Geological Investigations in the Bird River Sill, Southeastern Manitoba (Part of NTS 52L5): Geology and Preliminary Geochemical Results by C.A
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Complex Basalt-Mugearite Sill in Piton Des Neiges Volcano, Reunion
THE AMERICAN MINERALOGIST. VOL. 52, SEPTEMBER-OCTOBER, 1967 COMPLEX BASALT-MUGEARITE SILL IN PITON DES NEIGES VOLCANO, REUNION B. G. J. UetoN, Grant Institute oJ Geology,Uniaersi,ty oJ Ed.inburgh, Edinbwrgh, Scotland, AND W. J. WaoswoRru, Deportmentof Geology,The Un'it;ersity, Manchester,England.. ABsrRAcr An extensive suite of minor intrusions, contempcraneous with the late-stage differenti- ated lavas of Piton des Neiges volcano, occurs within an old agglomeratic complex. An 8-m sill within this suite is strongly difierentiated with a basaltic centre (Thorton Tuttle Index 27.6), residual veins of benmoreite (T. T. Index 75.2), and still more extreme veinlets of quartz trachyte. Although gravitative settling of olivine, augite and ore irz silzr is believed to be responsible for some of the observed variation, the over-all composition of the sill is con- siderably more basic than the mugearite which forms the chilled contacts. It is therefore concluded that considerable magmatic difierentiation must have preceded the emplacement of the sill. This probably took place in a dykeJike magma body with a compositional gra- dient from mugearite at the top to olivine basalt in the lower parts. INrnonucrroN The island of Reunion, in the western Indian Ocean, has the form of a volcanic doublet overlying a great volcanic complex rising from the deep ocean floor. The southeastern component of this doublet is still highly active and erupts relatively undifierentiated, olivine-rich basalts of mildly alkaline or transitional type (Coombs, 1963; Upton and Wads- worth, 1966). The northwestern volcano however has been inactive a sufficient time for erosionalprocesses to have hollowed out amphitheatre- headed valleys up to 2500 meters deep in the volcanic pile. -
Controls on the Expression of Igneous Intrusions in Seismic Reflection Data GEOSPHERE; V
Research Paper GEOSPHERE Controls on the expression of igneous intrusions in seismic reflection data GEOSPHERE; v. 11, no. 4 Craig Magee, Shivani M. Maharaj, Thilo Wrona, and Christopher A.-L. Jackson Basins Research Group (BRG), Department of Earth Science and Engineering, Imperial College, 39 Prince Consort Road, London SW7 2BP, UK doi:10.1130/GES01150.1 14 figures; 2 tables ABSTRACT geometries in the field is, however, hampered by a lack of high-quality, fully CORRESPONDENCE: [email protected] three-dimensional (3-D) exposures and the 2-D nature of the Earth’s surface The architecture of subsurface magma plumbing systems influences a va- (Fig. 1). Geophysical techniques such as magnetotellurics, InSAR (interfero- CITATION: Magee, C., Maharaj, S.M., Wrona, T., riety of igneous processes, including the physiochemical evolution of magma metric synthetic aperture radar), and reflection seismology have therefore and Jackson, C.A.-L., 2015, Controls on the expres- sion of igneous intrusions in seismic reflection data: and extrusion sites. Seismic reflection data provides a unique opportunity to been employed to either constrain subsurface intrusions or track real-time Geosphere, v. 11, no. 4, p. 1024–1041, doi: 10 .1130 image and analyze these subvolcanic systems in three dimensions and has magma migration (e.g., Smallwood and Maresh, 2002; Wright et al., 2006; /GES01150.1. arguably revolutionized our understanding of magma emplacement. In par- Biggs et al., 2011; Pagli et al., 2012). Of these techniques, reflection seismol- ticular, the observation of (1) interconnected sills, (2) transgressive sill limbs, ogy arguably provides the most complete and detailed imaging of individual Received 11 November 2014 and (3) magma flow indicators in seismic data suggest that sill complexes intrusions and intrusion systems. -
New Exploration Methods for Platinum and Rhodium Deposits
SYNTHESIS REPORT FOR PUBLICATION CONTRACT No : BRE2-CT92-0302 PROJECT N* : BE-5793 TITLE : NEW EXPLORATION METHOD FOR PLATINUM AND RHODIUM DEPOSITS POOR IN BASE METAL SULPHIDES PROJECT COORDINATOR : BRGM PARTNERS : UNIVERSITY OF MANCHESTER UNIVERSITY OF COPENHAGEN CNRS NANCY STARTING DATE :30.11.92 DURATION :36 MONTHS *** PROJECT FUNDED BY THE EUROPEAN * * COMMUNITY UNDER THE BRITE/ELJRAM * * PROGRAMME * * *** E DATE: 30.1.96 H. TITLE, AUTHOR NAMES AND ADRESSES NEW EXPLORATION METHODS FOR PLATINUM AND RHODIUM POOR IN BASE METAL SULPHIDES NEXTPRIM (EC Contract BRE2-CT92-0302 - Project BE-5793) Coordinator BRGM : M. Ohnenstetter, Z. Johan, A. Cocherie, A.M. Fouillac. C. Guerrot 3, Avenue Claude Guillemin, BP 6009,4.5060 ORLEANS CEDEX 2, France. Partners CNRS : D. Ohnenstetter, M. Chaussidon, O. Rouer CRPG, 15, rue Notre Dame Des Pauvres, B.P. 20, 54501 Vand@uvre les Nan~ y, France. University of Couenha~en : E. Makovicky, M. Makovicky, J. Rose-Hansen, S. Karup- Mgller Geological Institute, f?kter Voldgade 10, 1350 Copenhagen K, Danemark University of Manchester : D. Vaughan, G. Turner, R.A.D. Pattrick, A.P. Gize. 1. Lyon, I. McDonald Department of Geology, Williamson Building, Oxford Road, M 13 9PL Manchester. England III. ABSTRACT A multidisciplinary approach has been applied to four subeconomic deposits of platinum metals in order to propose a new model of formation for platinum group element (PGE) deposits devoid of significant base metal sulphides (BMS). The aim was to facilitate the identification of new targets for PGE exploration. Two of the deposits occur in Albania, in the Tropoja and Bulqiza massifs respectively; these belong to an ophiolitic belt created in an oceanic environment during the Upper Jurassic. -
Origin of Platinum Group Minerals (PGM) Inclusions in Chromite Deposits of the Urals
minerals Article Origin of Platinum Group Minerals (PGM) Inclusions in Chromite Deposits of the Urals Federica Zaccarini 1,*, Giorgio Garuti 1, Evgeny Pushkarev 2 and Oskar Thalhammer 1 1 Department of Applied Geosciences and Geophysics, University of Leoben, Peter Tunner Str.5, A 8700 Leoben, Austria; [email protected] (G.G.); [email protected] (O.T.) 2 Institute of Geology and Geochemistry, Ural Branch of the Russian Academy of Science, Str. Pochtovy per. 7, 620151 Ekaterinburg, Russia; [email protected] * Correspondence: [email protected]; Tel.: +43-3842-402-6218 Received: 13 August 2018; Accepted: 28 August 2018; Published: 31 August 2018 Abstract: This paper reviews a database of about 1500 published and 1000 unpublished microprobe analyses of platinum-group minerals (PGM) from chromite deposits associated with ophiolites and Alaskan-type complexes of the Urals. Composition, texture, and paragenesis of unaltered PGM enclosed in fresh chromitite of the ophiolites indicate that the PGM formed by a sequence of crystallization events before, during, and probably after primary chromite precipitation. The most important controlling factors are sulfur fugacity and temperature. Laurite and Os–Ir–Ru alloys are pristine liquidus phases crystallized at high temperature and low sulfur fugacity: they were trapped in the chromite as solid particles. Oxygen thermobarometry supports that several chromitites underwent compositional equilibration down to 700 ◦C involving increase of the Fe3/Fe2 ratio. These chromitites contain a great number of PGM including—besides laurite and alloys—erlichmanite, Ir–Ni–sulfides, and Ir–Ru sulfarsenides formed by increasing sulfur fugacity. Correlation with chromite composition suggests that the latest stage of PGM crystallization might have occurred in the subsolidus. -
Detrital Platinum-Group Minerals (PGM) in Rivers of the Bushveld Complex, South Africa – a Reconnaissance Study
Detrital Platinum-Group Minerals (PGM) in Rivers of the Bushveld Complex, South Africa – A Reconnaissance Study Thomas Oberthür, Frank Melcher, Lothar Gast, Christian Wöhrl and Jerzy Lodziak Federal Institute for Geosciences and Natural Resources (BGR), Stilleweg 2, D-30655 Hannover, Germany e-mail: [email protected] Introduction Regional geology The initial major discovery of platinum in Sampling concentrated on stream the Bushveld Complex, which subsequently led to sediments of rivers in the vicinity of the original the discovery of the Merensky Reef, was made in discovery of the Merensky Reef on the farm 1924 by panning in a river bed on the farm Maandagshoek close to Burgersfort in the Eastern Maandagshoek in the Eastern Bushveld (Merensky Bushveld (Fig. 1). The localities investigated by 1924, 1926, Wagner 1929, Cawthorn 1999a, 1999b, Cawthorn (1999b, 2001), i. e. those documented by 2001). Wagner (1929) also reports on a number of Merensky (1924) as Pt-bearing, and additional alluvial diggings in the Bushveld Complex that places along the Moopetsi river were sampled. The produced some platinum. However, as mining river valley runs approximately north-south, commenced on the rich pipes and reef-type deposits subparallel to the layering of the Mafic Phase of the of the Bushveld, alluvial PGM soon became Bushveld Complex, and is between 2 and 3 km forgotten and no published information on the wide. On the farm Maandagshoek, the Merensky placer PGM is available. Cawthorn (1999b, 2001) Reef and the UG2 are about 2 km apart and crop performed geochemical investigations of stream- out on the western and eastern side, respectively, of sediments at and close to the 1924 discovery site the Moopetsi river. -
The Tasmania Basin – Gondwanan Petroleum System
The Tasmania Basin – Gondwanan Petroleum System Dr Catherine Reid School of Earth Sciences, University of Tasmania APDI SPIRT “Petroleum System Modelling Onshore Tasmania” Partial Report on work completed to December 2002 TASMANIA BASIN – GONDWANAN SYSTEM Catherine Reid BASIN DEVELOPMENT LATE CARBONIFEROUS TO TRIASSIC The Parmeener Supergroup (Banks, 1973) contains both marine and terrestrial rocks from the Tasmania Basin, ranging in age from Late Carboniferous to Late Triassic. The supergroup is divided (Forsyth et al., 1974) into the Lower Parmeener, of mostly marine Late Carboniferous to Permian rocks, and the Upper Parmeener of terrestrial origin and Late Permian to Triassic age. The Lower and Upper Parmeener Supergroups are lithostratigraphic units and their boundary does not correlate to the Permian and Triassic biostratigraphic boundary, which is in the lower part of the Upper Parmeener Supergroup. Mapping and drilling programs by the Geological Survey of Tasmania and other private companies have revealed many of the details of the lower Parmeener Supergroup. THE LOWER PARMEENER SUPERGROUP The Parmeener Supergroup lies with pronounced unconformity on older folded and metamorphosed sedimentary and igneous rocks. The Late Carboniferous Tasmania Basin was a broadly north-south trending basin with pronounced highs in the northeast, northwest and southwest. During the mid-Carboniferous much of Gondwanaland was under widespread glaciation (Crowell & Frakes, 1975), and many Late Palaeozoic deposits reflect this glacial influence. Continental ice was developed in the Tasmanian region, with fjord glaciers and ice sheets reaching sea-level that left glacigenic deposits of mostly glaciomarine origin (Hand, 1993) as the ice sheet retreated. The lowermost Parmeener rocks (Fig. 1A) are debris flow diamictites, dropstone diamictites, glacial outwash conglomerates and sandstones, pebbly mudstones and rhythmites (Clarke, 1989; Hand, 1993). -
Platinum-Group Element and Minerals in the Lower and Middle Group Chromitites of the Western Bushveld Complex, South Africa
Helmholtz-Zentrum Dresden-Rossendorf (HZDR) Platinum-group element and minerals in the Lower and Middle Group chromitites of the western Bushveld Complex, South Africa Junge, M.; Oberthür, T.; Osbahr, I.; Gutter, P.; Originally published: August 2016 Mineralium Deposita 51(2016)7, 841-852 DOI: https://doi.org/10.1007/s00126-016-0676-6 Perma-Link to Publication Repository of HZDR: https://www.hzdr.de/publications/Publ-26567 Release of the secondary publication based on the publisher's specified embargo time. Platinum-group elements and minerals in the Lower and Middle Group chromitites of the western Bushveld Complex, South Africa Malte Junge1, Thomas Oberthür1, Inga Osbahr2 and Paul Gutter3 1Federal Institute for Geosciences and Natural Resources (BGR), Stilleweg 2, D-30655 Hannover, Germany; [email protected] 2Helmholtz Institute Freiberg for Resource Technology, Halsbrücker Strasse 34, 09599 Freiberg, Germany 3SYLVANIA Platinum Ltd., P.O. Box 976, Florida Hills 1716, South Africa Abstract The chromitites of the Bushveld Complex in South Africa contain vast resources of platinum- group elements (PGE). However, knowledge of the distribution and the mineralogical siting of the PGE in the Lower Group (LG) and Middle Group (MG) chromitite seams of the Bushveld Complex is limited. We studied concentrates from the LG-6 and MG-2 chromitites of the western Bushveld Complex by a variety of microanalytical techniques. The dominant PGM are sulfides, namely laurite, cooperite-braggite and malanite-cuprorhodsite, followed by PGE-sulfarsenides, sperrylite, and Pt-Fe alloys. Laurite is the most abundant PGM (vol%). The matching sets of PGM present in the LG and MG chromitites of both the western and the eastern Bushveld Complex, and in the UG-2 chromitite, show strong similarities which support the assumption of a characteristic and general chromitite-related PGM assemblage. -
Iridarsenite (Ir, Ru)As2 C 2001-2005 Mineral Data Publishing, Version 1
Iridarsenite (Ir, Ru)As2 c 2001-2005 Mineral Data Publishing, version 1 Crystal Data: Monoclinic. Point Group: 2/m. As irregular inclusions, to 60 µm, in a matrix of rutheniridosmine. Physical Properties: Hardness = n.d. VHN = 488 and 686 (100 g load) on two grains. D(meas.) = n.d. D(calc.) = 10.9 Optical Properties: Opaque. Color: In polished section, medium gray with brownish tint. Luster: Metallic. Pleochroism: Weak to none. Anisotropism: Weak but distinct, from medium gray to pale orange-brown. R1–R2: (470) 47.2–46.9, (546) 45.4–46.1, (589) 44.9–46.6, (650) 41.4–44.0 ◦ 0 Cell Data: Space Group: P 21/c (synthetic). a = 6.05 b = 6.06 c = 6.18 β = 113 17 Z=4 X-ray Powder Pattern: Papua New Guinea. 3.90 (100), 2.840 (70), 2.069 (60), 2.610 (50), 1.910 (50), 1.943 (40), 1.875 (40) Chemistry: (1) (2) Ir 40.7 52.2 Ru 10.3 1.7 Os 1.3 0.4 Pt 0.5 1.1 Rh 0.9 0.2 Pd 0.1 As 46.2 44.0 S 0.2 Total 99.0 99.9 (1) Papua New Guinea; by electron microprobe, corresponds to (Ir0.69Ru0.33Os0.02)Σ=1.04As2.00. (2) Do.; by electron microprobe, average of four other grains; corresponds to (Ir0.92Ru0.06 Os0.01Pt0.02Rh0.01)Σ=1.02(As1.97S0.03)Σ=2.00. Occurrence: In nuggets or fragments of natural Os–Ir–Ru alloys. Association: Irarsite, ruthenarsenite, rutheniridosmine. Distribution: From an unspecified locality [probably the Waria River, Bowutu Mountains, or the Yodda Goldfield] in Papua New Guinea [TL]. -
Braggite (Pt, Pd, Ni)S
Braggite (Pt, Pd, Ni)S c 2001-2005 Mineral Data Publishing, version 1 Crystal Data: Tetragonal. Point Group: 4/m or 4. As prisms, to 2 cm, and rounded grains. Twinning: Rarely observed. Physical Properties: Hardness = n.d. VHN = 946–1064, 997 average (100 g load). D(meas.) = ∼10 D(calc.) = 9.383 Optical Properties: Opaque. Color: White in reflected light. Luster: Metallic. Anisotropism: Distinct, in purplish and pinkish shades of gray and brown. R1–R2: (400) 41.3–41.8, (420) 41.8–42.4, (440) 42.1–43.0, (460) 42.4–43.4, (480) 42.5–43.8, (500) 42.7–44.1, (520) 42.7–44.2, (540) 42.6–44.2, (560) 42.5–44.2, (580) 42.4–44.2, (600) 42.3–44.1, (620) 42.2–44.1, (640) 41.9–44.0, (660) 41.9–43.9, (680) 41.9–43.8, (700) 41.5–43.8 Cell Data: Space Group: P 42/m. a = 6.367 c = 6.561 Z = 8 X-ray Powder Pattern: Potgietersrus district, South Africa; can be confused with vysotskite. 2.86 (100), 2.93 (30), 2.64 (30), 1.852 (30), 1.423 (30), 1.713 (20), 1.595 (2) Chemistry: (1) (2) (1) (2) Pt 63.2 62.1 Ni 4.4 2.0 Pd 15.4 19.0 S 17.4 16.9 Total 100.4 100.0 (1) Potgietersrus district, South Africa; by electron microprobe, corresponding to (Pt0.60Pd0.27 Ni0.14)Σ=1.01S1.00. (2) Stillwater complex, Montana, USA; by electron microprobe, corresponding to (Pt0.60Pd0.34Ni0.06)Σ=1.00S1.00. -
Colloform High-Purity Platinum from the Placer Deposit
Colloform high-purity platinum from the placer deposit of Koura River (Gornaya Shoriya, Russia) Nesterenko G.V.1, Zhmodik S.M.1,2, Airiyants E.V.1, Belyanin D.K.1,2, Kolpakov V.V.1, Bogush A.A.1,3,* 1V.S. Sobolev Institute of Geology and Mineralogy, Siberian Branch of the Russian Academy of Sciences, Novosibirsk 630090, Russia 2Novosibirsk State University, Novosibirsk 630090, Russia 3Department of Civil, Environmental & Geomatic Engineering, University College London, London WC1E 6BT, UK *Corresponding author: A.A. Bogush, E-mail: [email protected] Abstract A microinclusion of colloform high-purity platinum in a grain of platinum-group minerals (PGM) from the alluvial gold-bearing placer deposit in the south of Western Siberia (Russia) was detected and characterized for the first time. It is different in composition, texture, and conditions of formation from high-purity platinum of other regions described in the literature. The main characteristics of investigated high-purity platinum are colloform-layered texture, admixture of Fe (0.37-0.78 wt.%), and paragenesis of Cu-rich isoferroplatinum, hongshiite, and rhodarsenide. The PGM grain with high-purity platinum is multiphase and heterogeneous in texture. It is a product of intensive metasomatic transformation of Cu-rich isoferroplatinum (Pt3(Fe0.6Cu0.4)). The transformation was carried out in two stages: 1 - copper stage including three substages (Cu-rich isoferroplatinum, copper platinum and hongshiite); and 2 - arsenic (rhodarsenide). The formation of high-purity platinum was separated in time from the formation of isoferroplatinum and was carried out by precipitation from postmagmatic solutions. Keywords: platinum-group elements (PGE), platinum-group minerals (PGM), high-purity platinum, Cu-rich isoferroplatinum, hongshiite, alluvial placer, Gornaya Shoriya Introduction High-purity platinum was discovered in the gold-bearing placer deposit of Koura River situated in Gornaya Shoriya (south-western Siberia, Russia, Fig. -
Description of Map Units
GEOLOGIC MAP OF THE LATIR VOLCANIC FIELD AND ADJACENT AREAS, NORTHERN NEW MEXICO By Peter W. Lipman and John C. Reed, Jr. 1989 DESCRIPTION OF MAP UNITS [Ages for Tertiary igneous rocks are based on potassium-argon (K-Ar) and fission-track (F-T) determinations by H. H. Mehnert and C. W. Naeser (Lipman and others, 1986), except where otherwise noted. Dates on Proterozoic igneous rocks are uranium-lead (U-Pb) determinations on zircon by S. A. Bowring (Bowring and others, 1984, and oral commun., 1985). Volcanic and plutonic rock names are in accord with the IUGS classification system, except that a few volcanic names (such as quartz latite) are used as defined by Lipman (1975) following historic regional usage. The Tertiary igneous rocks, other than the peralkaline rhyolites associated with the Questa caldera, constitute a high-K subalkaline suite similar to those of other Tertiary volcanic fields in the southern Rocky Mountains, but the modifiers called for by some classification schemes have been dropped for brevity: thus, a unit is called andesite, rather than alkali andesite or high-K andesite. Because many units were mapped on the basis of compositional affinities, map symbols were selected to emphasize composition more than geographic identifier: thus, all andesite symbols start with Ta; all quartz latites with Tq, and so forth.] SURFICIAL DEPOSITS ds Mine dumps (Holocene)—In and adjacent to the inactive open pit operation of Union Molycorp. Consist of angular blocks and finer debris, mainly from the Sulphur Gulch pluton Qal Alluvium (Holocene)—Silt, sand, gravel, and peaty material in valley bottoms. -
Osmium (Os, Ir, Ru) C 2001-2005 Mineral Data Publishing, Version 1
Osmium (Os, Ir, Ru) c 2001-2005 Mineral Data Publishing, version 1 Crystal Data: Hexagonal. Point Group: 6/m 2/m 2/m. Rare crystals are hexagonal tabular, to 3 mm; commonly as euhedral prismatic inclusions in Pt–Fe alloys. Physical Properties: Hardness = n.d. VHN = 1206–1246 (25 g load). D(meas.) = 22.48 D(calc.) = 22.59 Optical Properties: Opaque. Color: White with a bluish gray tinge in reflected light. Pleochroism: Noticeable. Anisotropism: Strong, reddish orange. R1–R2: (400) — , (420) 62.7–63.9, (440) 63.9–64.7, (460) 63.9–64.6, (480) 63.8–64.4, (500) 63.3–63.8, (520) 62.7–63.2, (540) 62.1–62.7, (560) 61.5–61.8, (580) 60.9–61.4, (600) 60.4–60.7, (620) 59.9–60.2, (640) 59.6–59.8, (660) 59.3–59.9, (680) 59.2–60.0, (700) 59.4–60.0 Cell Data: Space Group: P 63/mmc. a = 2.7341 c = 4.3197 Z = 2 X-ray Powder Pattern: Synthetic osmium. 2.076 (100), 2.367 (35), 2.160 (35), 1.3668 (20), 1.2300 (20), 1.1551 (20), 1.595 (18) Chemistry: (1) (2) (3) Os 94.1 84.8 98.8 r 5.4 12.0 0.3 Ru 0.8 2.2 Pt 0.1 1.7 Rh 0.5 Pd 0.1 0.2 Total 100.4 101.3 99.3 (1) Atlin, Canada; by electron microprobe. (2) Joubdo stream, Ethiopia; by electron microprobe. (3) Gusevogorskii pluton, Russia; by electron microprobe, average of four analyses.