoboken, NJ 07030, USA Jossey-Bass, 989 Market Street, San Francisco, CA 94103-1741, USA Wiley-VCH Verlag GmbH, Boschstr. 12, D-69469 Weinheim, Germany John Wiley & Sons Australia Ltd, 42 McDougall Street, Milton, Queensland 4064, Australia John Wiley & Sons (Asia) Pte Ltd, 2 Clementi Loop #02-01, Jin Xing Distripark, Singapore 129809 John Wiley & Sons Canada Ltd, 6045 Freemont Blvd, Mississauga, Ontario, Canada L5R 4J3 Wiley also publishes its books in a variety of electronic formats.