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ACTA MINERALOGICA-PETROGRAPHICA ABSTRACT SERIES HU ISSN 1589-4835 HU ISSN 0324-6523 Editor-In-Chief Tibor Szederkényi University of Szeged, Szeged, Hungary E-mail: [email protected] Associate Editor Elemér Pál-Molnár University of Szeged, Szeged, Hungary E-mail: [email protected] EDITORIAL BOARD Magdolna Hetényi Gábor Papp University of Szeged, Szeged, Hungary Hungarian Natural History Museum, Budapest, Hungary Péter Árkai Dr. Csaba Szabó Laboratory for Geochemical Research, Hungarian Eötvös Loránd University, Budapest, Hungary Academy of Sciences, Budapest, Hungary György Buda Gyula Szöőr Eötvös Loránd University, Budapest, Hungary University of Debrecen, Debrecen, Hungary Imre Kubovics István Viczián Eötvös Loránd University, Budapest, Hungary Hungarian Institute of Geology, Budapest, Hungary Tibor Zelenka Hungarian Geological Survey, Budapest, Hungary Abbreviated title: Acta Mineral. Petrogr. Abstr. Ser., Szeged The Acta Mineralogica-Petrographica is published by the Department of Mineralogy, Geochemistry and Petrology, University of Szeged On the cover: Lamellar limestone, Létrás-tető, Bükk Mountains, Hungary. Photo: Attila Kovács. Designed by: Elemér Pál Molnár & György Sipos A forum for giving an insight in the state of the art of Mineral Sciences in the Carpathian–Pannonian Region… MCC2 2nd MINERAL SCIENCES IN THE CARPATHIANS INTERNATIONAL CONFERENCE Miskolc, Hungary, 6–7 March 2003 ABSTRACTS Edited by Béla Fehér and Sándor Szakáll English text was revised for major grammatical problems by Erzsébet Tóth, Tamás Váczi and Tamás G. Weiszburg Sponsored by Koch Sándor Foundation (Miskolc) Mineralholding Ltd. (Budapest) Foundation for Hungarian Minerals (Miskolc) Socrates/Erasmus Curriculum Development Programme (CDA) on a Co-ordinated European Curriculum in Mineral Sciences Szeged, Hungary 2003 Organizers Herman Ottó Museum, Miskolc University of Miskolc Co-organizers Austrian Mineralogical Society Hungarian Geological Society Mineralogical Society of Poland Mineralogical Society of Romania Slovak Geological Society Ukrainian Mineralogical Society CBGA Commission on Mineralogy and Geochemistry INTERNATIONAL SCIENTIFIC BOARD Martin Chovan Comenius University, Bratislava, Slovakia Aleksandra Gawęda University of Silesia, Sosnowiec, Poland Friedrich Koller University of Vienna, Vienna, Austria Victor M. Kvasnytsya Institute of Geochemistry, Mineralogy and Ore Formation, National Academy of Sciences, Kyiv, Ukraine Milan Novák Masaryk University, Brno, Czech Republic Gábor Papp Hungarian Natural History Museum, Budapest, Hungary Gheorghe Udubaşa Geological Institute of Romania, Bucharest, Romania LOCAL ORGANIZING COMMITTEE Sándor Szakáll (Chairman) University of Miskolc, Miskolc, Hungary Béla Fehér Herman Ottó Museum, Miskolc, Hungary Ferenc Mádai University of Miskolc, Miskolc, Hungary Timea Tóth-Szabó Herman Ottó Museum, Miskolc, Hungary Acta Mineralogica-Petrographica, Abstract Series 1, Szeged, 2003 INCORPORATION OF “INVISIBLE GOLD” TO THE SULPHIDE MINERALS FROM TATRIC UNIT (WESTERN CARPATHIANS, SLOVAK REPUBLIC) ANDRÁŠ, P.1, CHOVAN, M.2 & OZDÍN, D.2 1 Geological Institute, Slovak Academy of Sciences, Severná 5, SK-974 01 Banská Bystrica, Slovak Republic. E-mail: [email protected] 2 Deparment of Mineralogy and Petrology, Comenius University, Mlynská dolina G, SK-842 15 Bratislava, Slovak Republic. The main gold carriers among the sulphide minerals of As, S, Sb with Au usually follow the temporary increase of the Tatric Unit are arsenopyrite and pyrite. They are usually the As-content during the dynamic varying crystallization enriched in Sb and their characteristic feature is the strong conditions, the suitable temperature and pH conditions. The inhomogeneity caused preferentially by negative As-Au vs. quiet stable crystallization conditions seems to be not very S-(Sb, Fe) correlation. The Au contents in arsenopyrite reach suitable for Au-incorporation. up to 6700 ppm (point analyses from the Trojárová deposit) After some common assumptions the submicroscopic and in pyrite vary from 0 to 62 ppm (from the Pezinok de- gold is situated in lattice deformations. WAGNER et al. posit). Mössbauer spectroscopy proved that the dominant (1988) and CATHELINEAU et al. (1989) published opinion part of the Au content in gold-bearing sulphide minerals is that Au is incorporated to the sulpides in “non-metallic” (with the exception of the Jasenie deposit) represented by anion form. BOYLE (1979) and COOK & CHRYSSOULIS invisible gold. (1990) suggested that Au substitutes for As in arsenopyrite. The incorporation of Au into the crystals show many ir- This hypothesis is based on comparison of ionic radii of regularities. We cannot define any definite scheme but we covalently bonded As and Au. JOHAN et al. (1989) used can present several relatively expressive trends: electron-probe data from gold-rich arsenopyrite and stoichi- It is possible to distinguish three types of gold-bearing ometric calculations to propose that Au is substituting for the sulphide crystals: with more or less homogeneous distribu- excess As, which actually is present in Fe sites. SCHOONEN tion of Au, with Au-enriched crystal cores and Au enriched et al. (1992) and FLEET et al. (1993) show the great impor- crystal rims. The Au-enrichment shows an important positive tance of adsorption-redox reactions on surface of the sul- correlation with As contents. This correlation is usually ab- phides growth zones in the gold-bearing sulphide ores form- sent in homogeneous sulphide crystals. Au-As enrichment of ing process. The Au transport is possible in form of miscel- crystal rims was described from the Malé Karpaty Mts. re- laneous fluids (by diffusion too) and Au is not incorporated gion (Pezinok, Trojárová deposits) and from some occur- to sulphide structure but to pores, vacancies and on surface rences of Nízke Tatry Mts. (Mlynná dolina Valley). Opposite of mineral growth-zones. According to this assumption py- trend was observed at the Dúbrava, Vyšná Boca and Nižná rite and arsenopyrite contain in aqueous fluids at the growth Boca deposits (Nízke Tatry Mts.). plain surfaces oxidizable S-H and Sx-H surface groups (≡ 0 Incorporation of Au into the sulphide minerals depends SSH), so they can reduce AuOH(H2O) ligands and create on various factors: stoichiometry, stability of the aqueous Au-S complexes on surface of arsenopyrite and pyrite complexes, presence of a suitable bonding-relations. Impor- crystals (SCHOONEN et al. 1992). tant supposition of gold incorporation to the sulphides is the The last mentioned mechanism is the most probable one high arsenic concentration. The presented process is usually for the investigated Western Carpathian deposits. Such as- accompanied by Sb, S and Fe content decrease in connection sumption could explain nearly any As:Au correlation in with the acidification of the ore-forming fluids. Critical value ICP/MS-laser ablation and microprobe point analyses and on of this decrease is different at various deposits but is usually the other hand an important As:Au correlation in AAS bulk- approximately constant within one single deposit. analyses of distinct growth zones of gold-bearing sulphide Au enters into the crystals during favourable conditions minerals (there were realised parallel analyses of separately from CO2 containing aqueous solution of low salinities (from dissolved crystal rims and crystal cores). 1 to 11 weight equiv. % NaCl). Homogenization tempera- tures vary from 230 to 325 °C and the crystallization tem- peratures are about 330-450 °C. The coprecipitation of Fe, 3 Acta Mineralogica-Petrographica, Abstract Series 1, Szeged, 2003 WESTERN CARPATHIAN AND SELECTED EUROPEAN Sb-MINERALIZATIONS; Pb -ISOTOPE STUDY ANDRÁŠ, P.1, CHOVAN, M.2, SCHROLL, E.3, NEIVA, A. M. R.4, KRÁL, J.5 & ZACHARIÁŠ, J.6 1 Geological Institute, Slovak Academy of Sciences, Severná 5, SK-974 01 Banská Bystrica, Slovak Republic. E-mail: [email protected] 2 Deparment of Mineralogy and Petrology, Comenius University, Mlynská dolina G, SK-842 15 Bratislava, Slovak Republic. 3, Institute of Mineralogy and Crystallography, University of Vienna, Althanstrasse 14, A-1090 Vienna, Austria. 4 Departamento de Ciencias da Terra, Universidade de Coimbra, P-3000 Coimbra, Portugal. 5 Slovak Geological Office - Geological Survey of Slovak Republic, Mlynská dolina 1, SK-817 04 Bratislava, Slovak Rep. 6 Institute of Geochemistry, Mineralogy and Mineral Resources, Faculty of Science, Charles University, Albertov 6, CZ-128 43 Praha 2, Czech Republic. The Pb-isotope study of Sb-mineralizations from the of ore formation during Variscan orogeny. The oldest model Western Carpathians show a polycyclic character of the ore ages determined from Krásna Hora deposit (510–435 Ma). forming process. Pb-isotope data from Hynčice deposit correspond with De- Tatric Unit - the oldest model ages (corresponding to vonian age – 380 Ma and the sample from Příbram with uranogenic lead) were determined in samples from the Nízke Carboniferous (or Lower Permian?) age – 295 Ma. With the Tatry Mts (about 400 Ma). The second group of the data exception of the data from Krásna Hora deposit the samples from this region vary between 300-330 Ma and the third one indicate average crust origin of lead (µ1 < 9.80). about 200 Ma (ANDRÁŠ et al., 1998). The main field of the The oldest 206Pb/204Pb model ages both from Dúrico – results from the Malé Karpaty Mts. is clustered round time- Beirão district and from Trás-os-Montés (Galicia-Trás-os- linea at 200-250 Ma (Pezinok deposit). The second group
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  • Mineral Index

    Mineral Index

    Mineral Index Abhurite T.73, T.355 Anandite-Zlvl, T.116, T.455 Actinolite T.115, T.475 Anandite-20r T.116, T.45S Adamite T.73,T.405, T.60S Ancylite-(Ce) T.74,T.35S Adelite T.115, T.40S Andalusite (VoU, T.52,T.22S), T.27S, T.60S Aegirine T.73, T.30S Andesine (VoU, T.58, T.22S), T.41S Aenigmatite T.115, T.46S Andorite T.74, T.31S Aerugite (VoU, T.64, T.22S), T.34S Andradite T.74, T.36S Agrellite T.115, T.47S Andremeyerite T.116, T.41S Aikinite T.73,T.27S, T.60S Andrewsite T.116, T.465 Akatoreite T.73, T.54S, T.615 Angelellite T.74,T.59S Akermanite T.73, T.33S Ankerite T.74,T.305 Aktashite T.73, T.36S Annite T.146, T.44S Albite T.73,T.30S, T.60S Anorthite T.74,T.415 Aleksite T.73, T.35S Anorthoclase T.74,T.30S, T.60S Alforsite T.73, T.325 Anthoinite T.74, T.31S Allactite T.73, T.38S Anthophyllite T.74, T.47S, T.61S Allanite-(Ce) T.146, T.51S Antigorite T.74,T.375, 60S Allanite-(La) T.115, T.44S Antlerite T.74, T.32S, T.60S Allanite-(Y) T.146, T.51S Apatite T.75, T.32S, T.60S Alleghanyite T.73, T.36S Aphthitalite T.75,T.42S, T.60 Allophane T.115, T.59S Apuanite T.75,T.34S Alluaudite T.115, T.45S Archerite T.75,T.31S Almandine T.73, T.36S Arctite T.146, T.53S Alstonite T.73,T.315 Arcubisite T.75, T.31S Althausite T.73,T.40S Ardaite T.75,T.39S Alumino-barroisite T.166, T.57S Ardennite T.166, T.55S Alumino-ferra-hornblende T.166, T.57S Arfvedsonite T.146, T.55S, T.61S Alumino-katophorite T.166, T.57S Argentojarosite T.116, T.45S Alumino-magnesio-hornblende T.159,T.555 Argentotennantite T.75,T.47S Alumino-taramite T.166, T.57S Argyrodite (VoU,
  • Western Carpathians, Poland)

    Western Carpathians, Poland)

    Geological Quarterly, 2006, 50 (1): 169–194 Late Jurassic-Miocene evolution of the Outer Carpathian fold-and-thrust belt and its foredeep basin (Western Carpathians, Poland) Nestor OSZCZYPKO Oszczypko N. (2006) — Late Jurassic-Miocene evolution of the Outer Carpathian fold-and-thrust belt and its foredeep basin (Western Carpathians, Poland). Geol. Quart., 50 (1): 169–194. Warszawa. The Outer Carpathian Basin domain developed in its initial stage as a Jurassic-Early Cretaceous rifted passive margin that faced the east- ern parts of the oceanic Alpine Tethys. Following closure of this oceanic basin during the Late Cretaceous and collision of the Inner Western Carpathian orogenic wedge with the Outer Carpathian passive margin at the Cretaceous-Paleocene transition, the Outer Carpathian Basin domain was transformed into a foreland basin that was progressively scooped out by nappes and thrust sheets. In the pre- and syn-orogenic evolution of the Outer Carpathian basins the following prominent periods can be distinguished: (1) Middle Juras- sic-Early Cretaceous syn-rift opening of basins followed by Early Cretaceous post-rift thermal subsidence, (2) latest Creta- ceous-Paleocene syn-collisional inversion, (3) Late Paleocene to Middle Eocene flexural subsidence and (4) Late Eocene-Early Miocene synorogenic closure of the basins. In the Outer Carpathian domain driving forces of tectonic subsidence were syn-rift and thermal post-rift processes, as well as tectonic loads related to the emplacement of nappes and slab-pull. Similar to other orogenic belts, folding of the Outer Carpathians commenced in their internal parts and progressed in time towards the continental foreland. This process was initi- ated at the end of the Paleocene at the Pieniny Klippen Belt/Magura Basin boundary and was completed during early Burdigalian in the northern part of the Krosno Flysch Basin.