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19th Biennial ConferenceEUROPEAN CURRENTRESEARCH ON FLUID INCLUSIONSECROFI-XIX17–20 July, 2007University of Bern, SwitzerlandPROGRAMME and ABSTRACTS

Conference SponsersThe following companies and organizations are thanked for their generous sponsorship of the ECROFI-XIXConference:Max und ElsaBeer-Brawand-Fonds

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 1ECROFI-XIX Organizing CommitteeRock–Water Interaction, Institute of Geological Sciences, University of Bern,Baltzerstrasse 1+3, CH-3012 Bern, SwitzerlandLarryn W. DiamondThomas PettkeSarah AntenenIvan MercolliCarl SpandlerRegula GesemannAlexandre TarantolaMonika PainsiJános KodolányiECROFI International Advisory BoardDavid A. BanksRobert J. BodnarBenedetto de VivoLarryn W. DiamondJean DubessyMaria Luce FrezzottiAlfons Van den KerkhofVolker LüdersFernando NoronhaCsaba SzabòJacques PirononSchool of Earth Science, University of Leeds, United KingdomDepartment of Geosciences, Virginia Tech, Blacksburg, UnitedStates of AmericaDipartimento di Geofisica e Volcanologia, Universita“Federico II”, Naples, ItalyInstitute of Geological Sciences, University of Bern,SwitzerlandG2R/CNRS, Université Henri-Poincaré, Nancy, FranceDipartimento Scienze della Terra, Università di Siena, ItalyGeowissenschaftliches Zentrum der Universität Göttingen,GermanyGeoforschungsZentrum Potsdam, GermanyCentro de Geologia da Universidade do Porto, PortugalDepartment of Petrology and Geochemistry, Eötvös University,Budapest, HungaryCREGU, CNRS, Nancy, France1

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 2SCOPE AND HISTORY OF ECROFIScope of ECROFIThe series of biennial conferences on European Current Research on Fluid Inclusions(ECROFI)attracts a wide range of Earth scientists investigating the roles of fluids and magmas within the Earth andplanetary bodies. Primarily, the meetings keep the scientific community up to date on new developments inanalysis and interpretation of fluid and melt inclusions, and on how the information gleaned from inclusionshelps to answer wider questions in the earth sciences. In addition, ECROFI provides a congenial setting forgraduate students and young investigators to present their research to a broad audience, to consult withexperts relevant to their research projects, and to contact potential employers in person.ECROFI participants belong to universities, government research institutions or commercial companies,including those involved in petroleum exploration, ore exploration and deep-geological disposal of wastes.Most participants come from Western and Eastern Europe, but many scientists from the Americas, Africa, Asiaand Australasia also regularly attend the meetings. ECROFI-XIX at the University of Bern, for example, bringstogether approximately 140 participants from 28 countries. Thus, although the “E” in “ECROFI” stands forEurope, the meetings are truly intercontinental. Accordingly, the official conference language is English.The current meeting, ECROFI-XIX, hosts 130 scientific communications (74 posters and 56 oralpresentations, including 7 keynote lectures) on the following topics: advances in analytical techniques;thermodynamic and experimental models of fluid properties, systematics of inclusion behaviour, advances inanalytical techniques, diagenetic and petroleum fluids, geothermal systems, deep crustal and mantle fluids,ore deposits, melt inclusions and igneous processes, the role of fluids in tectonics, and some novel applicationsof fluid inclusions. The meeting is preceded by workshops on selected analytical methods and by a field tripto the Bernese Alps, it includes a mid-conference petrography workshop, and it is followed by a field trip tomineral deposits in the Western Italian Alps.History of ECROFIThe first meeting of what was later dubbed “ECROFI” was held in 1969 at the Natural History Museumof Bern, organized by H. A. Stalder (Bern) and G. Deicha (Paris). Forty-nine scientists took part in thatmeeting, among them such well known names as R. Clocchiatti, E.J. Gübelin, B. Poty, E. Roedder and J.-C.Touray. The success of this first ECROFI meeting, and the rapidly growing international interest in fluidinclusion studies at the beginning of the 1970s, spurred a series of similar meetings in various parts ofEurope.By the time Utrecht hosted a meeting in 1981, a certain tradition was recognized by the European fluidinclusion community. The organizers at Utrecht, H. Swanenberg, R. Kreulen and J. Touret, named theirconference “ECRFI-VI” (later written ECROFI), and they retrospectively identified five previous meetings asits forerunners in a series. Thus, Bern, 1969 (ECROFI-I) and Milano, 1973 (ECROFI-II) formed the early lineof descent. Apparently the assignment of the next two meetings in the series was not clearly announced atUtrecht, and so the identities of ECROFI-III and IV are now something of a mystery. The meeting at Durhamin 1976 was certainly one of them, but according to A. Stalder, J. Touret and E. Horn, all of whom attendedthe Utrecht meeting, two conferences in France come into question for the missing title: either Paris in 1975or Nancy in 1978. Our collective memory is clear thereafter and the meeting at Karlsruhe in 1979 is agreedto have been ECROFI-V.From ECROFI-V onwards, the meetings have been held biennially at different venues. The chronologicallist below was compiled by H. A. Stalder and L. W. Diamond.2

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 3Chronological list of ECROFI meetingsNo. Date VenueOrganizersNumber of presentationsPublished ProceedingsI13–15 Sep.1969Naturhistorsiches Museum, Bern,SwitzerlandH.A. Stalder (Bern), G. Deicha (Paris)20 presentations (oral)Abstracts in Fl. Incl. Res. 3 (1970).Twenty papers in Schweiz. Min. Petr.Mitt. 50(1): 1–208 (1970)II2-3 Oct.1973Universitá di Milano, Italy (SocietàItaliana di Mineralogia e Petrologia)P. Zuffardi, G. Perna11 presentations (oral)Eight papers in Rend. Soc. Ital. Min.Petr. 30: 337–459 (1974)III?4 Dec.1975Centre Nationale de la RechercheScientifique (CNRS), Paris, FranceG. DeichaAbstracts in Fl. Incl. Res. 9 (1976).Twenty-three papers in Bull. Soc. Fr.Min. Crist. 99: 67–192 (1976)IIIorIV?14–17 Dec.1976University of Durham, EnglandGeological and Mineralogical Societiesof England38 presentationsAbstracts in J. Geol. Soc. Lond. 134:385–397 and in Trans. Inst. MiningMetallurg. 86 B154–160 (1977).IV?26–29 Sep.1978Soc. Fr. Minéral. Crist. and CNRS,Nancy, FranceAmmou-Chokroum, Bernard, Bolfa,Brown, Cases, de La Roche, Lougnon,Poty, Protas, Souchier, Weisbrod,Willaime57 presentationsAbstracts in Fl. Incl. Res. 12 (1979).Nineteen papers in Bull. Min. 102(5-6): 471–683 (1979)VFeb.1979Universität Karlsruhe, GermanyE. AlthausVI22–24 Apr.1981Universiteit Utrecht, NetherlandsH. Schwanenberg, R. Kreulen, J.Touret34 presentationsAbstracts in Fl. Incl. Res. 14 (1981).Fifteen papers in special issue ofChem. Geol. 37: 1–214 (1982)VII6-8 Apr.1983Université de Orléans, FranceA. Gelderon, L. Lebel, J-C. Touray46 presentationsAbtracts in Fl. Incl. Res. 16 (1983).Eighteen papers in Bull. Min. 107,123–340 (1984)VIII10–12 Apr.1985Universität Göttingen, GermanyE.E. Horn66 presentations (40 oral)Abtracts in Fl. Incl. Res. 18 (1985)Twenty-nine papers in special issueof Chem. Geol. 61: 1–308 (1982)3

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 4IX4–6 May1987Universidade do Porto, PortugalF. Noronha75 presentations (64 oral)Abstracts in Fl. Incl. Res. 20 (1987).Sixteen papers in Bull. Min. 111:249–426 (1988)X Apr. 6–81989Imperial College, London, EnglandA.H. Rankin, D.H.M. Alderton, T.J.Shepherd82 presentations (54 oral)Abstracts in Fl. Incl. Res. 22 (1989).Eighteen papers in special issue ofMin. Mag. 375: 143–341 (1990)XI10-12 Apr.1991Universitá di Firenze, ItalyP. Lattanzi167 presentationsAbstracts in Fl. Incl. Res. 24 (1991).and Plinius, Supp. ital. Eur. J. Min. 5:1-267 (1991). Twenty-five papers inEur. J. Min. 4: 863–1202 (1992)XII14–16 Jun.1993Uniwersytet Warszawski, Warsaw,PolandA. Kozlowski95 presentationsAbstracts in Arch. Mineralog. 49(1):1–271 (1993). Eight papers in Eur. J.Min. 6: 743–872 (1994)XIII21-23 Jun.1995Sitges (Inst. Cien. Terr. “JaumeAlmera” CSIC, Barcelona), SpainC. Aroya, A. Canals, J. García-Veigas,E. Cardellach150 presentationsAbstracts in Bol. Soc. Esp. Mineral.18(1): 1–301 (1995).Fourteen papers in Eur. J. Min. 8:879–1096 (1996)XIV1-4 Jul.1997Ecoles des Mines, Nancy, FranceM. Cathelineau, J. Dubessy, M.-C.Boiron, J. Pironon192 presentationsAbstracts in XIV ECROFI AbstractsVolume, 365 pp. (1997), CREGU,Nancy. Twelve papers in Eur. J. Min.10: 1095–1251 (1998)XV21-24 Jun.1999Geoforschungszentrum (GFZ)Potsdam, GermanyV. Lüders123 presentations (47 oral)Abstracts in Terra Nostra 99/6: 1–332 (1999).XVI2-4 May2001Universidade do Porto, PortugalF. Noronha132 presentations (47 oral)Abstracts in Memórias 7: 1–485(2001), Depto. de Geologia,Universidade do Porto. Twelvepapers in special issue of Chem.Geol. 194: 3–244 (2003)XVII5-7 Jun.2003Eötvös University, Budapest, HungaryCsaba Szabo125 presentations (48 oral)Abstracts in Acta Mineralogica-Petrographica 2: 1–236 (2003), ActaUniversitatis Szegediensis.Eleven papers in special issue ofChem. Geol. 223: 3–178 (2005)4

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 5XVIII6-9 Jul.2005Universitá degli Studi, Siena, ItalyM.-L. Frezzotti, F. Tecce, L. Dallai,C. Ghezzo184 presentations (88 oral)Abstracts on CD. Fourteen papers inspecial issue of Chem. Geol., 237:233–465 (2007)XIX17-20 Jul.2007Universität Bern, SwitzerlandL.W. Diamond, T. Pettke130 presentations (56 oral)5

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 77

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 9ECROFI-XIX SCIENTIFIC PROGRAMMETimes show start of slots; Presenters’ names are underlined; O denotes “oral”, P denotes “poster”DAY 1: TUESDAY 17 JULY08:15 Opening of ConferenceORAL: Theoretical Studies08:30 O-1 Perfetti E., Dubessy J., Thiéry R.An equation of state based on molecular interactions.Application to modelling of liquid-vapour phase equilibria(PVTX properties) of H 2S, H 2O and H 2O-gas (H 2S, CO 2, CH 4)systems08:45 O-2 Duan Z., Mao S. Equation of State applied in the study of fluid inclusions09:00 O-3 Bakker R.J. Bulk-diffusion of fluids through quartz: experimentalevidence?09:15 Session DiscussionORAL: Experimental I: Synthetic Fluid Inclusions09:30 O-4 Simon A.C. Pettke T. Platinum solubility in a vapor – brine – melt assemblage09:45 O-5 Dubois M., Coquinot Y., Castelain Phase relationships in the H 2O-NaCl-LiCl system: A synthesisT., Monnin C., Gouy S., Goffé B.10:00 O-6 Painsi M., Diamond L.W. New P–V–T andT hdata from synthetic fluid inclusions for 6mass% aqueous NaCl solution + 21 mol% CO 210:15 O-7 Kotelnikova Z.A., Kotelnikov A.R. Properties of sodium sulfate solution under high temperatureand pressure: a study of synthetic fluid inclusions10:30 Session Discussion10:45 Refreshments BreakORAL: Magmatic-Hydrothermal Ore Deposits I11:15 O-8 Heinrich C.A. (KEYNOTE) From picograms in bubbles to megatons in rocks11:45 O-9Lüders V., Romer R.L., Gilg H.A.,Fluid origin and evolution at the Sweet Home Mine (Alma,Bodnar R.J., Pettke T.Colorado) – a poor cousin of the giant Climax molybdenumdeposit12:00 O-10 Conliffe J., Feely M., Selby D. Nature and timing of mineralising fluids during theAppalachian-Caledonian Orogeny12:15 Session Discussion12:30 Lunch BreakORAL: Diagenesis-I14:00 O-11 Goldstein R. H. (KEYNOTE) Fluid inclusions key in changing paradigms in carbonatediagenesis14:30 O-12 Blamey N.J.F., Ryder A.G., OwensP., Feely M., Naranjo-Vesga, J.F.Fluorescence lifetime measurements of single hydrocarbonbearingfluid inclusions14:45 O-13 Ridley J., Dutkiewicz A., GeorgeS.C., Volk H.Hydrocarbon-aqueous mixtures in syndiagenetic fluidinclusions15:00 Session DiscussionORAL: Tectonics15:15 O-14 Tarantola A., Diamond L.W.,Stünitz H.Effects of plastic deformation on fluid inclusions in quartz: anexperimental study9

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 1015:30 O-15 Siebenaller, L., Boiron M.-C.,Vanderhaeghe O., Jessell M.,Banks D.Fluid inclusion distribution associated to quartzmicrostructures: A record of the exhumation of the NaxosMetamorphic Core Complex (Cyclades, Greece)15:45 O-16 Invernizzi C. Fluid inclusion in HP/LT units of Southern Apennine (Italy): acontribution to burial/exhumation history16:00 O-17 Mullis J., Vennemann T., deCapitani C., Franz L.16:15 Session Discussion16:30 Refreshments Break17:00 Day 1 Poster SessionTheoretical StudiesFluid-rock interaction along the Glarus thrust at Lochseiteand its impact on calc-mylonite formation and thrusting.P-1 Becker S.P., Bodnar R.J. Interpretation of fluid inclusions that homogenize by halitedisappearanceP-2 Fall A., Bodnar R.J., Reynolds T.J. Precision of thermal history reconstruction with fluidinclusionsP-3 Pernot N., Dubois M. GEOPROFI: An evolutionary software to calculate inclusionisochores from equations of stateP-4 Driesner T., Heinrich C.A. SoWatFlinc – a program for the computation of accurate fluidproperties in the system H O-NaCl2Experimental IP-5 Bali E., Audétat A. Synthetic fluid inclusions in rutile: a new technique to studymantle fluidsP-6 Bell A.S., Simon A.C. An Experimental Investigation of PGE Solubilities in Basalt –Vapour – Brine – Oxide – Sulfide AssemblagesP-7 Sekine K., Hayashi K. A bi-axial loading testers equipped heating microscope stage:Investigation on stress controlled decrepitation crackP-8 Spandler C., Mavrogenes J.,Hermann J.Diagenesis IExperimental constraints on element mobility from subductedsediments using high-P synthetic fluid/melt inclusionsP-9 Canals À., Piqué À., Grandia F. A new look at old data: microthermometric data of a fluoriteveinP-10 Dutkiewicz A., Ridley J., GeorgeS.C., Mossman D.J., Volk H.Oil-bearing fluid inclusions associated with thePalaeoproterozoic Oklo natural fission reactors, GabonP-11 Fintor K., Tóth T.M., Schubert F. Fracture cementation of the Baksa Gneiss Complex,Pannonian Basin: Traces of paleofluids of extremely diverseoriginP-12 Jarmolowicz-Szulc K. Hydrocarbon inclusions in quartz – questions and answersP-13 Prokofiev V.Yu., Melnikov F.P., Colloid solutions within fluid inclusions in chalcedonySelector S.L., Ezhov A.A., TrubkinN.V.P-14 Ramos-Rosique A., Levresse G.,Tritlla J., Jiménez Sandoval S.PVTx modelling of fluid inclusions in diamond quartz crystalsfrom the Sierra Madre Oriental, Southeast MexicoP-15 Szabó B., Schubert F., Tóth T.M. Traces of hydrocarbon migration recorded by pore-fillinganalcime of a fractured metabasalt complexTectonicsP-16 Hennings S., Vollbrecht A., vanden Kerkhof A.M., Hein U.F.Healed microcracks in late Variscan granites – comparisonbetween the NE Bavarian Basement and the Harz Mountains(Germany)10

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 11P-17 Tecce F., Rossetti F., Olivetti V.,Bouybaouenne M.L.Fluid-rock interaction along a crustal shear zone: results froma fluid inclusion study on the Filali unit, Rif chain (Morocco)P-18 Bento dos Santos T.M., MunháJ.M.U., Tassinari C.C.G., NoronhaF.M., Guedes A., Fonseca P.E.,Oxygen fugacity and CO 2– N 2fluid inclusions as remnants offluid and geodynamic evolution of Ribeira Fold Belt, SEBrazilDias Neto C., Dória A.P-19 Heijboer T., Mullis J., Amacher P.,Vennemann T.Fluid inclusion investigations on fissure minerals from theGotthard NEAT base tunnel (Central Alps).P-20 Mullis J., Tarantola A. The application of fluid inclusions to fluid geochemistry andgeothermobarometry in diagenetic and low-grademetamorphic rocks in the external parts of the Central AlpsNovel ApplicationsP-21 Coquinot Y., Dubois M.,Masalehdani M., Naze N.,Potdevin J.-L.P-22 Ruggieri G., Boschi C., Dallai L.,Dini A., Gianelli G.A fluid inclusion study in thenardite and associatedmineralisations from burning coal waste heap, Avion,Northern FranceThe carbonated serpentinites in Tuscany (Italy), a geologicalanalogue of carbon dioxide sequestration: information fromfluid inclusions data.DAY 2: WEDNESDAY 18 JULYORAL: Experimental II: Diamond Anvil Cell08:30 O-18 Schmidt C. (KEYNOTE) The hydrothermal diamond-anvil cell: a versatile tool to studyaqueous fluids in situ at high pressures and temperatures09:00 O-19 Sanchez-Valle C., Bass J.D. Equation of state of H 2O from sound velocity measurementsin the diamond anvil cell by Brillouin scattering spectroscopy09:15 Session DiscussionORAL: Analytical Methods: Non-Destructive09:30 O-20 Baumgartner M. Coquinot Y.,Bakker R.J.09:45 O-21 Rickers K., Bleuet P., Cauzid J.,Lüders V.10:00 O-22 James-Smith J., Brugger J.,Cauzid J., Hazemann J.-L., Liu W.,Proux O., Testemale D., PhilippotP., Williams P.10:15 O-23 Stoller P., Krüger Y., Ricka J.,Frenz M.10:30 Session Discussion10:45 Refreshments BreakORAL: Magmatic-Hydrothermal Ore Deposits IIModifications on the Raman spectra of pure water and brinesin synthetic fluid inclusions caused by the quartz host mineralElemental partitioning during sub-critical phase separation:evidence from SR XRF, fluotomography and X-ray absorptiontechniques of liquid-vapour fluid inclusion assemblages fromthe granitic Torres del Paine Complex, PatagoniaArsenic Speciation in fluid inclusions from gold depositsusing X-ray Absorption Spectroscopy from ambient tohomogenisation temperaturesVolumetric imaging of fluid inclusions in quartz using secondharmonic generation microscopy11:15 O-24 Hanley J.J., Spooner E.T.C., HartC.J., Heinrich C.A., Guillong M.Evidence for sulfide melt oxidation and metal-rich aqueouscarbonicfluid exsolution in the intrusion-related Au system atFort Knox, Alaska11

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 1211:30 O-25 Harris C.R., Pettke T., HeinrichC.A., Kleine T.11:45 O-26 Driesner T., Kostova B., HeinrichC.A.12:00 O-27 Banks D., Rice C., Steele G.,Boyce A., Fallick T.12:15 Session Discussion12:30 Lunch Break14:00 Day 2 Poster SessionTracing the magmatic evolution of Cu-Au porphyry systemsby LA-MC-ICPMS analysis of Pb isotopes in fluid and meltinclusionsCombining numerical simulation of hydrothermal processesand fluid inclusions: quantitative reconstruction of ore-formingprocessesThe formation of the World’s largest silver deposit, CerroRico, BoliviaAnalytical Methods I: Non-destructiveP-23 Bakker R.J., Baumgartner M.,Coquinot Y.Experimental Raman spectra of salt hydrates in fluidinclusionsP-24 Cauzid J., Bleuet P., Martinez- Fluid inclusion analysis using synchrotron radiationCriado G., James-Smith J.,Hazemann J., Testemale D., ProuxO., Brugger J., Liu W., Rickers K.,Philippot P.P-25 Kyle J.R., Ketcham R.A.High resolution X-ray computed tomography of fluidinclusionsP-26 Krüger Y., Stoller P., Ricka, J.,Frenz M.Femtosecond lasers in fluid inclusion analysis: Overcomingmetastable phase statesAnalytical Methods II: Laser-Ablation ICPMSP-27 Allan M.M., Guillong M., Meier D.,Hanley J., Heinrich C.A., YardleyB.W.D.P-28 Courtieu C., Guillaume D., SalviS., Freydier R.P-29 Krause P., Brune J., Fricker M.,Günther D.P-30 Vry V., Wilkinson J., Jeffries T.LA-ICP-MS analysis of inclusions: Improved data reductioncapabilitiesApplication of Femtosecond Laser Ablation ICP-MS of fluidinclusions to the study of ore depositsAdvantages of an improved high performance 193 nm laserablation system for the direct analysis of fluid InclusionsValidation of 213 nm Laser Ablation Inductively CoupledPlasma Mass Spectrometry (LA-ICP-MS) for QuantitativeSingle Fluid Inclusion Analysis: A Calibration StudyP-31 Zacharias J., Wilkinson J. ExLAM 2000: Excel VBA application for processing oftransient signals from laser ablation (LA-ICP-MS) of fluidinclusions and solid phasesMagmatic-Hydrothermal Ore Deposits I + IIP-32 Badanina E.V.C., Gordienko V.V.,Thomas R., Syritso L.F.The cesium-rich melt from quartz-pollucite lens, Vasin Myl’kpegmatite, Kola peninsula, RussiaP-33 Dowman E., Rankin A., Wall F. Fluid and solid inclusion evidence for late-stage mobility ofzirconium, titanium and REE in carbonatite systemsP-34 Jaques L., Noronha F., Bobos I. Fluids associated with episyenitization of Variscan posttectonicGerês granite, northern PortugalP-35 Sokolov S.V. Phase composition of melt inclusions in monticellite andniocalite from carbonatites of the Oka complex (Quebec,Canada): confirmation of silicate–carbonate liquidimmiscibility12

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 1417:00 O-31 Berkesi M., Hidas K., Szabó C. CO 2-rich fluid inclusions in upper mantle derived xenoliths(Western Hungary, Tihany): microthermometry and Ramanmicrospectroscopic study17:15 Session DiscussionDAY 3: THURSDAY 19 JULYORAL: Analytical Methods: Laser Ablation ICPMS08:30 O-32 Guillong M., Heinrich C.A. LA-ICP-MS analysis of inclusions: Improved ablation anddetection08:45 O-33 Mutchler S., Fedele L., Bodnar R. AMS a new software package for reduction of Laser AblationICPMS data09:00 O-34 Zajacz Z., Halter W.09:15 Session DiscussionORAL: Mineral DepositsLA-ICPMS analyses of silicate melt inclusions in coprecipitatedminerals: Quantification, data analysis andmineral/melt partitioning09:30 O-35 Xue G., Marshall D. Formational conditions for the Dyakou emerald occurrence,Southeastern Yunnan, China09:45 O-36 Boiron M.-C., Cathelineau M.,Dubessy J., Fabre C., Boulvais P.,Banks D.Na-Ca-Mg rich brines and talc formation in the giant talcdeposit of Trimouns (Pyrenees): Fluid inclusion chemistryand stable isotope study10:00 O-37 Hurai V., Lexa O., Schulmann K.,Prochaska W., Chovan M.10:15 Session Discussion10:30 Refreshments BreakORAL: “Non-Magmatic” Ore Deposits11:00 O-38 Richard, A., Boiron, M,-C,,Cathelineau M., Boulvais P., BanksD., Mercadier J., Cuney M.11:15 O-39 Thorne W., Hagemann S., BanksD.11:30 O-40 Figueiredo e Silva R. C.,Hagemann S., Lobato L.M., BanksD.11:45 O-41 Petersen K.J., Hagemann S.G.,Neumayr P., Walshe J., Banks D.,Yardley B.12:00 Session Discussion12:15 Lunch BreakFluid inclusion and stable isotope constraints on the origin ofhydrothermal veins in the Gemeric Unit (WesternCarpathians)Fluid inclusion and stable isotope evidence for percolation ofbasinal brines in the Athabasca Basement around the RabbitLake, Eagle Point, P-Patch and Millenium unconformityrelateduranium deposits, CanadaHypogene fluid responsible for the transformation of BIF tohigh-grade iron ore (>65 wt %); insights from the 4 Eastdeposit, Paraburdoo, Western AustraliaHydrothermal fluid characteristics and evolution for the giantCarajas North Range iron deposits, BrazilIn-situ Laser ICPMS analyses of pre-, syn-, and post-goldhydrothermal fluids in the Kambalda Gold Camp, Yilgarncraton, Western Australia14

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 15ORAL: Magmatism13:45 O-42 Fedele L., Cannatelli C., Spera F.,Bohrson W., De Vivo B., Lima A.,Bodnar R.J.14:00 O-43 Schoenenberger J., Markl G.14:15 O-44 Graser G., Potter J., Koehler J.,Markl G.14:30 Session DiscussionGaining insights on magma evolution using melt inclusionsdata and thermodynamic modeling: two eruptions fromCampi Flegrei (Campania, Italy)The fluid evolution of the Motzfeldt intrusion – constraints ofagpaite genesisIsotopic, major, minor, and trace element geochemistry oflate stage fluids in the Ilímaussaq alkaline complex, SouthGreenlandORAL: Tribute to Ed Roedder14:45 O-45 Bodnar R.J. (KEYNOTE) The many contributions of Edwin Woods Roedder (1919-2006) to fluid and melt inclusion research15:15 Departure for Banquet EventsDAY 4: FRIDAY 20 JULYORAL: Epithermal Ore Deposits09:00 O-46 Simmons S.F., Brown K.L.(KEYNOTE)The concentrations and fluxes of gold in subaerialhydrothermal systems of New Zealand and Papua NewGuinea09:30 O-47 Kodera P., Lexa J., Fallick A.E. Paleohydrology and source of fluids of the Kremnica lowsulfidationepithermal Au-Ag deposit09:45 O-48 Kouzmanov K., Vennemann T.,Putlitz B., Baumgartner L., SkoraS., Heinrich C.A.Magmatic fluids in high-sulfidation epithermal veinsoverprinting a porphyry copper system: Stable isotope studyof pyrite-hosted fluid inclusions10:00 O-49 Lledo H.L., Cline J.S. The Searchlight Mining District: Linking low sulfidationepithermal mineralization with an underlying granitic plutonusing fluid inclusions10:15 Session Discussion10:30 Refreshments Break11:00 Day 4 Poster SessionDeep FluidsP-51 Dégi J., Török K., Kodolányi J.,Abart R.Changes of oxidation state in lower crustal garnet granulites:the role of CO 2-rich fluidsP-52 Fonarev V.I., Vasyukova O.V.,Vapnik Y.Fluid regime of the metamorphism in the Kolvitsa gabbroanorthositemassif (Northeast Baltic Shield): fluid inclusiondataP-53 Herms P., Bakker R.J., John T.,Schenk V.Fluid inclusions as indicator of fluid migration in thesubducting slab: an example from the eclogites of theRaspas Complex, EcuadorP-54 Hurai V., Janák M. Expulsion of fluids from anatectic melts duringdecompression of HP/UHP garnet-kyanite gneiss fromPohorje Mts., SloveniaP-55 Török K., Dégi J., Marosi G. Ultrahigh temperature melting of biotite in CO 2richenvironment and formation of orthopyroxene-garnetplagioclaserocks in the lower crust: A xenolith example fromthe Bakony-Balaton Highland Volcanic Field (W-Hungary)15

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 16“Non-Magmatic” Ore DepositsP-56 Barakat A., Marignac C., BoironM.C., Cathelineau M.Deciphering superimposed Panafrican and Variscanhydrothermal events through a fluid inclusion study in relationwith deformation: the gold occurrence of Ourika (WesternHigh Atlas, Morocco)Characterisation of the fluids in black-carbonate lithologiesfrom an auriferous shear-zone (NW Portugal)P-57 Dória A., Guedes A., Ribeiro M.A.,Ramos J.F.P-58 Dubois M., Salvi S., Béziat D. Peculiar fluids at the origin of orogenic gold deposits inBurkina Faso, West AfricaP-59 Lawrence D.M., Rankin A., Treloar Fluid inclusion and mineralogical studies of orogenic goldP., Harbidge P.deposits in the Loulo district, Mali, West Africa: criteria forP-60 Zachariás J., Sulcová, B., HrstkaT., Pudilová M.assessing a metamorphic or magmatic originFluids associated with early Au-Bi-Te-S and late Au-Ag-Bi-Sb-Pb-S mineralization: an example from the Kasejovice golddistrict, Bohemian Massif, Czech RepublicP-61 Prokofiev V.Yu., Baksheev I. A. Fluid inclusion study in minerals at the orogenic Berezovskygold deposit, Central Urals, RussiaP-62 Sezerer Kuru G. Fluid inclusion characteristics and isotope analyses of theSavciliebeyit (Kaman-Kırsehir) gold-bearing quartz veins inCentral AnatoliaP-63 Zoheir B., Moritz R. Fluid evolution and gold deposition conditions of the El-Sidgold deposit, EgyptP-64 Staude S., Wagner T., Markl G. Post-Variscan hydrothermal fluids in the Schwarzwald(Germany): fluid mixing without a visible mixing trend in fluidinclusion dataP-65 Bozkaya G., Gokce A., GrassineauN.V.P-66 Luptáková J., Biron, A., Hurai V.,Chovan M., Prochaska W.P-67 Tritlla J., Levresse G., LamadridH., Bourdet J., Corona-Esquivel R.P-68 Veselinovic-Williams M., TreloarP.J., Rankin A.H., Strmic-PalinkasS.Mineral DepositsFluid-inclusion and stable isotope characteristics of theArapuçandere (Karaköy-Yenice-Çanakkale) Pb-Zn-Cudeposits, Biga Peninsula, NW TurkeyHydrothermal fluids in the base-metal vein mineralization inthe Nízke Tatry Mts. (Western Carpathians, Slovakia)Basinal brines as witnesses of fluid flow changes in acompressional-to-extensional tectonic regime: the case of ElTule stratabound F-Sr deposit, NE MéxicoA preliminary fluid inclusions study of the Belo Brdo Pb-Zn(Ag) deposit, northern KosovoP-69 Koehler J., Markl G. Fluid geochemistry in the Ivigtut cryolite deposit, SouthGreenlandGeothermal SystemsP-70 Simmons S.F., Simpson M.P.,Reynolds T.J.Analytical Methods IIIP-71 Fabre C., Boiron M.-C., DubessyJ.P-72 Potter J., Zubowski S.M., SpoonerE.T.C., Bray C.J., Longstaffe F.J.,Gibson H.L.The significance of clathrates in fluid inclusions in theBroadlands-Ohaaki geothermal system, New ZealandMineral precipitations and fluid chemistry variations duringLIBS ablationAn online GC-irMS crushing technique for stable isotopeanalysis of trace gases in aqueous-dominated fluidinclusions: An example from the Noranda VMS District,Quebec, Canada16

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 17P-73 Audétat A. A new approach for measuring salinities of aqueous fluidinclusions that contain compressed gasesP-74 Burlinson K. An updated understanding of acoustic emission decrepitation12:30 Lunch BreakORAL: Deep Fluids14:00 O-50 Scambelluri M., Pettke T., VanRoermund H.L.M. (KEYNOTE)14:30 O-51 Van den Kerkhof A. M., Harlov D.,Johannsson L.14:45 O-52 Frezzotti M. L., Tecce F., PerucchiA., Ferrando S., Compagnoni R.15:00 Session DiscussionOn deep subduction fluids: the fluid and solid multiphaseinclusions in eclogite-facies mineralsFluid evolution of the igneous Varberg-Torpa charnockitegranitecomplex, SW SwedenInfrared imaging of H 2O concentrations in nominallyanhydrous minerals containing fluid inclusions, usingsynchrotron radiation15:15 Refreshments BreakORAL: Diagenesis-II15:45 O-53 Pierron O., Cathelineau M., BoironM.-C., Fourcade S., Richard L.16:00 O-54 Dublyansky Y., Borsato A., FrisiaS., Dallai L., Spötl C.16:15 O-55 Garofalo P.S., Günther D., Forti P.,Lauritzen S.-E., Constantin S.16:30 O-56 Gilg H. A., Krüger Y., Stoller P.,Frenz M., Boni M.16:45 Session DiscussionDrastic changes in fluid nature and source during latediagenesis (celestite-quartz veins) of the eastern part of theParis basin: evidence from Raman spectroscopy and isotopegeochemistryAnalysis of stable isotope properties of fluid inclusion waters:development of method and a case studyThe fluids of the giant selenite crystals of Naica (Chiuhahua,Mexico)Temperatures in sulfide oxidation zones: microthermometryof monophase aqueous fluid inclusions and stable isotopesystematics17:00 Plenary Discussion: Announcements of next venues of ECROFI, ACROFI, PACROFI, etc.18:00 Closure of Conference17

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 18Abstracts ofOral Presentations18

O1European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 20An equation of state based on molecular interactions. Application tomodelling of liquid-vapour phase equilibria (PVTX properties) of H 2S,H 2O and H 2O-gas (H 2S, CO 2, CH 4) systemsPerfetti, Erwan*, Dubessy*, Jean, and Thiéry Régis***UMR G2R et CREGU, Nancy Université, BP-239, 54506-Vandoeuvre-lès-Nancy, France* UMR LMV 6524, Université Blaise Pascal, 5 rue Kessler, F-63038 Clermont-Ferrand CedexModelling fluid-rock interactions, fluid mixingand unmixing, in geological processes requires robustequations of state (EOS) which must be applicable tosystems containing water, gases and salts over abroad range of temperatures and pressures. Hydrogenbonding, dipolar interactions, charge-charge andcharge-dipole interactions, are the main molecularinteractions in addition to the weak Van der Waalsinteractions. Cubic equations of state based on theVan der Waals theory allow simple modelling fromthe critical parameters of non-polar and neutral fluidcomponents with only Van der Waals interactions.However, the accuracy of such equations is poorwhen water is a major component of the fluid sinceneither association through hydrogen bonding nordipolar interactions are accounted for. In this paper, anew EOS taking into account these interactions ispresented for H 2O-gas systems.The Helmholtz energy of a fluid may bewritten as the sum of different energetic contributionsas a consequence of the factorization of the canonicpartition function. The model developed in this workconsiders three contributions. The first contributionrepresents the reference Van der Waals fluid which ismodelled using a Soave-Redlich-Kwong cubic EOS.The second contribution accounts for associationthrough hydrogen bonding and is modelled fromStatistical Association Fluid theory. The thirdcontribution corresponds to dipolar interactions andis established by the Mean Spherical Approximation(MSA) theory. For the pure H 2S system, theHelmholtz free energy contains only the referencefluid contribution and the dipolar interactions. Themolecule diameter and dipolar moment are deducedfrom fitting PVT experimental data along the saturationline. Values are coherent with the range ofexperimental data The model is a significantimprovement compared to the SRK equation alone.For pure water, dipolar interactions becomesignificant as hydrogen bonding decreases withincreasing temperature, and therefore suchinteractions must be considered. Hydrogen bondingis modelled using a four-site model. The resultingCPAMSA equation has six adjustable parameters.This equation results in a better reproduction of thethermodynamic properties of pure water along thesaturation line (pressure and molar volume of theliquid phase) than those obtained using cubic EOSequations or CPA equations taking into account Vander Waals interactions and association but neglectingdipolar interactions. Extrapolation to 10 kbar fortemperatures below 400 °C is satisfactory. Thepressure and temperature of the critical point areslightly underestimated because such theory is notcompatible with the fluctuation density correlations.Mixing rules are required for the referencefluid contribution, and for the dipolar moment in thecase of two distinct dipolar molecules such as H 2Oand H 2S. Classical mixing rules of cubic EOS havebeen chosen with a binary interaction parameterdeduced from fitting P-V-T-X experimental data ofonly the liquid phase. Calculated liquid-vapour phaseequilibria in the H 2O-H 2S, H 2O-CO 2, H 2O-CH 4systemsare reproduced within 7% of experimental errors. Thecalculated composition of the vapour phase isconsistent with experimental data. Binary interactionsparameters are close to zero except for the H 2O-CH 4system. This suggests that the model properly takesinto account the interactions in the H 2O-H 2S, H 2O-CO 2systems and that the induced moment is probablyneglected in the H 2O-CH 4system. The calculatedcritical curve of the H 2O-H 2S system is similar to thecritical curve of H 2O-CO 2, H 2O-CH 4systems and isnot continuous, such as in for the H 2O-NH 3system.In conclusion, this approach, which takesinto account major molecular interactions betweenfluid components, is probably the route to establishrelevant equations of state for geological fluids.Nevertheless, our model needs to be optimised,especially in the single-phase field and above thecritical point. The next step will be to introduce saltsusing the MSA theory.20

O2European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 22Equation of State applied in the study of fluid inclusionsDuan Zhenhao and Mao Shide*Departamento de 1 State Key Laboratory of Lithospheric Evolution, Institute of Geology and Geophysics,Chinese Academy of Sciences, Beijing, 100029, ChinaEquation of state (EOS) is very important inthe interpretation of fluid-inclusion data because itcan be used to derive homogenization conditions,isochores, and internal pressures of fluid inclusions.There are many equations or thermodynamic modelsused in the study of fluids, but most of them lackconsistent accuracy over a meaningful T-P space,yielding unreliable predictions. Therefore, cautionmust be taken in choosing or developing accurateEOS or models to study fluid inclusions. The objectiveof this study is to apply the best EOS or modelsdeveloped by previous researchers or us to give themost accurate calculation of homogenizationtemperature-pressure and isochores. These programscan be downloaded from(www.geochem-model.org/programs.htm)for convenient use.For pure fluid like H 2O, CO 2, CH 4, O 2, N 2, C 2H 6or H 2S, the best EOS in terms of precision andapplicable range are summarized in Table 1. Listed inTable 2 are the T-P ranges and references for H 2O-NaCl system and H 2O-NaCl-CH 4(including H 2O-CH 4)systems. Detailed information can be seen from thereferences. Other systems, such as CO 2-H 2O andCO 2-H 2O-NaCl are still under development. Once thehomogenization temperature and the compositionare determined for an fluid inclusion, the internalpressure of the fluid inclusion and the isochres canbe calculated. Isochores of other systems listed inTables 1 and 2 can also be drawn from our website.Table 1: EOS of pure fluidsFluidsH 2OTemperature(K)Pressure(bar)273-1273 0-100001273-2573 0-100000CO 2216.592-1100 0-80001100-2573 0-100000CH 490.694-625 0-10000673-2573 0-100000C 2H 690.352-625 0-700O 254.361-1000 0-820N 263.151-1000 0- 22000H 2S 187.67-760 0- 1700References(Wagner andPruß, 2002)(Duan andZhang, 2006)(Span andWagner,1996)(Zhang andDuan, 2005)(Setzmannand Wagner,1991)(Zhang et al.,2007)(Friend et al.,1991)(Schmidt andWagner, 1985)(Span et al.,2000)(Sakoda andUematsu,2004)Table T 2: EOS of HO-NaCl and H O-NaCl-CH2 2 4systemsSystems Temperature(K) Pressure(bar) References273-573 Ps-1000(Mao andDuan, 2007)(Spivey etH 2O- 273-548 1000-2000al., 2004)NaCl(Anderko573-1200 Ps-5000 and Pitzer,1993)H 2O- 273-523 Ps -2000CH 4573-1200 Ps -5000NaCl-(Duan andMao, 2006)(Duan et al.,2003)Note: Ps: vapor pressure of the solutions; xNaCl:mole fraction of NaCl assumed at undissociatedstate; H 2O–NaCl–CH 4system: the maximal molalityof CH 4not over its solubility.22

O3European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 24Bulk-diffusion of fluids through quartz: experimental evidence?Bakker, Ronald J.Mineralogy & Petrology, Institute of Applied Geosciences and Geophysics, University of Leoben, Peter-Tunner-Str. 5, 8700 Leoben, AustriaRe-equilibration of fluid inclusions is of majorimportance to the interpretation of compositional anddensity analyses. Mainly rock deformation andmetamorphism may change the properties ofinclusions. Processes that control re-equilibrationhave been experimentally investigated, but do notprovide conclusive principles about the behaviour offluid inclusions.Diffusion is a mechanism that may change theproperties of fluid inclusions. Especially, the mobilityof H 2O through quartz is an important research topicin geosciences. In this study, the availableexperimental work and diffusion models arescrutinized and directly applied to fluid inclusionbehaviour. A new mathematical diffusion model isdeveloped which can be applied to randomlydistributed fluid inclusions in a quartz crystal.Diffusion is characterized by concentrationprofiles in quartz and can be expressed in anArrhenius-plot to illustrate its temperature dependence.The parameters that define diffusion are solubility(equilibrium), diffusion coefficients, activation energy,chemical potential gradients (or fugacity) and thenature of diffusing species (e.g. neutral or charged),besides temperature and pressure. The analyticalmethods include the measurements of isotopicvariations of oxygen and hydrogen in quartz with IRspectroscopy or secondary ion MS. The uncertaintiesin knowledge, estimation of the parameters and theexperimental method result in highly imprecisenumbers on diffusion of H 2O through quartz. Moreover,experimentally estimated diffusion coefficients areonly based on a limited number of studies thatassume one-dimensional diffusion.The solubility of water in quartz is a highlyambiguous parameter because water can be presentin a variety of appearances (as molecules and ions).In this study, molecular H 2O in quartz is assumed tobe present as extrinsic impurities in a limited spacewithin the crystal lattice and its diffusion is responsiblefor the alteration of fluid inclusions. Consequently,solubility decreases with increasing pressure, incontrast to solubility expressed in charge compensateddefect concentration.The water concentration in a quartz grain ismainly defined by pore fluids, and gradients due tochanges in pore fluid properties can be expressedaccording to an infinite external source model at aspherical quartz grain (3D-diffusion). Fluid inclusionshave only a minor effect on this concentration profiledue to their relative small sizes. Diffusion into and outof fluid inclusions is modelled according to aninstantaneous point source model, in which the pointsource is a sphere, and the background concentrationin the quartz is defined according to the previouslymentioned diffusion model.Re-equilibration rates of synthetic fluidinclusions calculated with diffusion coefficientsobtained from previous studies are extremely slow atan experimental time-scale, and cannot result in theobserved alterations of synthetic fluid inclusions (seeBakker & Diamond, 2003). Synthetic fluid inclusionsare most probably connected to numerous crystaldefects, such as dislocation and nano-cracks, whichenhance fluid transport through the crystal. The valueof the diffusion coefficient is, therefore, questionable.The properties of fluid inclusions have not yet beenused to experimentally estimate diffusion coefficientsof fluid components through quartz. Their alterationscan be directly used to obtain diffusion models.REFERENCESBakker R.J., Diamond L.W. (2003) Acta Mineral.Petrogr. 2: 17-1824

O4European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 26Platinum solubility in a vapor – brine – melt assemblage.Simon, Adam C. * and Pettke, Thomas ***Department of Geoscience, University of Nevada-Las Vegas, Las Vegas, NV 89154-4010, U.S.A.**Institute of Geological Sciences, University of Bern, Baltzerstrasse 1+3, CH-3012, Bern, SwitzerlandBoudreau et al. (1986) proposed an orthomagmaticmodel for platinum-group-element (PGE)deposits associated with layered mafic intrusions.Since Boudreau’s initial publication, several groupshave attempted to constrain the partitioning behaviorof PGEs at magmatic conditions (cf. Hanley et al.,2005). However, there is yet no consensus on thebehavior of PGEs at high P and T. The new datapresented here will hopefully contribute to resolvingthis debate.In this study, we performed experiments toconstrain the partitioning of Pt in a sulfur-free vapor– brine – rhyolite melt assemblage. All runs wereperformed at 140 MPa, 800°C and fO 2= NNO. Fluidinclusions were trapped in quenched silicate melt asthe latter cooled through the glass transitiontemperature (Fig 1). Thus, these inclusions trappedfluid which had equilibrated with the system for theentire run duration. The concentration of Pt in fluidinclusions was measured by using LA-ICPMS.Platinum solubility data (± 1σ) are given in Table 1.The number of inclusions analzyed, n, is provided foreach run.Figure 1: Glass-hosted synthetic fluid inclusions.Daughter crystals of AgCl in vapor.The measured solubility data were used tocalculate Nernst-type partition coefficients (± 1σ;Table 2) which are strictly valid only at the experimentalconditions described herein. These data are useful indescribing the relative roles of vapor and brine toscavenge and transport Pt, but they are only a guideand care must be exercised when extrapolating toother PTX conditions. Equilibrium was evaluated bynoting the consistency of Pt concentrations in fluidinclusion assemblages and the variance of calculatedNernst-type partition coefficients with run times up to560 hours. Vapor/brine and vapor/melt partitioncoefficient values remain relatively constant. Thebrine/melt partition coefficient values exhibit morescatter; we suggest that this order of magnitudevariance may be a function of the presence ofaccidentally trapped Pt nuggets.In spite of the variance of Pt concentrations inbrine, model calculations using these partitioncoefficients suggest that aqueous vapor and brinecan scavenge sufficient quantities of Pt (and byanalogy other PGEs) to form large-tonnage PGE-richhydrothermal ore deposits.Run Hours Vapor (n) Brine (n) Melt (n)4 206 0.9± 0.4 (9)5 110 1.0± 0.7 (6)6 377 0.2± 0.04 (8)7 205 3.0± 1.9 (6)8 560 0.7± 0.2 (5)14 160 1.2± 0.4 (9)3.5 ± 0.6(4)5.4 ± 2.6(5)0.32 ± 0.05(16)0.53 ± 0.09(16)11 ± 3 (8) 0.32 ± 0.03(17)45 ± 17(3)Table 1. Experimental Pt solubility.0.30 ± 0.09(16)22 ± 7 (5) 0.20 ± 0.05(6)4 ± 1 (7) 0.20 ± 0.03(20)Run D v/b D v/m D b/m4 0.2 ± 0.15 3 ± 1 11 ± 35 0.2 ± 0.2 2 ± 1 10 ± 56 0.1 ± 0.05 9 ± 7 150 ± 737 0.1 ± 0.05 1 ± 0.3 63 ± 238 0.03 ± 0.01 4 ± 1 110 ± 4214 0.3 ± 0.1 6 ± 2 21 ± 7Table 2. Nernst-type partition coefficients.REFERENCESBoudreau AE, Mathez EA, McCallum IS. (1986) J.Petr., 27, 967-968.Hanley, J.J., Pettke, T., Mungall, J.E. andSpooner, E.T.C. (2005) GCA, 69, 2593-2611.26

O6European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 30New P-V-T andT hT data from synthetic fluid inclusions for 6 mass%aqueous NaCl solution + 21 mol% CO 2Painsi, Monika* and Diamond, Larryn W.**Institute of Geological Sciences, University of Bern, Baltzerstrasse 1+3, 3012 Bern, SwitzerlandThe components CO 2, H 2O and NaCl aremajor constituents of aqueous fluids circulatingthrough rocks in a number of different geologicenvironments. Accordingly, much effort has beeninvested to qualitatively and quantitatively describethe phase behaviour of this system. To date, however,most experiments have been designed to constrainonly the phase boundaries between the homogeneousfluid and the coexisting liquid and gas phases. Fewstudies provide measurements of molar volumes.This is an undeniable gap for the fluid inclusionist,given that fluids once trapped in an inclusion behaveas an isochoric system. In this study we haveattempted to thoroughly investigate one isopleth ofthe ternary system (a mixture consisting of a 6mass% NaCl solution and 21 mol% CO 2) with respectto the above-mentioned requirements.For this purpose, we chose the synthetic fluidinclusion technique, in which a fluid of knowncomposition is sealed in a gold capsule together witha pre-fractured quartz rod. At experimental conditionsthese cracks heal and trap the surrounding fluid (e.g.Sterner & Bodnar, 1984). We condensed CO 2directlyinto capsules containing the NaCl solution. Oursyntheses were performed at temperatures andpressures ranging from 500 to 700 °C and 2000 to4000 bar, so as to trap a homogeneous, ternary fluid.The resulting inclusions were analyzed bymicrothermometry and Raman spectroscopy.Temperatures of four phase transition were measured:(1) the melting of CO 2, as check on its purity (inaddition to Raman spectroscopy), (2) the dissociationof clathrate, to verify the salinity, (3) the homogenisationof the two carbonic phases, which is diagnostic of thetotal molar volume of the inclusion when the bulkcomposition is known, and (4) the total homogenisationof the carbonic and aqueous phases. These dataallowed us to construct a set of isochores for thechosen isopleth and to define the P–Tboundaries ofmiscibility.A useful representation of the experimentalresults is shown in Fig. 1, from which one can directlyobtain the total homogenisation temperatures for agiven bulk molar volume of the investigated isopleth.The critical temperature of Schmidt and Bodnar(2000) is compatible with our observations, but ourresults show notable discrepancies with respect tothe study of Gehrig (1980), in which a large viewingcell was used to obtain isoplethic P–V m –T data.Fig. 1. Total homogenisation temperatures as afunction of bulk molar volume for the isoplethx(CO )= 0.2101, x(HO) = 0.7747 and x(NaCl) =2 20.0152.REFERENCESGehrig M. (1980) Doctoral dissertation, Univ.Karlsruhe.Krüger Y. (2001) Doctoral dissertation, Univ. of Bern.Schmidt C., Bodnar R.J. (2000) Geochim.Cosmochim. Acta 64:3853-3869Sterner S.M., Bodnar R.J.(1984) Geochim.Cosmochim. Acta 48:2659-266830

O7European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 32Properties of sodium sulfate solution under high temperature andpressure: a study of synthetic fluid inclusionsKotelnikova, Zoya A.* and Kotelnikov, Alexey R.***Institute of Geology of Ore Deposits, Petrography, Mineralogy, and Geochemistry, Russian Academy ofSciences, 35 Staromonetny, Moscow, 119017 Russia**Institute of Experimental Mineralogy, Russian Academy of Sciences, Chernogolovka, Moscow oblast’,142432 RussiaThe phase diagrams of aqueous solutions ofsilicates, aluminosilicates and many salts belong tothe P-Q type (critical phenomena occur both insaturated and undersaturated solutions). Their phasediagrams are additionally complicated by liquidimmiscibility phenomena.Previously, non-inert behavior of quartz wasobserved in equilibrium with a NaF-containing fluid.Quartz interacted with the fluid producing malladrate(Na 2SiF 6) and a sodium hydrosilicate. As a result, thealkalinity of the fluid increased.Accordingly, it was supposed that quartz willremain inert in Na 2SO 4solutions, because intermediatesilicate-sulfate compounds have never beenobserved. We synthesized fluid inclusions in quartzby trapping Na 2SO 4-containing solutions at 300–800ºC and 0.5–3.0 kbar. Ravich (1974) studied theNa 2SO 4–H 2O system up to the P-T parameters of theupper critical point Q. Our results at similar parametersappeared to be not in full agreement with his data.This can be explained by quartz-fluid interaction.All inclusions synthesized at the P-T conditionsof the upper two-phase area homogenized to liquid.We believe that this indicates that the upper part ofthe critical curve corresponds to the L 1=L 2equilibrium.Thus, this critical curve is not a continuation of theliquid=gas critical curve of the lower critical region,and it has its own metastable continuation to lowerP-T parameters. The phase diagram of such a binarysystem displays a metastable liquid immiscibilityfield, which may become stable in systems with ahigher number of components.We observed liquid immiscibility in a saturatedNa 2SO 4solution trapped in inclusions synthesizedunder the conditions of the upper heterogeneousfield. In three-phase inclusions (vapor-liquid-crystal)synthesized at 700 ºC and 2 kbar, the appearance ofa second liquid phase in equilibrium with vapor wasobserved at a temperature of 250 o C. The volume ofthis liquid phase increased up to a temperature of300 o C. The two liquids existed in the inclusions up tothe temperatures of their decrepitation (higher than400 o C). Liquid immiscibility was also observed ininclusions synthesized at 1 kbar and 700 o C.In order to confirm the fact of quartz interactionwith saline aqueous fluid, experiments were conductedunder the same P-T-X conditions but with the additionof albite. In these experiments, liquid immiscibilitytook place in undersaturated solutions (in two-phasevapor-liquid inclusions). The different character ofliquid immiscibility in inclusions synthesized with andwithout albite suggests that the presence ofaluminosilicate influences phase equilibria in thefluids. Thus we can conclude that quartz is not inert,and its presence increases the number of componentsin the system. The field of liquid immiscibility in theternary Na 2SO 4–H 2O–SiO 2system is stable. Theminimum temperature at which three non-crystallinephases may coexist in this system is 250 o C.A glass-like phase appeared in some inclusionssynthesized at 800 o C and 3 kbar. In our opinion, thisprovides compelling evidence for quartz–fluidinteraction. The glassy phase unmixes into twoliquids, and the coexistence of four equilibrium noncrystallinephases was observed in these inclusionsat temperatures of 220–300 o C.REFERENCESRavich, M.I. (1974) Water–Salt Systems at ElevatedTemperatures and Pressures. Nauka, Moscow [InRussian].32

O8European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 34From picograms in bubbles to megatons in rocksHeinrich, Christoph A.Department of Earth Sciences, Swiss Federal Institute of Technology, ETH Zürich, SwitzerlandTechniques for analysing trace elements inindividual fluid inclusions have built a bridge betweenstudies of ore metal solubility in the laboratory on onehand, and field investigations aimed at quantifyinggeochemical transport processes in large-scale geologicalsystems on the other. This talk will sum marisesome recent technical developments, but mainlyaims at stimulating a discussion on how to best utiliseour new technical possibilities to learn more abouttransport processes in large-scale geological systems.The subduction zone environment leading to giantporphyry-Cu-Mo-Au deposits provides the example:what can we learn, from microanalysis of ppmconcentrations of ore-forming elements in μm-sizedfluid and melt inclusions, about the formation of giantore deposits in which as much as 100 Mt of copperare accumulated by selective mineral precipitation?Fluid microanalysis has opened new approachesto experimental studies at high pressures andtemperatures. Phases that are unquenchable ordifficult to characterise in situ can be trapped asinclusions or in interstices of solid minerals, forsubsequent microanalysis of major and traceelements. This has helped to characterise the mobilephase in the subducted slab (Kessel et al., 2005),transferring incompatible elements to the overridingmantle region of calc-alkaline magma generation,thus initiating the chain of processes ultimately leadingto hydrothermal ore formation. The chemicalevolution of magmas along their ascent route throughmantle and crust is being studied by analysis of meltinclusions in igneous phenocrysts, but the quan ti ficationfor hydrous and internally crystallised inclusionstill presents a challenge (Zajacz and Halter 2007).Studies of melt inclusions in ore-forming andesiticvolcanoes have identified the importance of magmamixing between mantle and crustal components,which determine the overall budget of ore-formingele ments available for subsequent generation of deposits (Halter et al., 2005). The role of sulphide andsulphate saturation seems to be of central importancefor the generation of metal-rich hydrothermalfluids, by volatile exsolution from crystallising magmas.In some of the largest porphyry-Cu-Mo-Au de posits,this hydrothermal input fluid is a single phase ofvapour-like density and rather low salinity (

O9European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 36Fluid origin and evolution at the Sweet Home Mine (Alma, Colorado) –a poor cousin of the giant Climax molybdenum depositLüders, Volker*, Romer, Rolf L.*, Gilg, H. Albert**, Bodnar, Robert J.*** and Pettke, Thomas***** GeoForschungsZentrum Potsdam, Telegrafenberg, D-14473 Potsdam, Germany** Lehrstuhl für Ingenieurgeologie, TU München, Arcisstr. 21, D-80290 München, Germany*** Department of Geosciences, Virginia Tech, Blacksburg, VA 24061, USA****University of Bern, Institute of Geological Sciences, Baltzerstrasse 1-3, CH-3012 Bern (Switzerland)Mineral assemblages at the Sweet Home Mine(Alma district, Peak County, Colorado) are similar tothose of Climax-type molybdenum deposits. Theformation of world-class Mo deposits in the ColoradoMineral belt is connected with igneous activity duringthe Tertiary that was related to the development ofthe Rio Grande rift system. Ore fluids are consideredto be derived exclusively from magmas (e.g., Steinand Hannah, 1985; Seedorf and Einaudi, 2004). Thedeposition of the early stage quartz-molybdenumpyrite-topaz-muscovite-fluoriteand subsequenthübnerite and sulfide-rhodochrosite-fluorite mineralizationat the Sweet Home Mine seems to haveoccurred coeval with the final stage of magmaticactivity and ore formation at the nearby giant ClimaxMo deposit at about 26 to 25 Ma. The mineralizationdeposited at depths of about 3000 m and is related toat least two major fluid systems: (i) one dominated bymagmatic fluids and (ii) another dominated bymeteoric fluids.The sulfur isotopic composition of pyrites, andthe strontium isotopic composition as well as theREE+Y content of fluorites suggest that the quartzmolybdenum-pyrite-topaz-muscovite-fluoritemineralization deposited from magmatic fluids undera fluctuating pressure regime at temperatures ofabout 400 °C as indicated by the presence of CO 2-bearing, medium salinity fluid inclusions in early milkyquartz. LA-ICPMS analyses of fluid inclusions inquartz prove there to be considerably lower metalcontents in the Sweet Home Mine fluids than thosereported from porphyry-Cu-Au or Climax-type fluids.The origin of the magmatic fluids is not quite clear;they may either be derived from magma(s) associatedwith the deep seated Alma Batholith or from distalporphyry stocks.The formation of abundant subsequent sulfidemineralization with fluorite and gemmy rhodochrositeas gangue minerals is dominated by meteoric fluidsthat mixed at variable proportions with magmaticfluids. Sulfide mineralization deposited under ahydostatic pressure regime from low to mediumsaline ±CO 2-bearing fluids at temperatures below400°C and is characterized by mostly negative δ 34 Svalues of sulfides, highly variable δ 18 O values ofrhodochrosites, and low REE+Y content in fluorite.Lead isotopic composition of galena as well as highlyvariable 87 Sr/ 86 Sr ratios of fluorites, rhodochrosite,and apatites indicate that at least part of the lead andstrontium originated from a much more radiogenicsource than Climax-type granites do. It seems verylikely that magmatic intrusion(s) triggered themigration of meteoric water and caused water/rockinteraction on a large scale which led to the depositionof abundant sulfide-rhodochrosite-flurorite mineralizationat the Sweet Home Mine.REFERENCESSeedorf E, Einaudi MT (2004) Econ. Geol. 99: 3-37Stein HJ, Hannah JL (1985) Geology 13: 469-47436

O10European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 38Nature and timing of mineralising fluids during the Appalachian-Caledonian OrogenyConliffe, James*, Feely, Martin* and Selby, David*** Department of Earth and Ocean Sciences, National University of Ireland, Galway, Galway, Ireland** Department of Earth Sciences, University of Durham, Durham, United KingdomEstablishing the timing and nature of magmaticrelatedhydrothermal system is vital in developing abetter understanding of fluid flow during orogenesis.Herein we combine fluid inclusion data with Re-Osmolybdenite geochronology in order to constrain thenature and timing of granite-related mineralisingfluids during the Appalachian-Caledonian Orogen(ACO).Granite-related molybdenite mineralisation hasbeen reported throughout the ACO and is often foundin association with economic and sub-economicdeposits of Mo, Cu, Au, W and Sn. The P-T-x characteristicsof fluids are used to develop a framework formolybdenite mineralisation along the ACO and arecombined with Re-Os molybdenite ages in order toestablish absolute time constraints for these molybdenitesystems. Specifically fluid inclusion studiesand Re-Os geochronology from molybdenite mineralisationin the Connemara Granites (Western Ireland)and the Lake District Granites (England) have identifieddifferences in the timing and fluid chemistry ofthese systems (Selby et al., 2003; Feely et al., inpress; Selby et al. in prep.).Re-Os geochronology indicates that molybdenitemineralisation in the late-Caledonian GalwayBatholith and its satellite plutons in Connemaraoccurred from 422.5 ± 1.7 Ma to ~383 Ma (Selby etal., 2003; Feely et al., in press). These ages areidentical, within uncertainty, to ID-TIMS U-Pb zirconemplacement ages for the host granites, and show thatmagmatism and mineralisation in Connemara occurredcontemporaneously. Geochemical, fluid inclusions andlimited stable isotope (δ 18 O, δD, δ 34 S) studies haveshown that molybdenite mineralisation in theConnemara Granites is associated with late magmaticaqueous-carbonic fluids.Re-Os ages for mineralisation in the LakeDistrict range from 405.4 ± 0.4 Ma for the Shapgranite to 391.9 ± 2.8 Ma for the Skiddaw Granite(Selby et al. in prep.). When compared with U-Pbages for the Lake District Granites Re-Os ages showthat mineralisation in the Shap Granite occurred atthe same time as granite emplacement. In contrastmineralisation, in part, occurred at least 4 m.y. afterthe emplacement of the Skiddaw Granite, and maybe related to post-magmatic hydrothermal systems.Fluid inclusion studies of the Lake District Graniteshave shown that mineralisation was associated withboiling of low-moderate salinity (0-8 eq. wt% NaCl)aqueous fluids between 300 and 400°C. Unlike theConnemara Granites no evidence for carbonic fluidsassociated with molybdenite mineralisation havebeen recorded from the Lake District Granites. Thissuggests significant genetic variation in fluidsassociated with molybdenite mineralisation acrossthe ACO and may be related to the source of granitemagma in Connemara and the Lake District.These results provide constraints on the timingof molybdenite mineralisation and its relationship toboth magmatic-hydrothermal and post magmatichydrothermal systems. In addition variations in thechemistry composition of mineralizing fluids in theConnemara and Lake District Granites reflect spatialand temporal evolution of the ACO. Current researchis focussed on P-T-x-t characteristics of fluidsassociated with granite-related molybdenite mineralisationsystems elsewhere in the ACO. This willestablish absolute time constraints for these hydrothermalsystems and will ultimately lead to a betterunderstanding of fluid activity during the evolution ofthe ACO.REFERENCESSelby, D., Creaser, R.A. and Feely, M. (2003)Geochemical Journal. 38: 291-294.Feely, M., Selby, D., Conliffe, J. and Judge, M. (inpress) Trans. Inst. Min. Metall. (Section B; AppliedEarth Science38

O11European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 40Fluid inclusions key in changing paradigms in carbonate diagenesisGoldstein, Robert H.Department of Geology, University of Kansas, 120 Lindley Hall, 1475 Jayhawk Blvd, Lawrence, Kansas66045, USAThere still remains a fundamental challenge incarbonate hydrocarbon reservoir work, the predictionof the spatial distribution of diagenetic alteration ofporosity and permeability. Fluid inclusion work hasplayed a pivotal role in redefining how researchersview diagenetic processes, illustrating the deficienciesof many of the models commonly used forunderstanding diagenesis and pointing research innew directions.Common approaches for predicting diageneticalteration have focused on modern settings in whichlow-temperature fluids, and meteoric-, marine-,evaporated-marine-, or mixed-fluids were regardedto be of primary importance. These models predictedthat for each of these settings, one would expect aparticular diagenetic product, including dissolution ofprimary grains, dolomitization, and cementation withcarbonate minerals. For decades, these predictionsappeared to be confirmed by cement stratigraphicand isotopic studies. Recently, however, integrationof fluid inclusion studies with these techniques hasshown that such models do not adequately describediagenetic alteration.Meteoric diagenesis commonly is thought tohave the most important diagenetic impact oncarbonate rocks. Surprisingly, however, muchdissolutional pore space, previously thought to formin low-temperature meteoric water, forms in othersettings. In addition, much of the calcite cement,previously ascribed to meteoric origins, has otherorigins.Seawater is commonly expected to precipitatearagonite and high-Mg calcite, as is observed inmodern systems. Some researchers expectdolomitization, as equilibrium would predict. Fluidinclusion work has shown that although seawatersalinity has remained similar throughout thePhanerozoic, seawater Mg/Ca, SO 4, and pCO 2haschanged, leading to times of predominant aragoniteprecipitation, calcite precipitation, and even aragonitedissolution in seawater. Most dolomite turns out notto form from normal unaltered seawater. The variousdiagenetic products of seawater depend on age andsetting.Mixing zones, where seawater and freshwatermixes, normally are considered to be the site ofdolomitization and perhaps dissolution. Most wouldassume that mixing ratio would be the primary controlon diagenetic product. Recent studies incorporatingfluid inclusions show that mixing ratios do not appearto exert the primary control on diagenetic product,and that mixed systems yield calcite, high-Mg calcite,and aragonite cement, or dissolution. Dolomite istypically absent.Reflux models describe how evaporativeconcentration of seawater at the surface causes adensity inversion, allowing the dense brines to sinkinto the sediment through less dense brines. Althoughviews on this subject have varied, many researchershave underestimated its importance. Fluid inclusionwork shows that reflux is far more important thanpreviously thought, and that it takes very littleevaporation to drive it. Evaporation of seawaterappears to provide a chemical and hydrologic drivelacking in many simple marine systems, leading tolarge amounts of dolomitization and calcite cementation.Finally, many low-temperature models appearto be giving way to high-temperature models ofcarbonate diagenesis. Fluid inclusion work inparticular has shown that many precipitates formedfrom fluids of varying temperature and composition,and that the temperature was higher than expectedfor normal burial heating. These data have proven tobe key in showing that many carbonate rocks arealtered as warm fluids are injected into cooler rocks.The contribution of fluid inclusion work suggeststhat it may be time discard many of the acceptedpredictive diagenetic models, and replace them withnew conceptual models.40

O12European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 42Fluorescence lifetime measurements of single hydrocarbon-bearingfluid inclusionsBlamey N.J.F.*, Ryder A.G.*, Owens, P.* Feely, M.** and Naranjo-Vesga, J.F.***Nanoscale Biophotonics Laboratory, Department of Chemistry, National University of Ireland, Galway,Ireland.**Department of Earth and Ocean Science, National University of Ireland, Galway, Ireland.Fluorescent colours obtained using UVexcitation are commonly used to visually approximatethe API gravity of hydrocarbon-bearing fluid inclusions(HCFI) (Bodnar, 1990). This allows visualdiscrimination of single or multiple generations into aparagenetic sequence. However, HCFI compositionmeasured by Gas Chromatography does notnecessarily correlate with fluorescent colour (Georgeet al., 2001). Human colour perception is impreciseand operator dependant; therefore observingfluorescent colours is at best a qualitative tool. Herewe show that using fluorescence lifetimes is moreaccurate than colour at discriminating HCFIgenerations. Fluorescence lifetimes providequantitative measurements that are repeatable,unaffected by host mineral colour, inclusion size,inclusion dimensions, or operator perception.Fluorescence lifetime measurements correlatewith crude oil composition; heavy, less mature oilshaving shorter lifetimes than light, mature oils (Ryderet al., 2004). Here we present data based onfrequency domain (FD) lifetime measurements andFluorescence Lifetime Imaging Microscopy (FLIM)using 405 nm excitation. Fluorescence lifetimes arecalculated from phase delay and demodulationmeasurements using a variety of different modelsand then correlated to crude oil compositions. Thesystem has an optical resolution of

O13European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 44Hydrocarbon-aqueous mixtures in syn-diagenetic fluid inclusionsRidley, J.*, Dutkiewicz, A.**, George, S.C.*** and Volk, H.***** Department of Geosciences, Colorado State University, Fort Collins, CO 80523-1482, USA** School of Geosciences, University of Sydney, Sydney, NSW 2006 Australia*** Australian Centre for Astrobiology, Macquarie University, Sydney, NSW 2109, Australia**** CSIRO Petroleum, P.O. Box 136, North Ryde, NSW 1670, AustraliaHydrocarbons have finite solubility in water athigh P and T, but to date this solubility has not beendocumented in fluid inclusions. Multi-phase inclusionswith fluorescing liquid hydrocarbons or bitumen as aminor component to a dominant aqueous phase or toaqueous–carbonic phases are here described fromOklo in the uraniferous Paleo-proterozoic FAFormation of the Franceville Basin of Gabon (seeDutkiewicz et al., this volume), and have also beenfound to be widespread in the U-bearing NeoarcheanWitwatersrand Supersequence, South Africa, and thePaleoproterozoic Matinenda Formation of theHuronian Supersequence, Ontario. Such inclusionsare key evidence for hydrocarbon generation andmigration in these ancient sedimentary basins.Hydrocarbon-bearing inclusions at Oklo generallycontain low-salinity liquid H 2O, gas, and2-3 vol. % fluorescing hydrocarbons as single ormultiple µm sized globules within the aqueous phase,or as a thin meniscus between liquid and gas. Manyassemblages are homogeneous with constant phaseproportions: In others, a visible hydrocarbon phase isnot ubiquitous; however, fluorescence under Ramanlaser excitation shows that gas phases containsignificant volatile higher hydrocarbons.Inclusions were trapped during or afterdiagenetic occlusion of porosity. Partial homogenisation(L + V → L) is at diagenetic temperatures (120 –180 ºC). Total homogenisation by dissolution of thehydrocarbon phase would be at 250 ºC or higher(using Thiéry, 2006), but has not been experimentallyachieved, possibly because of post-entrapment‘bitumenisation’ of the hydrocarbon phase.Interpretation of entrapment at around 250 ºC is,however, in apparent conflict with the strongfluorescence of the inclusion oils and with solventextractGC-MS data which show a molecularcomposition of a normal oil of peak or post-peak oilwindow maturity (≈ 125 – 150 ºC). This mismatch ofestimates of transport and entrapment temperaturemay be a result of one or more of:• Transport as an emulsion of oil droplets in agas-charged aqueous phase.• Oils with abnormal aqueous solubility as aresult of high concentration of polar and otherhydrophilic compounds, possibly as a result of Uinduced radiolysis and hydrocarbon oxidation (e.g.Court et al., 2006). GC-MS data show highconcentrations of low molecular weight water solublecompounds (benzene, furan etc), but high molecularweight polar compounds were not sought.• Unreliability of molecular maturity indicatorsand molecular mass distributions of oils at temperatureindicators significantly above peak oil window.REFERENCESCourt RW, Sephton MA, Parnell J and Gilmour I,2006, The alteration of organic matter in responseto ionising irradiation: Chemical trends andimplications for extraterrestrial sample analysis.GCA 70, 1020-1039.Thiéry R, 2006, Thermodynamic modelling ofaqueous CH 4-bearing fluid inclusions trapped inhydrocarbon-rich environments. Chem. Geol. 227,154-164.44

O14European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 46Effect of plastic deformation on fluid inclusions in quartz: anexperimental studyTarantola, Alexandre*, Diamond, Larryn W.* and Stünitz, Holger*** Institute of Geological Sciences, University of Bern, Baltzerstr. 3, 3012 Bern, Switzerland** Institute of Geology and Paleontology, University of Basel, Bernoullistr. 32, 4056 Basel, SwitzerlandSeveral experimental studies have characterizedre-equilibration of fluid inclusions subjected tohydrostatic under- or overpressures (e.g. Sterner andBodnar, 1989; Bakker and Jansen, 1991; Vityk andBodnar, 1998). However, little is known experimentallyabout the effects of plastic deformation on theproperties of fluid inclusions. For want of a clearinterpretative framework, the potentially usefulinformation from inclusions within sheared hydrothermalveins and metamorphic rocks remains largelyinaccessible.To elucidate the behaviour of fluid inclusionsduring plastic deformation of their host crystals weare undertaking experiments using a Griggs-typepiston-cylinder apparatus. In addition to offeringhigher experimental pressures than conventionalcold-seal autoclaves, the apparatus permits experimentsunder deviatoric stress. Our samples are ofnatural CO 2–H 2O–NaCl inclusions in large, undeformedquartz crystals. At Tlab, the volume fraction ofthe carbonic phase (ϕ car) is ~0.2.Prior to the experiments numerous inclusionswere mapped, photographed and analysed bymicrothermometry and Raman spectroscopy todetermine their molar volumes and compositions.The corresponding isochores were calculated andfound to span a range of pressures at 700 °C, themean internal pressure being ~600 MPa. Based onthis information a first set of control experiments wasconducted under hydrostatic conditions. The sampleswere placed at 700 °C and 500, 600 or 800 MPa (allwithin the α-quartz field) for 16 hours, in order toinduce static re-equilibration of the inclusions underinternal under- or overpressure. At these conditionsonly one homogeneous phase is stable in the CO 2–H 2O–NaCl system. Following the experiments theinclusions were relocated and reanalysed. In eachcase, irreversible changes in the shape of theinclusions were observed, similar to those reported inthe cited earlier studies. A complication of the presentexperiments is that H 2generated within the Griggsapparatus diffused into the inclusions, partiallyreducing the CO 2and producing variable CH 4/CO 2ratios. Nevertheless, the initial variation in molarvolumes of the inclusions was considerably reducedduring the experiments, converging on the valuesexpected for the experimentally imposed P–Tconditions.With the effects of hydrostatic re-equilibrationthus known for these samples, a second set ofexperiments was conducted at 700 °C and 600 MPaand at 50 to 100 MPa deviatoric stress for 12 to 133hours, leading to mean strain rates of 10 -6 to 10 -7 s -1 .New inclusion shapes were observed, often withbranches emanating from the inclusions. Inclusionsinitially aligned along healed fractures weretransposed. Most interestingly, new gas-free aqueousinclusions (homogeneous liquid at Tlab) were formed,close to but separate from relicts of the originalinclusions. The relicts themselves have highlyenriched gas contents (ϕ up to 0.8), indicatingcarpartitioning of H 2O and CO 2from the originallyhomogeneous CO 2–H 2O–NaCl mixture into separateinclusions. Isochores calculated for the transposedinclusions lie close to the P-Tconditions of theexperiments, whereas the newly formed inclusionsshow a span of isochores.The observed ranges in textures, compositionsand molar volumes of the inclusions in the latterexperiments are remarkably similar to those innaturally deformed quartz in ductile shear zones.This similarity promises an approach to interpretsuch natural samples.REFERENCESSterner S.M., Bodnar R.J. (1989) J. Metam. Geol. 7:243-260.Vityk M.O., Bodnar R.J. (1998) Contrib. Mineral.Petrol. 132: 149-162.Bakker R.J., Jansen J.B.H. (1991) Geochim.Cosmochim. Acta 55: 2215-2230.46

O15European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 48Fluid inclusion distribution associated with quartz microstructures: Arecord of the exhumation of the Naxos Metamorphic Core Complex(Cyclades, Greece)Siebenaller, Luc*, Boiron, Marie-Christine*, Vanderhaeghe, Olivier * , Jessell, Mark** and Banks, David **** G2R, Nancy-Université, CNRS, BP 239, 54506, Vandoeuvre-les-Nancy** IRD LMTG UMR 5563, 14 avenue Edouard Belin, 31400, Toulouse*** School of Earth and Environment, University of Leeds, Woodhouse Lane, Leeds, LS2 9JT, UKRecent work on Metamorphic Core Complex(MCC) indicates that surface-derived fluids penetratethe continental crust down to the brittle/ductiletransition. Can trapping conditions of fluids havingcirculated during the development of a MCC becorrelated to the different deformation stages affectingrocks during their migration through the brittle/ductiletransition? When studying this question it is highlyimportance to take into account the influence of thedeformation on the fluid circulations and to characterisewhether these fluids preserve their original signatureduring exhumation.The island of Naxos displays a structuralsection from a non-metamorphic upper unit affectedby brittle deformation juxtaposed to ductilely deformedhigh-grade metamorphic rocks along a detachmentzone characterized by pervasive cataclasis andretrogression. The downward migration of the brittle/ductile transition relative to rocks affected byexhumation is marked by high-angle normal faultscross-cutting the detachment zone. The circulation offluids is attested by discordant as well as ductilelydeformed veins, the abundance of which increasestowards the detachment and which were analysed atone site from the leucogneiss.A multi-technique approach based on thestudy of fluid inclusions has been carried out. Inparticular, the orientation of the fluid inclusion planes(FIPs) has been measured, in order to reconstructthe geometry of fluid percolation. This was combinedwith the chemical characterisation of individualinclusions (microthermometry, Raman spectroscopy,LA-ICPMS, bulk crush leach and stable isotopegeochemistry). These techniques applied syste ma ticallyto the different quartz vein generations reveal 5different fluid circulation events that record theretrograde P-T pathway. A particular halite-calcitesiderite-marcasitebearingfluid was only recordedwithin the completely transposed earliest veins and isrepresented by primary inclusions which are randomlydistributed within quartz grains. LA-ICPMS datareveal that it is a magmatic brine that contains ratherhigh concentrations in metals (Zn, Cu, Fe, Ag andPb). These fluids yield trapping temperatures of 420to >500 °C and pressures of 1.0 to 2.0 kbar and arerelated to the latest ductile fabrics before rockspassed to the brittle deformation zone. This transitionis reflected by the presence of well defined FIPscrosscutting these quartz grains. Three types ofmetamorphic CO 2-rich fluids from these FIPs couldbe differentiated according to their distribution relativeto the quartz microstructures and their respectivecompositions. These fluids yield trapping temperaturesfrom 210 to 400 °C and pressures from 0.4 to 1.5kbar and attest to the transition from ductile to brittledeformation. The fifth generation of fluids representsmeteoric fluids that were recorded only within FIPsthat crosscut quartz grain boundaries.Combining a detailed study of quartzmicrostructures and the distribution of fluids givesanswers to the geometry of fluid circulations and theirrespective relative chronologies of percolation duringthe exhumation of the MCC of Naxos Island. On theother hand, fluid inclusions analysed within recrystallisedand deformed quartz grains show a large varietyof homogenisation temperatures and thus reflect thatduring deformation the original signatures are lost.48

O16European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 50Fluid inclusion in HP/LT units of Southern Apennine (Italy): acontribution to burial/exhumation historyInvernizzi, Chiara**Dipartimento di Scienze della Terra – Università di Camerino, Via Gentile III da Varano,Camerino (MC) - ItalyTectonic units of the Southern Appennines ofItaly (Calabria-Lucanian border) belong to an accretionarywedge structure. These units consist of aMeso-Cenozoic succession, recently grouped intotwo tectonic units (Iannace et al., 2005): a wellpreserved HP-LT calcareous-marly unit (the Lungro-Verbicaro Unit, LVU) and an underlying nonmetamorphicunit (Pollino-Ciagola Unit, PCU), bothbelonging to the Afro-Adriatic continental paleomargin.They are tectonically overlain by ophiolite-bearingunits (Diamante-Terranova and Liguride complex). Inparticular, the Liguride complex (LC) is made ofmedium- to low-metamorphic Frido Unit and nonmetamorphicNorth-Calabrian Unit. From petrographicanalyses, some of these units reached blueschistfacies condition (LVU and Frido Unit).It was possible to highlight several steps of thedeformation history of the examined units thanks to:- an accurate meso-structural analysis at the outcropscale, aimed to recognized different vein assemblages;- an accurate petrographic analysis on fluid inclusionswhich allowed to ascribe different fluid inclusionassemblages to prograde and retrograde events,based on texture and microthermometric data.The fluid inclusion study contributed to betterdefine temperature condition relative to each event.In fact, syn-tectonic quartz/calcite veins in metasedimentscontain various types of fluid inclusions;most are two-phases at room T with an aqueousNaCl-H 2O solution. Both primary and secondaryinclusions have been observed. Other inclusionssurvived the prograde metamorphism developing atypical dendritic morphology (Vityk & Bodnar, 1995).Finally, relationships between paleo-tempe raturereconstructions from fluid inclusions micro thermometryand mode and time of exhumation processeswithin the wedge are tentatively suggested.REFERENCESIannace A., Bonardi G., D’Errico M., Mazzoli S.,Perrone V., Vitale S. (2005). C. R. Geoscience, 337,1541-1550Vityk M.O. & Bodnar R.J. (1995) Contr. Min. Petr.,121(3), 309-323.50

O17European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 52Fluid-rock interaction along the Glarus thrust at Lochseite and itsimpact on calc-mylonite formation and thrustingMullis, Josef*, Vennemann, Torsten**, de Capitani, Christian* and Franz, Leander** Institute of Mineralogy and Petrography, University of Basel, Switzerland** Mineralogical and Geochemical Institute, University of Lausanne, SwitzerlandNumerous stable isotope investigations alongthe Glarus thrust show that fluids must have played akey role during deformation (for a review see Burkhard& Kerrich, 1990 and Abart et al., 2002). The aim ofthe present study is to evaluate the influence of highpressuremethane-bearing fluids on rock alterationabove and below the Glarus thrust, on the formationof the Lochseite calc-mylonite and on thrustingitself.The calc-mylonite of the Lochseite locality is afine-grained limestone with abundant thin veinspredominantly of calcite. The footwall rocks consist ofInfrahelvetic flysch with fine marly and silty slatesalternating with sandstone layers. The Verrucano inthe hanging wall consists of massive siltstones andsandstones with intercalated conglomerate horizons.Characteristic features of all three formations aremultiple vein generations due to hydrofracturing,dissolution and precipitation of calcite. In addition,the lowermost two meters of the Verrucano above thethrust is intensely deformed and has a green colour.In contrast to the overlying reddish Verrucano, ferriciron oxides are replaced by pyrite and more abundantchlorite.Fluid inclusion investigations were performedon thrust-related fissure quartz and calcite. Detailedstable isotope investigations on quartz, calcite, wholerock silicates and carbonates as well on fluidinclusions were performed in all lithologies.Preliminary results are:- Immiscible methane-rich and methane-bearingwater-rich fluids were produced by maturation oforganic matter within the Infrahelvetic flysch belowthe Glarus thrust and were trapped in fissureminerals at 228°C and 2.9 kbar.- The clay-rich Verrucano thrust sheet with itssubhorizontal foliation acted as a classicpermeability barrier to the highly pressurized CH 4-bearing fluids.- The lowermost green Verrucano is the reactionzone, where CH 4was oxidized in the presence offerric iron oxides and water to CO 2.- Acidic alteration of feldspars led to massivegrowth of sericite, chlorite and quartz in thelowermost Verrucano and to a lesser extend in theuppermost Flysch below the Lochseite calcmylonite.- Hydrofracturing, acidic alteration, and brecciationof the lowermost Verrucano created porosity andallowed fluid circulation between the uppermostflysch and the lowermost Verrucano.- The circulation of acidic fluids into the footwallflysch has dissolved calcite in the flysch matrixand re-deposited it at the flysch/Verrucanointerface.- Seismic valving related hydrofracturing causedcalcite precipitation and vein mineralization(Etheridge et al, 1984). This led to the formation ofthe carbonate, which was later transformed to theLochseite calc-mylonite. This is confirmed by thecarbon isotope composition of calcite measured inthe flysch.- Supported by high fluid pressures, the Lochseitecalc-mylonite situated between the two more rigidlithologies acted as a “weak décollement layer”that accommodated the thrust movements abovethe Infrahelvetic flysch.REFERENCESAbart, R., Badertscher, N., Burkhard, M. & Povoden,E. (2002) CMP143: 192-208.Burkhard, M. & Kerrich, R. (1990) SMPM 70: 77-82.Etherdige, M.A., Wall, V.J., Cox, S.F. & Vernon, R.H.(1984) J. Geophys. Res. 89: 4344-4358.52

O18European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 54The hydrothermal diamond-anvil cell: a versatile tool to study aqueousfluids in situ at high pressures and temperaturesSchmidt, Christian**GeoForschungsZentrum Potsdam, Telegrafenberg, Potsdam, 14473 GermanyAqueous fluids and their interaction withmineral assemblages play a key role for the mobilityof elements and, thus, material flux in the lithosphere.Understanding element and isotope transport andfractionation in these environments requires knowledgeof solubilities, dissolution kinetics, speciation,and other properties of such fluids. For theexperimental determination of these properties, directobservation at the pressure and temperature ofinterest is required or of advantage. The invention ofthe hydrothermal diamond-anvil cell (HDAC; Bassettet al., 1993) has extended the PT range in whichaqueous fluids can be studied in situ using opticalmicroscopy and various spectroscopic and X-raytechniques, up to the conditions of the upper mantleand dehydrating slabs. Bassett-type HDACs havebeen utilized in experiments on aqueous fluids to 23GPa at 850 °C (Lin et al., 2004) and 5 GPa at 1000°C (Kawamoto et al., 2004).Modifications of the HDAC design (Bassett etal., 2000; Schmidt and Rickers, 2003) facilitateapplication of synchrotron-radiation X-ray techniquesto investigate the behaviour of dissolved heavyelements with X-ray emission energies as low as ~4keV and absorption edge energies as low as ~5 keV.Time-resolved SR-XRF analyses have been used toobtain quantitative information on the solubility ofaccessory minerals in aqueous fluids, the kinetics offluid-mineral interaction, and trace element partitioningbetween aqueous fluids and silicate melts (e.g.,Schmidt et al., 2006; Schmidt et al., 2007). For Ti (Kαenergy = 4.5 keV), a minimum detection limit of 4E-05 mol/kg was achieved in recent in situ SR-XRFexperiments on the solubility and dissolution kineticsof rutile in H 2O+NaAlSi 3O 8and H 2O+Na 2Si 3O 7fluidsto 800 °C and 1.3 GPa. The complexation of heavyelements in aqueous melts and fluids has beeninvestigated in situ by X-ray absorption techniques,e.g., SR-XAFS analyses of the La L 3-edge in a studyof the hydration structure of aqueous La 3+ (0.007 m)to 300 °C and 160 MPa (Anderson et al., 2002) orSR-XANES measure-ments on Fe 2+ in watersaturatedhaplogranitic melt to 700 °C and 500 MPa(Wilke et al., 2006).Raman spectroscopy and Bassett-type HDACshave been used to study the behaviour of lightelements (Z

O19European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 56Equation of state of H 2O from sound velocity measurements in thediamond anvil cell by Brillouin scattering spectroscopySanchez-Valle, Carmen *,** , Bass, Jay D. ***Institute for Mineralogy and Petrology, ETH Zurich, Clausiusstrasse 25 NW, CH-8092 Zurich, Switzerland**Department of Geology, University of Illinois at Urbana-Champaign, 1301 W. Green St. NHB, Urbana IL61801, USA.Saline-rich aqueous fluids play an importantrole in metamorphic reactions and chemical transportin a wide range of geological environments. Insubduction zones, aqueous fluids expelled fromsubducting slabs lead to the important geochemicalphenomena of mantle wedge metasomatism and arcmagmatism and mediate the recycling of elements inthe Earth. Reconizing the role of deep fluid in theseprocesses a number of significant but unansweredquestions arise as to their chemical composition, theextent of mass transfer, or the mechanism of elementaltransport from the slab to the mantle wedge. Answersto these questions depend on quantitativethermodynamic modeling of fluid-mineral interactions,that is greatly limited by the lack of thermodynamicdata of complex aqueous fluids at high pressure (P)and temperature (T) conditions [Manning, 2004].Water is the main component in deep geologicalfluids but data on its thermodynamic properties at theP and T of interest for subduction zones are scarceas a result of the experimental difficulties. Equationsof state (EoS) for H 2O usually employed to predictthermodynamic properties at high pressures thus relyheavily on extrapolation of sparse low-pressureexperimental data (< 1 GPa) [Saul and Wagner,1989] and molecular dynamic calculations [Belonoshkoand Saxena, 1991; Brodholt and Wood, 1993].To address this problem, we conducted soundvelocity measurements in an externally heateddiamond anvil cell using Brillouin scatteringspectroscopy to determine the equation of state(EoS) of H 2O up to 400 °C and 7 GPa. Soundvelocities measured in H 2O are in excellent agreementwith previous measurements using ImpulsiveStimulated Scattering (ISS) (Fig.1) [Wiryana et al.,1998; Abramson and Brown, 2004].The determined EoS is used to evaluate thepressure and temperature dependences ofthermodynamic properties of water, including thermalexpansion coefficients, isothermal and adiabaticcompressibilities and heat capacities. The results arecombined with previous experimental and theoreticalEoS to provide an internally consistent dataset for thethermodynamical properties of H 2O at P-T conditionsrelevant for deep subduction processes.Fig.1. Sound velocities measured in H 2O as afunction of P and T, along with previousmeasurements using the ISS technique.REFERENCESManning, C.E. (2004) Earth Planet. Sci. Lett. 223,1-16.Saul, A. and Wagner, W. (1989) J. Phys. Chem. Ref.Data 18, 1537-1564.Belonoshko, A. and Saxena, S.K. (1991) Geochim.Cosmochim. Acta 55, 381-392.Brodholt, J.P. and Wood, B.P. (1993) J. Geophys.Res. 98, 519-536.Wiryana et al., (1998) Earth Planet. Sci. Lett. 163,123-131.Abramson, E.H. and Brown, J.M. (2004) Geochim.Cosmochim. Acta 68, 1827-1835.56

O20European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 58Modifications of the Raman spectra of pure water and brines insynthetic fluid inclusions caused by the quartz host mineralBaumgartner, Miriam*, Coquinot, Yvan* and Bakker, Ronald J.**Department of Applied Geosciences and Geophysics, Mineralogy and Petrology, University of Leoben,Peter-Tunner Str. 5, Leoben, 8700 AustriaThe Raman stretching bands of water from2800 up to 3800 cm -1 are very sensitive to the amountof dissolved electrolytes in the solution. For thisreason Raman spectroscopy is often used todetermine the salinity of fluid inclusions. In our studyof synthetic fluid inclusions in quartz we havedeconvoluted the Raman spectra of water and ofNaCl-solutions using three Gaussian-Lorentziancontributions. It is thus possible to characterizespecific peak positions of these contributions fordifferent salinities.The Raman spectra of liquids in fluid inclusionscan be substantially different from those in free waterdroplets owing to the physical properties of the hostmineral. The laser beam is polarized as it traversesthe quartz host. The effects of such polarization onthe characterization of entrapped fluid in inclusions isthe topic of this study.In birefringent minerals like quartz the spectrumis influenced by the crystallographic orientation of thehost. This was investigated by measuring NaCl- andpure water-containing fluid inclusions in samples ofwell known orientation. Measurements of fluidinclusions where the quartz section is orientatedparallel to the optical axis show strong modificationsin the Raman bands during rotation of the sample onthe microscope stage (Fig. 1). The slope of thespectrum in the range of 3200 to 3400 cm -1 is variablefor the enclosed fluid, depending on the rotationangle of the sample. In addition, a shift in thedeconvoluted peak positions could be observed.There is a maximum and minimum about every 45°of rotation, which indicates a good correlation withthe optical properties of quartz. Quartz sliceswith asurface orientated perpendicular to the c-axis (opticalaxis) did not show rotational effects.Another polarisation effect may be caused atthe quartz-fluid inclusion interface. Depending on theangle of the surface of the inclusion wall where theincident Raman laser beam enters, polarisationeffects could appear which additionally affect theRaman spectra.These phenomena may cause erroneousestimations of the salinity of fluid inclusions, as it canbe seen in Fig. 2.Fig. 1. Influence of birefringence on the pure liquidwater Raman spectra during the rotation of thesample on the microscope stage.Fig. 2. Filled dots represent peak positionsmeasured in reference solutions, whereas peakpositions marked with error bars representmeasurements in fluid inclusions during 90° ofrotation.58

O21European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 60Elemental partitioning during sub-critical phase separation: evidencefrom SR XRF, fluotomography and X-ray absorption techniques ofliquid-vapour fluid inclusion assemblages from the granitic Torres delPaine Complex, PatagoniaRickers, Karen*,**,***, Bleuet, Pierre***, Cauzid, Jean***, and Lüders, Volker***HASYLAB at Deutsches Elektronen-Synchrotron DESY, Notkestrasse 85, Hamburg, 22603 Germany**GeoForschungsZentrum Potsdam, Telegrafenberg, Potsdam, 14473 Germany***European Synchrotron Radiation Facility ESRF, 6, Rue Jules Horowitz, BP220, Grenoble, 38043 FranceFluid phase separation (boiling) can be theprimary cause for major variations in fluid compositionin many hydrothermal systems. Such variationscommonly lead to extreme enrichments of importantmetals and to the formation of ore deposits. Theprocess of element partitioning is closely linked to thespeciation of the element in the different phases atthe temperature of fluid phase separation.In this study we investigated on the elementpartitioning of liquid-vapour assemblages formed bysub-critical phase separation in a granitic system.Synchrotron-radiation induced micro-XRF wasapplied on single inclusions for trace element analysisof elements with Z > 16. Measurements wereperformed with spot sizes of 1 x 4 μm (ID18F andID22, ESRF). Helical fluorescence tomography wasapplied on selected inclusions for three-dimensionaltrace element analysis. Temperature-dependant Cuand Zn microfluorescence XANES experiments wereperformed at ID22 at temperatures up to 460 °Cusing a Linkam THMSG-600 heating-stage and amultielement detector.The studied fluid inclusion boiling assemblagesare hosted in quartz from miarolic cavities of theTorres del Paine granite complex (Chile). Formationtemperatures of hydrothermal quartz in vugs rangebetween 280 °C and 340 °C. Multielement analysisshowed that brines mainly contain Mn, Fe, Ni, Zn, As,Br, Rb, Mo, Cs, Pb ± Cu, W, Sn, Sr, Yb, Ge whilevapours are composed of Mn, Fe, Zn ± K, Ca, Cl, Br.The detection of the additional elements Cu, Rb, As,Mo, Sn and Pb in the vapour is linked to the presenceof daughter crystals present in or close to theinclusion. Three-dimensional analysis byfluotomography showed the crystals to be realdaughter phases.Trace element partitioning coefficientsdisplayed that element partitioning is nothomogeneous. Especially Mo and Cu may eitherbecome partitioned into the vapour or into the liquidphase. Micro-XANES measurements were perfomedto unravel the metal speciation during elementpartitioning. Measurements were performed on Cuand Zn because the two elements have a contrastingpartitioning behaviour: while Cu is dominantlydetected in vapour-rich inclusions and mayoccasionally be present in brines, zinc is generallypresent in both phases and always more concentratedin brine-type inclusions (Fig. 1).Fig. 1. Optical view of a liquid-vapour assemblageand corresponding elemental distribution map ofZn. Length of scale bar is 90 μm.XANES experiments from room temperature toformation temperatures show a change in oxitationstate from Cu 2+ to Cu 1+ in the vapour only and anoverall presence of Cu 2+ in the brine. Zn-XANESspectra indicate that Zn is most propably complexedas ZnCl 42+in the temperature range 25 – 370 °C forboth, liquid and vapour rich inclusions. This showsthat in contrast to Cu, changes in speciation are notresponsible for the partitioning of Zn into the liquidand the vapour phase.60

O22European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 62Arsenic Speciation in fluid inclusions from gold deposits using X-rayAbsorption Spectroscopy from ambient to homogenisationtemperaturesJames-Smith, Julianne a,c , Brugger, Joël a , Hazemann, Jean-Louis c , Liu, Weihua d , Proux, Olivier e , Testemale,Denis c , Philippot, Pascal fandWilliams, Patrick g .aDepartment of Geology & Geophysics, University of Adelaide, 5000, AustraliabESRF, 38042, Grenoble, FrancecInstitut Néel, CNRS, 38042, Grenoble, FrancedMinerals and Exploration, CSIRO, Clayton, AustraliaeLab. de Géophysique Interne et Tectonophysique, UMR CNRS Université Joseph Fourier, 38400 Saint-Martin-d’Heres, FrancefGéobiosphère Actuelle et Primitive, IPGP, Paris, FrancegJames Cook University, Queensland, AustraliaThe chemical composition of fluid inclusionsfound within gold lodes provides a unique windowinto the mineralization processes. In order to relatethe elemental concentrations measured in fluidinclusions with the mineral assemblages (i.e. mineralsolubility) and to imply the mineralizing process (e.g.phase separation, fluid-fluid and fluid-rock interaction),knowledge of element speciation is essential atelevated temperatures.Recent experiments (May 2007) wereconducted on the CRG-FAME beamline at the ESRF(Grenoble, France). The primary aim of this experimentwas to obtain X-ray absorption spectroscopy (XAS)data at the As K edge (11867 eV) to help determineAs speciation from ambient conditions tohomogenisation temperatures. The CRG-FAMEbeamline at the ESRF is dedicated to XASspectroscopy in Earth and Environmental Sciences.The experiment is part of the commissioning of thebeamline for microfocusing. We reached a beam sizeof 15 x 15 µm 2 , ideal for in situ XAS analysis of fluidinclusions.During this experiment, X-ray Absorption NearEdge Structure (XANES) and Extended X-rayAbsorption Fine Structure (EXAFS) spectra werecollected for 18 fluid inclusions (5 – 35 wt.% equivalentNaCl) from three gold deposits (Australia, Madagascar,Italy). Arsenic concentrations of fluid inclusionsmeasured by PIXE, SR-XRF or crush leach methodranged from 147 ppm to above 1 wt%. Data wererecorded in the fluorescence mode using a VortexSi-drift detector from 11500 eV to 12500 eV with anX-ray flux of 10 10 photons/second. Concurrent heatingof the fluid inclusions using a Linkam THMSG-600heating stage during spectra acquisition enableddata to be collected at temperatures above roomtemperature up to homogenisation temperature. Wesucceeded in collecting spectra up to 235˚C, asinclusions decrepitated at about this temperature.It was possible to collect good quality EXAFSdata (up to k ~ 10 Å -1 ) on the As-rich inclusions.Preliminary analysis of the XANES data indicatesthat:• Photo-oxidation of As(III) to As(V) is a majorproblem, that can be easily monitored by XANESspectroscopy. All inclusions were totallytransformed to As(V) after ~1 hour beam exposure.By reducing the flux to ~10 9 , it was possible tocollect EXAFS data on the Madagascar samplewith little As(V). In dilute samples (e.g. typical lowsalinity,

O23European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 64Volumetric imaging of fluid inclusions in quartz using second harmonicgeneration microscopyStoller, Patrick*, Krüger, Yves**, Ricka, Jaro* and Frenz, Martin**Institute of Applied Physics, University of Bern, Sidlerstrasse 5, Bern, 3012 Switzerland**LFA – Labor für Fluid-Einschluss Analytik, Cäcilienrain 3, Bern, 3007 SwitzerlandInformation about the composition and densityof fluid inclusions can be used to estimate thepressure-temperature conditions during inclusionformation. In gas-bearing fluid inclusions containing,for example, CH 4, N 2, or low-density CO 2, determinationof the total fluid density requires knowledge of thevolume fraction of the gas bubble in addition toinformation about the liquid-gas homogenizationtemperature, the fluid composition, and the appropriateequation of state. Existing techniques for determiningthe volume fraction have been limited to fluorescentinclusions or inclusions of certain regular shapes. Wedemonstrate that second harmonic generationmicroscopy can be used to three-dimensionally imageand determine the volume of fluid inclusions ofarbitrary shape in quartz (Stoller et al., 2007). Secondharmonic generation is a nonlinear optical process inwhich two laser photons are converted into a singlephoton at double the frequency; it can occur only incrystals without inversion symmetry (e.g. quartz).To perform the measurements we used anultra-short pulse laser oscillator (800 nm wavelength,

O24European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 66Evidence for sulfide melt oxidation and metal-rich aqueous-carbonicfluid exsolution in the intrusion-related Au system at Fort Knox, AlaskaHanley, J.J.*, Spooner, E.T.C.**, Hart, C.J.***, Heinrich, C.A.* and Guillong, M.**Isotope Geochemistry and Mineral Resources, ETH Zürich, Zürich, Switzerland, CH8092**Department of Geology, University of Toronto, 22 Russell Street, Toronto, Canada, M5S 3B1***Centre for Exploration Targeting, University of Western Australia, Crawley, WA, Australia 6009Early magmatic titanite grains within samplesof granite at Fort Knox, Alaska, USA, contain (in theircores) inclusions of sulfide melt that coexist withsilicate melt inclusions trapped at a minimumtemperature of ~ 780 o C (based on sulfide meltthermometry). Textural and mineralogical evidenceindicates that this sulfide melt phase was destroyeddue to an increase in oxygen fugacity during titanitegrowth. In the same samples, apatite inclusionshosted in quartz phenocrysts trapped coexistingprimary inclusions containing silicate melt and a lowsalinity (~ 4-6 wt% eq. NaCl based on clathratemelting temperatures), aqueous-carbonic fluid (CO 2~ 21-39 vol%) (Fig. 1). Aqueous-carbonic fluidinclusions decrepitate at ~ 400 o C; however, apatitebiotitehalogen exchange thermometry indicates thatthe inclusions in apatite were trapped at a minimumtemperature of 560-680 o C. In contrast to the apatitein quartz, apatite included in the titanite grew at anearlier stage and contains only silicate melt inclusionswith no coexisting aqueous-carbonic fluid, suggestingthat the silicate melt became saturated in the aqueouscarbonicphase after the resorption of the sulfide meltphase.Fig. 1. Coeval silicate melt (SILMI) and aqueouscarbonicfluid inclusion (FI) trapped in magmaticapatite hosted within biotite (photo at 20 o C).Laser ablation ICP-MS analyses of the sulfidemelt inclusions in titanite, and aqueous-carbonic fluidinclusions in apatite, were conducted at the ETHZürich. The sulfide melt phase is an Fe-S melt phasecontaining between 200 and 1800 ppm Cu, andconcentrations of Ag, As, Bi, Sb, Te, W, Mo and Ni inthe 10-100 ppm range. Notably, Au concentrationsare in the ppm range. The aqueous-carbonic fluidphase is Na-dominated (Na/ΣCa+K+Mg+Fe ~ 6-10)with a Rb/Sr ratio of between 0.3-1.3, consistent withthe bulk composition of the granite. Ore metalconcentrations are in the range of 1-20 ppm.Estimated fluid/silicate melt partition coefficients (D)for the coeval aqueous-carbonic fluid and silicatemelt trapped in apatite yield values near ~ 1 for Asand Sb. Selected metal ratios and normative metalabundance patterns in the sulfide melt dropletshosted in titanite and aqueous-carbonic fluidinclusions in apatite are very similar.The results show that ore-forming graniticmagmas at Fort Knox were saturated at an earlystage in a sulfide melt phase. Resorption of thesulfide melt coincided closely with the saturation ofthe crystallizing magma in a low salinity aqueouscarbonicfluid into which the ore metals partitioned.However, ore metal compatibilities in the aqueouscarbonicfluid and silicate melt phase werecomparable. Therefore, unless fluid-silicate meltpartition coefficients changed significantly duringgranite crystallization, prolonged exsolution of metalrichore fluids could be sustained without depletingthe granitic melt in ore metals.The study confirms a magmatic origin formetal-rich, aqueous-carbonic fluids in intrusionrelatedgold systems. Systematic identification andanalysis of Au-rich sulfide melt inclusions in settings“inboard” of convergent plate margins may findapplication in locating mineralised granites andpredicting the metal associations in the ore.66

O25European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 68Tracing the magmatic evolution of Cu-Au porphyry systems by LA-MC-ICPMS analysis of Pb isotopes in fluid and melt inclusionsHarris, Caroline R.*, Pettke, Thomas,** Heinrich, Christoph,* and Kleine, Thorsten**Department of Earth Sciences, Swiss Federal Institute of Technology, ETH Zurich, 8092 Switzerland**Institute of Geological Sciences, University of Bern, 3012 Bern, SwitzerlandIsotopic analysis of fluid inclusions, meltinclusions, and mineral separates have the potentialto identify end-members of a system that may beobscured by whole rock analysis. We have used LA-MC-ICPMS to analyze Pb isotopes in high-temperaturefluids from the porphyry stage of ore deposition in twodeposits from the Apuseni Mountains, Romania.These fluid inclusions contain up to 10,000 ppm Pb,and hence ratios normalized to both 206 Pb and 204 Pbare well resolved. Melt inclusions in feldspars fromthe host magmas have Pb contents about two tothree orders of magnitude lower. Nonetheless, LA-MC-ICPMS analysis of ratios normalized to both206Pb and 204 Pb can be used in conjunction with in situfeldspar microanalysis and conventional whole rockdata to interpret the magmatic evolution of thesystem.Samples are from the “golden quadrilateral” ofthe Apuseni Mountains, which is the richestconcentration of Cu-Au deposits in Europe and hasbeen mined since pre-Roman times. Fluid inclusionsin quartz veins, melt inclusions hosted in feldspar,and different mineral separates were analyzed by LA-MC-ICPMS and are compared to conventional bulkanalyses of mineral separates and igneous wholerocks. Samples are from two Cu-Au porphyry deposits,Rosia Poieni and Deva, which are hosted by Miocene,subvolcanic andesites intruded into a trans-tensionalenvironment. Fresh host rocks were sampled torepresent a comprehensive range in age and chemicalcomposition. Rocks hosting the porphyry depositsexhibit adakite-like geochemical signatures of LILEenrichment, high Sr and Pb contents, and mantle-likeSr and Nd isotopes.Whole rock analyses of host andesites weremade in solution mode using Tl mass bias corrections,and provide the basis for comparison of fluids, melts,and minerals. Laser ablation analyses were correctedfor mass bias by admixing desolvated Tl. This studyillustrates the geologic usefulness of the method,which was developed with synthetic Pb fluid inclusions(Pettke et al., in prep), attaining within run precisions(± 2SE) of as good as 200 ppm (normalized to 206 Pb)and 400 ppm (normalized to 204 Pb), and inclusion toinclusion reproducibilities (± 2SD) of as good as0.08% and 0.15%, respectively.Pb isotopes of sulfides and fluid inclusionsfrom high temperature stockwork veins in bothdeposits overlap with those of the age-correctedmagmatic host signatures. Fluid inclusion ratios areindistinguishable from high temperature sulfides butless radiogenic than galena from the same deposits.Melt inclusions from feldspar cores show arange from values less radiogenic to more radiogenicthan the host rocks, indicating magma mingling,which was also observed in the field. Feldspar coreratios are more radiogenic than host rocks. Host rocksignatures are therefore dominated by the moreprimitive magmatic input that is recorded in inversefeldspar and amphibole zoning (Ivascanu et al.,2004). Results favor the theory that ore depositionaccompanies a later, more primitive pulse ofmagmatism (e.g. Halter et al., 2005; Kamenov et al.,2005).REFERENCESHalter, W., Heinrich, C., and Pettke, T. (2005)Mineral. Depos. 39: 845-863.Ivascanu., P., Kouzmanov, K., Pettke, T., Heinrich,C. (2004) IGCP 486: 229-230.Kamenov, G., Perfit, M., Jonasson, I., and Mueller,P. (2005) Chem. Geol. 219: 131-148.Pettke, T., Audetat, A., Oberli, F., Wiechert, U.,Harris, C., and Heinrich, C. (in preparation).68

O26European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 70Combining numerical simulation of hydrothermal processes and fluidinclusions: quantitative reconstruction of ore-forming processesDriesner, T.*, Kostova, B.** and Heinrich, C.A.**Institute of Isotope Geochemistry and Mineral Resources, ETH Zurich, Clausiusstrasse 25, 8092 Zurich,Switzerland**Bulgarian Academy of Sciences, Sofia, BulgariaStand-alone fluid inclusion studies oftenprovide a series of isolated snapshots of the evolutionof a fossil, ore-forming hydrothermal system that maybe difficult to cast into a quantitative, dynamicmodel.Numerical simulations can provide such aquantitative picture for the evolution of a givenhydrothermal process. With recent improvements insimulation methodology, simulations are about toreach the state where they can be used as a reliabletest of the physical realism of geological modelsderived from field and laboratory data.In a case study of this principle, Kostova et al.(2004) presented a synthesis of fluid inclusion datafrom the Yuzhna Petrovitza mine, Madan, Bulgaria.Comparison to numerical simulations (Hayba andIngebritsen, 1997) showed quantitative agreementbetween observed and simulated temperature-depthpatterns (Fig. 1). LA-ICPMS analyses of ore metalsagreed well with predictions from solubility data. Adetailed thermodynamic analysis (Driesner et al.,2005) could quantitatively predict ore grades basedon the composition of the incoming ore fluid (asmeasured with LA-ICPMS) and the simulated T-Pdepthevolution.The presentation reviews the above resultsand outlines a few fundamental physical principlesthat make a given hydrothermal ore deposit likely tobe the result of an interplay of processes in a verylimited parameter space. This is in contrast to theabundant view that hydrothermal ore deposits are theresult of a rather arbitrary and unconstrainedinteractions of various natural processes. Thecombination of careful fluid inclusion studies andnumerical simulation is the tool of choice if trulyquantitative reconstructions of fossil systems shall beobtained.REFERENCESDriesner T. Kostova B., Heinrich C.A. (2005) V.M.Goldschmidt Conference: A157Hayba D. and Ingebritsen S.E. (1997) J GeophysRes B102: 12235-12252Kostova B., Pettke T., Driesner T., Petrov P., andHeinrich C. A. (2004) Schweiz. Miner. Petrog. Mitt.,84, 25-36.Fig. 1. A: Fluid inclusion homogenization temperatures from three different paragenetic stages in thedevelopment of the Yuzhna Petrovitsa deposit, Madan (Kostova et al, 2004 and Driesner et al., 2005). B:comparison of the results shown in Fig. A to simulations presented by Hayba & Ingebritsen (1997).70

O27European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 72The formation of the World’s largest silver deposit, Cerro Rico, BoliviaBanks, David*, Rice, Clive**, Steele, George***, Boyce, Adrian**** and Fallick, Tony*****School of Earth and Environment, University of Leeds, U.K.**Department of Geology and Petroleum Geology, University of Aberdeen, Aberdeen, U.K.***Rio Tinto Mining and Exploration Ltd, Santiago, Chile.**** SUERC Rankine Avenue, East Kilbride, Glasgow, U.KCerro Rico de Potosi is the world’s largestsilver deposit. Since 1544 production has exceeded2 billion ozs and 100,000 tonnes of tin. Cerro Rico isprimarily a vein-hosted mineral deposit and is bestclassified as a Bolivian polymetallic vein deposit.Bonanza vein and disseminated silver ores weredeposited in an advanced argillic lithocap in theupper part of the deposit and tin is found in veins atdepth. The deposit is centred on a rhyodacite dome,dated at 13.8 Ma, located on the western boundary ofan early Miocene caldera complex.We have measured the homogenizationtemperatures, salinities and chemical compositionsof fluid inclusions hosted by quartz phenocrysts in thedacite dome, early quartz-tourmaline alteration facies,the three stages of vein formation and latehydrothermal barite in the lithocap. Quartz phenocrystsfrom the dacite dome contain high salinity, L-W-Sbrines, V–rich inclusions and L-W fluids co-existingwith melt inclusions that have compositionscorresponding to fractionated granites and they alsocontain elevated levels of silver. A medium salinity,L-W fluid persists through the different parageneticstages and is diluted by low salinity meteoric watersin the last stages of mineralization. Th of inclusions atthe magmatic stage are c. 300 ° C decreasing graduallyto c. 220 ° C in the later stages of mineralization. Thelate stage barite mineralization is significantly cooler.The L-W-S brines have salinities of c. 35% NaClequiv. and the L-W fluid, responsible for themineralization, has a salinity of c. 13% NaCl equiv.LA-ICP-MS analyses of individual inclusionsshows that at the magmatic stage the L-V-S brinescontain 19 ppm Ag, V-rich inclusions 4 ppm and theL-V inclusions 360 ppm increasing to 640 ppm in theinitial hydrothermal stage and decreasing to

O28European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 74What do melt inclusions tell us about the mantle?Szabó Csaba *,***Lithosphere Fluid Research Laboratory, Eötvös University, Budapest, Hungary**Division of Earth Environmental System, Pusan National University, Busan, KoreaMelt inclusions (MI), in general, are smalldroplets of any kind of melts enclosed in a hostmineral, which were trapped accidentally at hightemperatures (±pressures) and subsequently quenchedor partially or totally crystallized. In mantleenvironments silicate MI are the most abundant, howeversulfide and carbonatite MI also occur and arerelevant to the focus of interest.Silicate melt accumulations in the mantleoccurring as inclusions, melt pockets, interstitialglass patches and veins have been described fromseveral localities of upper mantle xenoliths all overthe world (e.g. Schiano and Bourdon, 1999). Thesemelt accumulations provide essential information onmelting and melt migration related to processes ofmetasomatism, melt-mantle interaction, and fluidmeltimmiscibility, which impart incompatible major,minor and trace elements into depleted regions ofotherwise fertile mantle. Also, silicate MI are keymaterials to reveal post-entrapment processes suchas crystallization on the inclusion walls or immiscibilityof volatiles and silicates within the inclusions (e.g.,Danyushevsky et al., 2000).The most important message of MI studies inmantle xenoliths is that they may preserve thecomposition of high pressure and temperature melts,because the large elastic modulus of their hostmantle silicates (e.g., orthopyroxene, clinopyroxene,olivine) prevent them from low-pressure re-equilibrationand decompression during ascent to thesurface. It is noteworthy that, by contrast, interstitialglass patches, melt pockets or veins in the uppermantle xenoliths significantly re-equilibrate and theirchemical composition and/or textural features usuallyreflect lowering pressure and temperature conditions(e.g., Schiano and Bourdon, 1999). Therefore, earlystageor primary silicate MI from deep lithosphereenvironments are generally considered to be mantlesilicate melts that were trapped at high pressure andtemperature in equilibrium with the peridotiticassemblages.It is generally accepted that sulfide MI canprovide insight into processes such as mantledepletion and enrichment, as well as the origin of Fe-Ni-Cu sulfide ore bodies. Petrographic and majorele ment characteristics of sulfide phases in uppermantle xenoliths are consistent with their origin as animmiscible phase formed during partial melting.Other workers, however, have also suggested anorigin by metasomatic fluid infiltration of thelithospheric mantle. Re-Os isotopes of sulfide MI inmantle peridotites have lately contributed much informationon ages of the lithospheric mantle (e.g., Alardet al., 2002).Studies on primary carbonatite MI provideinformation on genesis of carbonatite, as well asformation of other low-degree partial melts in themantle. Primary carbonatite melts are regarded asparticularly reactive agents with extremely lowviscosity and their entrapment as MI is a distinctiveevent in the mantle. Generally, carbonatite melt isinterpreted as one the most important carriers ofincompatible trace and major elements, which widelycontribute to the metasomatic processes of the uppermantle. Although the trace element content of nearsolidusmelts such as e.g., carbonatite is still poorlyknown, their study provides significant knowledge tobetter understand element partition under mantleenvironments (e.g., Lee et al., 2000).REFERENCESAlard, O., Griffin, W.L., Pearson, N.J., Lorand, J.-P.and O’Reilly,S. (2002) Earth Planet. Sci. Lett. 203:651-663.Danyushevsky, L.V., Della-Pasqua, F.N. & Sokolov,S. (2000) Contrib. Mineral. Petrol. 138: 68-83.Lee W. J., Huang W. L. and Wyllie P. J. (2000)Contrib. Mineral. Petrol. 138: 199-213.Schiano, P and Bourdon, B. (1999) Earth Planet.Sci. Lett. 169: 173-188.74

O29European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 76Inclusions of saline melts in halite from chloride xenoliths ofUdachnaya-East kimberlite, SiberiaGrishina, Svetlana*, Polozov, Alexander **, Titov, Anatoly* and Goryainov, Sergey**Institute of Geology, Mineralogy and Petrography, Novosibirsk, 630090 Russia**Institute of Geochemistry, Irkutsk , RUSSIASeveral recent papers have reported themantle origin of chloride-carbonate nodules inkimberlites from the Udachnaya-East pipe (Siberia)(1-2). Alkali components have been found in carbonateand olivine-hosted inclusions in Udachnaya kimberlites(3-4).We have studied inclusions in halite from 7dominantly chloride xenoliths (containing more than80% of halite) in kimberlites from the same occurrence.Primary inclusions in all the samples are abundantwater-free CO 2inclusions of low density. Usually CO 2gas inclusions occur along with mineral inclusionsand inclusions of saline melts. Besides separate gasinclusions, gas phase occur as the part of combinedmineral inclusions or in inclusions of saline melts.Most common is unusual habit of gas phaseincorporated in sylvite crystals (Fig.1b).Inclusions of saline melts consist of crystallinephases including sylvite, KCl, CaCl 2, anhydrite orcalcite, and gas (Fig. 1). The absence of water inthese solids is demonstrated by the total absence ofsymmetric and asymmetric stretching vibrations inthe 3000-4000 cm -1spectral range of the Ramanspectrum. Some inclusions contain silicate and orephases such as magnetite and Ti-magnetite.aFigure 1. a - an open cavity of a CO 2-bearingmultiphase inclusion: 1- CaSO 4, 2, 3 - KCl 4-NaCl.BSE image; b – inclusion of the same type incrossed nicols.bCO 2Sylvite, highly hygroscopic solid KCl, CaCl 2and anhydrite also occur as mineral inclusions inhalite in all studied samples. Identification ofephemeral Ca-bearing chlorite inclusions were madeby Raman spectrum and EDS analysis (5). Thetypical habit is orientation of elongate sylvite crystalsat 45 o or 0 o to the cleavage of halite.Halite is a unique mineral that contains distinctinclusion types for sedimentary, hydrothermal ormetamorphic origin (5-6). Inclusions of saline meltsrepresent a new inclusion type for halite, and exhibitcharacteristic structures of crystallization from salinemelt. Their homogenization temperatures range from600 to 730 o C. Petrography, composition and thesculpture structure of the inclusions are evidence ofa high temperature water-absent origin. However, itis not evidence of a magmatic origin. Halite fromxenoliths has undergone melting at high temperature,but originally it could represent material assimilatedfrom the country sedimentary rocks.AcknowledgmentsWe thank Victor Sharygin and Anatoly Tomilenko fordonating samples and helpful comments.REFERENCES1. Kamenetsky, M.B., et al., (2004), Geology 32:845–848.2. Maas, R., (2005), et al., Geology 33: 549–552.3. Kamenetsky, V.S., et al., (2007) Chem. Geol.237: 384–4004. Golovin, A.V., et al., (2007), Petrology 15: pp.168–183.5. Petrychenko, O.Y. et al., (2005), Chem.Geol.,219:149-1616. Grishina S, Dubessy J. Kontorovich, A, Pironon,J. (1992) Eur. J. Mineral., 4 : 1187-1202.76

O30European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 78Primary carbonatite melt inclusions in apatite and in K feldspar fromclinopyroxene-rich mantle xenoliths from Hungarian lamprophyres:implications for generation and evolution of carbonatite melts in theEarth’s mantleGuzmics, Tibor a , Kodolányi, János a, b , Kovács, István a, c , Bali, Eniko a, d , Zajacz, Zoltán a, e , Halter, Werner e andSzabó, Csaba a, faLithosphere Fluid Research Laboratory, Eötvös University, Budapest, HungarybInstitute of Geology, University of Bern, SwitzerlandcResearch School of Earth Sciences, The Australian National University, Canberra, AustraliadBayerisches Geoinstitut, Universität Bayreuth, GermanyeDepartment of Earth Sciences, Institute of Isotope Geochemistry and Mineral Resources, ETH,SwitzerlandfDivision of Earth Environmental System, Pusan National University, Busan, KoreaWe have studied metasomatic mantle xenolithsconsisting of clinopyroxene, apatite, K feldspar andphlogopite (CAKP) in lamprophyre dikes of theAlcsútdoboz-2 (Ad-2) borehole, Hungary (Szabó etal., 1993). Large numbers of primary, negative crystalshaped carbonatite melt inclusions (CMI) are trappedin apatite and K-feldspar.However, they are absent inclinopyroxene (Cpx) and phlogopite (Phl). Cpx andPhl are thought to represent the metasomatic reactionzone of the “initial” melt of the CMI, whereas apatite(Ap) and K feldspar (Kfs) are considered to be directcrystallization products of the same melt.Carbonatite melts that are trapped as meltinclusions have phosphorous dolomitic compositionin Ap and alkaline-siliceous dolomitic composition inKfs. Both apatite- and K feldspar-hosted CMI showpost entrapment crystallization onto the wall of meltinclusions. The amount of apatite crystallized ontothe wall in apatite-hosted CMI and the bulk compositionof these CMI have permitted us to calculate theentrapment temperature by using the Baker-Wyllieequation (1992). Calculations show an entrapmentT-range of 1090 – 1180 o C. As these melts sampledin Ap and Kfs cannot be the differentiation productsor residuums of each other, they are likely to havebeen formed by liquid-liquid separation, whichrequires their common origin. This is confirmed byREE patterns of numerous apatite-hosted CMI similarto that of K feldspar-hosted ones (Fig. 1), analyzedby LA-ICPMS. Due to liquid-liquid separation U, Th,Ba, Pb, Nb, Ta, P, Sr, Y and all the analyzed REE arepartitioned into the P-bearing carbonatite melt,whereas Cs, Rb, Na, K, Al, Zr and Hf prefer thesilicate-bearing one.Fig. 1. Average PM-normalized REE-patterns of 60CMI in apatite and 20 CMI in K-feldsparTheoretical considerations coupled withmathematical calculations, and a relevant pseudoternarysystem (Ap–Kfs–MgCO 3+CaCO 3+FeCO 3+Na 2CO 3+K 2CO 3) strongly indicate that duringmetasomatic reaction with ultramafic wall rock; thecomposition of the “initial” carbonatite melt changedin a way that resulted in the separation of twoimmiscible melts: a phosphate carbonatite and acarbonate-bearing alkaline aluminosiliceous melt.This process led to the formation of the reaction zone(Cpx and Phl), and oversaturation of apatite and K-feldspar in the phosphate carbonatite melt and in thecarbonate-bearing alkaline aluminosiliceous melt,respectively, which initiated the crystallization of thehost minerals (Ap and Kfs) from a continuouslypercolating melt(s).REFERENCESBaker M. B. and Wyllie P. J (1992) GeochimCosmochim Acta 56: 3409-3422.Szabó et al. (1993) Mineral. Petrol. 47:127-148.78

O31European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 80CO 2-rich fluid inclusions in upper mantle derived xenoliths (WesternHungary, Tihany): a microthermometric and Raman microspectroscopicstudyBerkesi, Marta*, Hidas, Károly* and Szabó, Csaba**Lithosphere Fluid Research Lab, Department of Petrology and Geochemistry, Eötvös University, PazmanyPeter stny. 1/c, Budapest, H-1117 Hungary, (http://lrg.elte.hu)The Tihany Maar Complex is the oldest volcano(K/Ar ages: 7.92±0.22 Ma, Balogh & Németh, 2005)of the Bakony-Balaton Highland Volcanic Field(BBHVF) in the central part of the Pannonian Basin(Hungary). Mantle derived spinel peridotite xenolithssporadically occur in the volcanic edifice. Peridotitesare mostly orthopyroxene-rich harzburgites withpoikilitic texture. The modal composition, texturalfeatures and major element composition of thesilicate minerals suggest that these orthopyroxenerichrocks were formed through an interaction ofSiO 2-rich silicate melt and peridotite wall-rock (Hidas,2006).Individual CO 2fluid inclusions have beenidentified in the peridotite xenoliths. Based on petrographicfeatures, two types of fluid inclusions havebeen distinguished. Type-1: orthopyroxene-hostednegative crystal shaped inclusions with size up to70-μm containing one phase (liquid) at ambientconditions, and type-2: orthopyroxene- and olivinehostedelongated or irregular shaped inclusions witha size varying between 5 and 20 μm. Latter onescontain one (liquid) or two (liquid and vapor) phasesat ambient conditions.The CO 2fluid inclusions have been studiedusing microthermometry and Raman micro spectroscopy.The microthermometric data suggests that inmost cases the fluid phase of the inclusions is pureCO 2(Tm = -56,6 - -56,9 o C). Furthermore, type-1inclusions have higher densities (0.89-1.12 g/cm 3 )than type-2 ones (type-2: 0.5-0.9 g/cm 3 ) in allxenoliths. Results from microthermometry suggestthe presence of further volatile species in some of thexenoliths, based on the Tm that is lower than that ofpure CO 2(

O32European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 82LA-ICP-MS analysis of inclusions: Improved ablation and detectionGuillong, Marcel, Heinrich, Christoph A.Department of Earth Sciences, Swiss Federal Institute of Technology, ETH Zürich, SwitzerlandQuantitative analysis of fluid inclusions byLaser Ablation ICP Mass Spectrometry is still ademanding task for both the analytical equipmentand the operator. Instrumentation that is dedicated toablation work and mainly to inclusion microanalysis isthe optimal, perhaps even the only path to success.Since 10 years (Gunther et al., 1998), the use of ahomogenized ArF excimer laser ablation system isestablished as the best suited for the controlledablation of inclusions in different kind of matrices,including quartz in particular. Recently, femtosecond(fs) UV lasers were used for ablation of solids(Gonzalez et al., 2004; Horn et al., 2006) but so farno published study described the ablationcharacteristics of quartz and inclusions.Due to the hardness and brittle nature ofquartz, controlled ablation is difficult even with shortUV wavelengths (193 nm) and a high energy density(40 J/cm 2 ). When ablating fluid inclusions intransparent minerals such as quartz, cracking nearthe crater rim commonly occurs; inclusions may alsoleak into cracks, or even explode. These processesoften result in non-representative sampling, thuspreventing quantification.An established strategy to reduce theseunwanted effects is the stepwise opening of the fluidinclusion, as described in Gunther et al., (1998). Inthe present study, an iris diaphragm was used tocontinuously increase the crater diameter from thesmallest possible opening (approx. 0.2 mm resultingin an 8 μm crater) to the desired crater diameter(Figure 1). With this technique, the cracking can bereduced significantly, and the final crater size can beprecisely adjusted to the given inclusion size.Short and well-shaped signal shapes improvedetection and quantification quality, but manyapplications are still limited by small inclusion sizeand low element concentrations. To improve the limitof detection for elements such as gold, copper, orplatinum group elements (PGEs), a number oftechnical measures are being tested and will bediscussed in this presentation.A promising approach is the addition of smallamounts of methane, nitrogen or hydrogen to the He-Ar carrier gas (Durrant, 1993; Sesi et al., 1994). Theadditional gas flows were optimized between 0 and20 ml/min. Improvements in sensitivity and limit ofdetection, but also additional interferences will bediscussed.Fig. 1. Dynamic crater diameter increase using aniris diaphragmREFERENCESDurrant, S.F., (1993), Fresenius Journal of AnalyticalChemistry,347, 389-392.Gonzalez, J., Liu, C.Y., Mao, X.L., and Russo, R.E.,(2004), Journal of Analytical AtomicSpectrometry,19, 1165-1168.Gunther, D., Audetat, A., Frischknecht, R., andHeinrich, C.A., (1998), Journal of Analytical AtomicSpectrometry,13, 263-270.Horn, I., von Blanckenburg, F., Schoenberg, R.,Steinhoefel, G., and Markl, G., (2006), Geochimicaet Cosmochimica Acta,70, 3677-3688.Sesi, N.N., Mackenzie, A., Shanks, K.E., Yang, P.Y.,and Hieftje, G.M., (1994), Spectrochimica Acta PartB-Atomic Spectroscopy,49, 1259-&.82

O33European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 84AMS a new software package for reduction of Laser Ablation ICPMSdataMutchler, S.*, Fedele L.* and Bodnar R. J.** Department of Geosciences Virginia Tech, 4044 Derring Hall (0420), Blacksburg, VA 24061 USATechniques for data collection and algorithmsfor the reduction of LA-ICPMS spectra have beenwidely published. However, the absence of userfriendly software has made data reduction a laboriousand error prone exercise. The data reduction processusually takes far longer than the actual collection ofthe ICPMS spectra. The AMS software package wasdeveloped in order to make LA-ICPMS data reductiona routine, accurate and easily reproducible task.Special emphasis was placed on data reduction foranalyses of fluid and melt inclusions; however AMSallows one to reduce data for analysis of anymaterial.AMS allows fluid inclusion concentrations to bedetermined directly from bulk salinities obtained bymicrothermometry. Melt inclusion concentrations canbe determined using normalization to 100% oxide orusing a known internal standard (such as an elementconcentration obtained from EPMA analysis) bothanalyzing an exposed (glassy or homogenized) meltinclusion, or calculating a host correction factor whenanalyzing a crystallized melt inclusion. AMS alsoincludes an improved method of drift correction,taking into account the real temporal sequence forexternal standard and sample analysis, while thecurrently available commercial software for LA-ICPMS data reduction assumes that all analyses areevenly spaced in time. Taking into account the truetime of the analysis allows the AMS software tocalculate a more accurate drift correction factor.Isotopic fractionation is major source of error inLA-ICPMS analyses and the amount of fractionationvaries by element. AMS generates a series ofdetailed plots for each element that show changes inelemental ratios and calculated concentrations as afunction of integration region. These plots can beused to determine the magnitude of fractionation foreach element during an analysis. Finally one of thelargest sources of error for LA-ICPMS analysis iserrors in the composition of the ICPMS standardsthemselves; AMS allows data reduction with the useof multiple standards for each sample analyses,improving the accuracy of the analytical data.Fig. 1. AMS software showing temporal driftcorrection using NIST610 and NIST612 asstandards84

O34European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 86LA-ICPMS analyses of silicate melt inclusions in co-precipitatedminerals: Quantification, data analysis and mineral/melt partitioningZajacz, Zoltán* and Halter, Werner**ETH Zürich, ETH Zentrum NW, Clausiusstrasse 25., Zürich, 8003 SwitzerlandWe present a new approach to determine thecomposition of silicate melt inclusions (SMI) usingLA-ICPMS. In this study, we take advantage of theoccurrence of SMI in co-precipitated mineral phasesto quantify their composition without depending onadditional sources of information. Quantitative SMIanalyses are obtained by assuming that the ratio ofselected elements in SMI trapped in different phasesare identical. In addition, the Fe/Mg exchange equi libriumbetween olivine and melt was successfullyused to quantify LA-ICPMS analyses of SMI inolivine.Results show that compositions of SMI fromthe various host minerals are identical within theiruncertainty (Fig. 1). Thus, (1) the quantification approachis valid, (2) analyses are not affected by thecomposition of the host phase, (3) the derived meltcompositions are representative of the original melt,excluding significant syn- or post-entrapment modi ficationsuch as boundary layer effects or diffusivereequilibration with the host mineral.Fig. 1. Comparison of the composition of silicatemelt inclusions in co-precipitated olivine andplagioclase. Concentration of major elements areplotted in wt% oxides, trace elements are plotted inppm of the element.With these data we established a large set ofmineral/melt partition coefficients for the investigatedmineral phases in hydrous calc-alkaline basalticandesiticmelts. The clinopyroxene/melt and plagioclase/meltpartition coefficients are consistent withthe lattice strain model of Blundy and Wood (1994)(Fig. 2).Fig. 2. Clinopyroxene/melt partitioning datacalculated using the SMI and host mineralcompositions as a function of effective ionic radius.Lines represent the fit obtained by the theoreticalmodel of Blundy and Wood (1994).In addition, our results showed that most plagioclaseand some olivine hosted SMI are cha racterizedby highly elevated Cu and Ag con centrations.This is due to heterogeneous entrapment of a Cu, Agand S-rich magmatic vapor phase and indicatesefficient transport of these elements by exsolvingvolatiles in early stages of magmatic evolution.Our new approach enables the investigation ofmelt inclusions in a much larger variety of systemsthan previously accessible.REFERENCESBlundy and Wood (1994) Nature 372: 452-454.86

O35European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 88Formational conditions for the Dyakou emerald occurrence,Southeastern Yunnan, ChinaXue, Guang* and Marshall, Dan**Earth Sciences Department, Simon Fraser University, Burnaby, BC, V5A 1S6, CanadaThe Dayakou emerald occurrence is locatednear the town of Mengdong in southern MalipoCounty in Yunnan Province, China. It occurs in thecentral area of the Nanwenhe metamorphic corecomplex, which sits between the Honghe fault zoneand the Wenshan-Malipo fault-fold zone, which areparts of Southeastern Yunnan fold belts on thewestern margin of the Yangtze platform.Previous work (Feng et al., 1998) determinedthat emerald mineralization occurs in two sets ofstructures; a set of NW-trending late-Silurian shearbands paralleling the main plane of foliation in theNanwanhe metamorphic complex and a set of late-Cretaceous NE-NNE-trending tensional fractures.These structures are infilled by felsic pegmatite veinsand quartz veins respectively. Typically, emeraldswithin pegmatite veins are more abundant and havebetter crystal form than emeralds associated with thequartz veins.Based on the study of fluid inclusions inemerald crystals, Zhang et al. (1999) determined thefluid inclusions within the emerald veins were H 2O-CO 2inclusions and estimated the homogenizationtemperatures for pegmatite veins and quartz veins at248 - 323 °C and 231 - 280 °C respectively. Salinitieswere also estimated to be 5 to 12 and 8 to 14 wt%NaCl equivalents for pegmatite veins and quartzveins respectively.Mapping and fluid inclusion studies as part ofthis study are consistent with all emerald mineralizationoccurring during the Cretaceous. This studyidenti fied a number of two-phase (L+V) saline fluidinclusions within the quartz, fluorite and emerald. Icenucleation temperatures between -30 °C and -45 °Cwere most commonly observed, as were eutectictemperatures between -8 °C and -23 °C and icemelting temperatures above -6.5 °C, corresponded tosalinities ranging up to approximately 10 wt% NaClequivalent for the general inclusion population. Totalhomogenization temperatures varied widely, with thebulk of the data falling between 160 °C and 260 °C.Total homo genization temperature data for inclusionswithin zoned emerald (Fig. 1) were better constrained,ranging from 200 °C to 260 °C. Moroz et al. (2004)reported similar results.Combined fluid inclusion isochores and independentmeasures of regional metamorphic gradeconstrain maximum temperatures to approximately550 °C and 6,000 bars.Fig. 1. SEM Cathode Luminescence photo of azoned emerald from Dyakou, China.REFERENCESFeng, M. G. et al. (1998) Regional geologicmapping report for Malipo and Dulong sheet at1:50,000. Yunnan, China: Internal publication,Yunnan bureau of geology and exploration.Moroz, I., Vapnik, Y. et al. (2004) in Pecchio, M.,Andrade, F.R.D., et al (eds.): Applied Mineralogy:Developments in Science and Technology.Proceedings ICAM 2004.Zhang, S., Feng, M., et al. (1999) GeologicalScience and Technology Information, 18: 50-54. (inChinese)88

O36European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 90Na-Ca-Mg rich brines and talc formation in the giant talc deposit ofTrimouns (Pyrenees): Fluid inclusion chemistry and stable isotopestudyBoiron, Marie-Christine*, Cathelineau, Michel*, Dubessy, Jean*, Fabre, Cécile*, Boulvais, Philippe** andBanks, David****G2R, Nancy-Université, CNRS, CREGU, BP 239, 54506, Vandoeuvre-les-Nancy**Géosciences Rennes - UMR CNRS 6118, Université de Rennes 1, Campus de Beaulieu, 35042 RennesCedex-France***School of Earth and Environment, University of Leeds, Woodhouse Lane, Leeds, LS2 9JT, UKFluid transfer at the basement / cover interfaceis frequently at the origin of mineral / metalconcentrations. Few information is known about thefluid origin (primary or secondary of the brines) anddetailed paleo-fluid chemistry (cation ratios, gas/ fluidratios, pH, …) of such deposits. Thus, a multitechniqueapproach based on the analysis ofindividual fluid inclusions has been carried out usingmicrothermometry, Raman spectroscopy, LIBS, LA-ICPMS together with the analysis of bulk leachatesand stable isotope geochemistry on the host minerals.The main objective of the paper is the identification ofthe fluid sources and the processes controlling thecomposition of the fluids in order to propose a modelof fluid circulation at the origin of the formation of oneof the biggest talc deposits in the world. The study isfocussed on the determination of the brine chemistry,especially the Mg content and associated elements,as well as the estimation of the pH of fluids based onthe consideration of chemical reactions.The formation of the Trimouns talc deposit,located in french Pyrenees, is closely linked tohydrothermal fluid circulations occurring during thealpine orogenesis in a shear zone between the SaintBarthelemy gneissic dome and the overthrustedcover consisting of marbles, dolomitic formations andblackschists. The T-P conditions of the brine circulationare 250-280 °C and 50 to 200 MPa corresponding to4-7 km depth. This P-T path shows that fluid underwentan important decompression processes favored bythe opening of discontinuities.The fluid responsible of the formation of thetalc deposit is a brine (5 to 6 mol/kg H 2O) showinghigh content in Ca and Na (Na/Ca ranging from 0.5to 2 molal and Ca/Mg from 15 to 21 molal) andcontaining traces of CO 2, CH 4and N 2. Traces of Li,Sr, Ba, Mn, Fe, Cu, Zn and Pb have been analysed.These brines display very low Cl/Br molar ratioranging from 130 to 160.The formation of the altering brine results from:i) the expulsion of a primary brine issued from theevaporation of seawater and having passed thehalite precipitation (Triassic levels) during tertiarytectonic activity and ii) the interaction of this brinewith dolomitic series enriched in organic matter.Brines are thus enriched in Ca (± Br). Interactions ofsuch fluids with blackschists surrounding the depositscould explain the presence of traces of CH 4and N 2inthe brines.Stable isotope compositions of host rocks andnewly-formed minerals (δ 18 O and δD on quartz andchlorite associated with talc) show that i) dolomitesare formed at the expense of marbles during thesame hydrothermal event, and ii) the fluids have anevaporitic brine component and have experiencedsignificant isotopic exchange with crustal rocks. Theyshowed strong interaction with the carbonaceousunits (calcite, organic matter) and basement rocks.90

O37European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 92Fluid inclusion and stable isotope constraints on the origin ofhydrothermal veins in the Gemeric Unit (Western Carpathians)Hurai, V.*, Lexa, O.**, Schulmann K.**, Prochaska W.***, Chovan, M.*****Geological Institute, Slovak Academy of Sciences, 840 05 Bratislava, Slovakia,e-mail: vratislav.hurai@savba.sk**Université Louis Pasteur, UMR CNRS 7516-17, 1 Rue Blessig, Strasbourg, France***Institut für Geowissenschaften, Montanuniversität Leoben, 8700 Leoben, Austria****Department of Mineralogy and Petrology, Comenius University, 842 15 Bratislava, SlovakiaThe Variscan basement of the Gemeric unitcontains more than a thousand siderite, barite andquartz-sulphide veins, from several hundreds metersup to 7 km long, arranged parallel to regional LowerCretaceous metamorphic fabrics. Fluid inclusions inearly siderite vein infilling contain medium salinity,NaCl-CaCl 2-rich brine (17–25 wt. %). According tocovariance of alkali metals, sulphate and halogens,the brine could be correlated with anhydritefractionatedseawater reworked by a low-temperaturediagenesis and a high-temperature interaction withcrustal rocks. Antithetic behaviour of Br-SO 4contentsin the brines is thought to have originated due toprogressive leaching of organogenic sediments andsulphate-to-sulphide reduction at rising temperatures(150–300 °C). Calculated δ 18 O fluidvalues (4–11‰)correlate well with metamorphic grade of the basementrocks, thus supporting the concept of a rock-bufferedfluid system at an early stage of the vein evolution.Fluid inclusions in quartz-tourmaline andquartz-sulphide stages superimposed on the earlysiderite exhibit a wider range of salinities (5–35 wt. %total, relative to H 2O). Enrichment in CaCl 2isinterpreted as reflecting advanced metamorphicdehydration and mixing of the modified basinal brinewith a low salinity fluid component. Immiscible CO 2-dominated (±N 2, CH 4) volatile phase indicate influx ofa deep-seated fluid of metamorphogenic or mantleorigin in an open hydrothermal system.Depths of burial derived from fluid inclusionisochores, oxygen isotope gradients, and formationtemperatures are consistent with a metamorphogenicorigin. The early siderite crystallized at 6–11 kmdepth and the quartz-tourmaline assemblageoriginated at depths of 11 15 km. The correspondingfluid thermal gradients between 13 and 39 °C/kmagree with those inferred from Alpine metamorphicmineral assemblages. The ore-forming brines arethought to have infiltrated from overlying tectonicallysqueezed Permian-Triassic authochthonous coverand/or from the Mesozoic nappes overriding theGemeric basement during the Early Cretaceous(110–140 Ma) compression and thrusting. Theconcept of descendent fluids accounts forcrystallization of barite in the proximity of Permian-Triassic sediments. Iron was leached from basicvolcanoclastics during initial stages of the veinevolution, whilst the sulphidic stages associated withUpper Cretaceous transpressive shearing may havebenefited from supply of elements from hypothesizedmagmatic intrusions.92

O38European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 94Fluid inclusion and stable isotope evidence for percolation of basinalbrines in the Athabasca Basement around the Rabbit Lake, Eagle Point,P-Patch and Millenium unconformity-related uranium deposits, CanadaRichard, Antonin*, Boiron, Marie-Christine*, Cathelineau, Michel*, Boulvais, Philippe**, Banks, David***,Mercadier, Julien* and Cuney Michel**G2R, Nancy-Université, CNRS, CREGU, BP 239, 54506, Vandoeuvre-les-Nancy**Géosciences Rennes - UMR CNRS 6118, Université de Rennes 1, Campus de Beaulieu, 35042 RennesCedex-France***School of Earth and Environment, University of Leeds, Woodhouse Lane, Leeds, LS2 9JT, UKThe aim of this study is to determine thecomposition of the paleo-fluids trapped in pre-, syn-,and post-ore quartz and dolomite veins around fourbasement-hosted unconformity-related uraniumdeposits, by using microthermometry, Ramanspectroscopy, crush-leach, LIBS and LA-ICP-MSanalyses on fluid inclusions, coupled with δ 18 O andδ 13 C measurements on host minerals.Unconformity-related uranium deposits are theworld’s largest low-cost uranium resource and occurat the interface between an Archean to lower-Proterozoic basement and a middle-Proterozoicintracratonic basin, mainly in the Athabasca Basin,Canada and in the Kombolgie sub-Basin, Australia.U mineralizations are either sediment-hosted or basement-hostedwhich stresses on the different possibleore-forming fluid regimes and uranium sources (Quirt,2003). With exception of the Rabbit Lake deposit(Derome, 2002) no fluid inclusion studies have beenperformed in basement-hosted deposits of theAthabasca Basin.Three types of fluids are commonly identifiedaround both basement-hosted and sediment-hosteddeposits: a NaCl-rich brine, a CaCl 2-rich brine and alow salinity fluid (Derome et al., 2005, 2007). Herethese three fluid types have been recognised in alldeposits.LA-ICP-MS analyses allowed to define thedistribution of major (Na, Ca, Mg, K, Li) and traceelements (Cu, Zn, Sr, Ba, Pb, Mn, Fe and particularlyU) in each fluid type, giving for the first time arelatively complete and accurate quantitativedescription of these fluids. Cl/Br ratios of bulk fluidinclusion populations measured by crush-leachconfirmed the basinal origin of the fluids. Moreprecisely, both the NaCl- and CaCl 2-rich brinesappear to be originally evaporated seawater thatcould have been expelled from evaporitic layersduring burial diagenesis. Stable isotope systematicsargue for an isotopic exchange between basinderivedfluids and the basement lithologies. TheCaCl 2-rich brine is thought to have exchanged Na forCa during fluid-rock interaction (albitization,chloritization) in the basement. The low salinity fluidis potentially of meteoric origin, or basementderived.Our results show that massive percolation ofbasinal brines occurred in the Athabasca Basementclose to the Rabbit Lake, Eagle Point, P-Patch andMillenium deposits. Although the exact role of thesebrines in the mineralization process is still a matter ofdebate, it appears that this percolation event is linkedwith all stages of alteration, including ore deposition.More generally, this study is a new contributionto the understanding of fluid transfer at the basementcoverinterface, as numerous U, Pb-Zn, Ag and Cumineralizations are found close to majorunconformities.REFERENCESDerome D. (2002) Unpublished PhD thesis,Université Henri Poincaré, Nancy, France, 232pp.Derome D., Cathelineau M., Cuney M., Fabre C.,Lhomme T. (2005) Econ. Geol. 100: 1529-1545.Derome D., Cathelineau M., Fabre C., Boiron M-C.,Lhomme T., Cuney M. (2007) Chem. Geol. 237: 3-4.Quirt D. (2003) Uranium Geochemistry 2003,Proceedings of an international conference, Nancy,France.94

O39European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 96Hypogene fluid responsible for the transformation of BIF to high-gradeiron ore (>65 wt %); insights from the 4 East deposit, Paraburdoo,Western AustraliaThorne, Warren*, Hagemann, Steffen* and Banks, David***Centre for Exploration Targeting, School of Earth and Geographical Science, University of WesternAustralia, Crawley, Western Australia, 6009 Australia**School of Earth Sciences, University of Leeds, Woodhouse Lane, Leeds, L52 9JT, United KingdomThe Paraburdoo deposit lies about 65 kmsouth of Mount Tom Price at the southern margin ofthe Hamersley Province. Recent deep drilling atParaburdoo, below the 4 East deposit, was completedto delineate deep extensions of the ore body. Thedrilling also intersected carbonate-altered (50-55 wt%Fe; hematite-dolomite-chlorite-pyrite) Banded IronFormation (BIF) transitional between unmineralisedBIF (~35 wt% Fe) and high-grade (>65 wt% Fe) ironore mineralisation, below the depth of modernweathering. Structural reconstruction of the 4 Eastdeposit suggests that the flat fault zones that nowunderlie the deposit were steeply dipping normalfaults, prior to late tilting. Hypogene carbonatealteration formed primarily in the hangingwall ofthese steeply dipping normal faults. Supergeneoverprint (removal of hypogene carbonate) of thehypogene carbonate-altered BIF results in theformation of high-grade iron ore which consists ofmartite, microplaty and anhedral hematite.Based on a careful petrographic study, primaryfluid inclusions are observed in dolomite fromdolomite-chlorite-pyrite veins in the hematitedolomite-chlorite-pyritealteration zone. Fluidinclusions in dolomite are rounded, ovate and irregularin shape. Their sizes are between 5-40 µm indiameter. They contain a liquid and vapour phasewith L/V ratios of 0.6 to 0.95. Fluid inclusions indolomite reveal only H 2O–CaCl 2primary inclusionsthat show high salinity (average 20.9 CaCl 2eq. wt%)and Th TOT(L)= 130 ± 11 o C (1σ; n=52). QuantitativeLA-ICPMS microanalysis of primary fluid inclusionsfrom dolomite in dolomite-chlorite-veins yield 6.1-10.8 wt% Ca (ave. 8.2 %), 5.4-9.5 wt% Na (ave.7.3 wt%), 1.0-7.7 wt% K (ave. 5.2 wt%), 0.6-5.2 ppmCu (ave. 2.2 ppm), 0.8-12.2 ppm Zn (ave. 5.4 ppm),1.7-10.3 ppm Sr (ave. 5.4), 0.4-2.2 ppm (ave. 1.1ppm) Ba, and 0.2-0.9 ppm Pb (ave. 0.4 ppm). Ionchromatography leachates (9 samples) from dolomiteand hematite within hematite-dolomite-chlorite-pyritealteration and hematite from high-grade ore showsimilar mass ratios with Na/K = 3.9 ± 2.1 (1σ, n = 9),Cl/SO 4= 297.1 ± 252.9, and, Na/Li = 1.1 ± 0.7. Thesamples have molar Cl/Br ratios of 175.1 ± 45.3, Na/Br = 45.1 ± 39.5 and K/Na of 0.2 ± 0.1.The fluids responsible for the formation ofhypogene alteration and ultimately high-grade ore atthe 4 East deposit at Paraburdoo were lowtemperature, 130 o C, saline fluids (Ca>Na>K) withelevated Cu and Zn (1.3 and 3.2 ppm, respectively).The high Cl/Br, low Na/Br ratios, high-Caconcentrations, and base metal content of the fluidssuggest that these basinal brines formed fromevaporated sea water and have undergone extensivedolomitization (Luders et al., 2003). Normal faultsthat underlie the 4 East deposit provide the fluidpathway for hypogene fluids from the underlyingcarbonate sequences of the Wittenoom Dolomite intothe unmineralised BIF. Such fluid flow and fluidgeochemistry are typical of Mississippi Valley-Type(MVT) deposits, where faults are the principal conduitsby which ascending metalliferous hydrothermal fluidsaccess limestone units resulting in in-situ dissolutionof the limestone and replacement of the host-rocksand mineralisation. The results from this work providenew insights in the fluids responsible for thetransformation of unmineralised BIF to high-gradeore in the 4 East deposit at Paraburdoo. It alsohighlights the importance of basinal faults that linkthe underlying Wittenoom Dolomite with the BIF as aprimary control on mineralisation.REFERENCESLuders et al. (2005) Int J Earth Science 94:990-100996

O40European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 98Hydrothermal fluid characteristics and evolution for the giant CarajasNorth Range iron deposits, BrazilFigueiredo e Silva, Rosaline C.*, Hagemann, Steffen**, Lobato, Lydia M.*, Banks, David****Departamento de Geologia, Universidade Federal de Minas Gerais, Belo Horizonte, 30670 Brazil**Center for Exploration Targeting, University of Western Australia, Nedlands, WA, 6009 Australia***School of Earth and Environment, University of Leeds, Leeds, LS2 9JT United KingdomIn the Carajás North Range, hydrothermalhigh-grade (>64% Fe) iron ore deposits are hostedby Archaean jaspilites (JP) from the Grão ParáGroup, Itacaiúnas Supergroup, which are under- andoverlain by mafic rocks. This study presents adetailed hydrothermal vein and breccia classificationbased on petrography and microthermometric resultson fluid inclusions trapped in veins and breccias.These data are used to constrain the hydrothermalevolution at the North Range Carajás iron deposits.Based on detailed mapping of the temporalevolution combined with textural features vein-brecciatypes are classified in: (a) brecciated qtz vein in JP;(b) vug-textured hem-qtz bedding-discordant andconcordant vein in JP; (c) brecciated carb (ironcloudy)-quartz vein in ore; (d) qtz-hem beddingdiscordant vein in ore; (e) brecciated qtz-hem vein inore.At room temperature, primary and pseudosecondary(P/PS) inclusions are mostly aqueousliquid-rich (10 to 20 vol. % vapour), with subordinatevapour-rich (70 to 80 vol.% vapour) inclusionsdocumented in vein types (a), (c) and (e). They occuras clusters or internal trails, have oval to irregularshapes and sizes ranging from Ca>K>Mg>Fe>Ba>Sr>Li) and Th TOT(L-V)from 119to 218 ° C. The P/PS inclusions from quartz crystals of(b) display two salinity groups: (1) H 2O-NaCl-FeCl 2-MgCl 2from 6.5 to 6.8 eq. wt % CaCl 2and Th TOT(L)from130 to 180 ° C ,and (2) 11.1 to 24.5 eq. wt % CaCl 2andTh TOT(L)from 148 to 233 ° C. Primary inclusions inquartz crystals from (c) also present two groups: (1)between 1.7 and 6.5 eq. wt % CaCl 2and Th TOT(L-V)between 165 and 190 ° C, (2) the other from 10.5 to22.8 eq. wt % CaCl 2(Na>Ca>Fe>K>Mg>Ba>Sr>Li)and T Th TOT(L-V)ranging from 170 to 219 ° C. Twophasefluid inclusions in carbonate crystals have thehighest obtained salinity values from 19.2 to 30.1 eq.wt % CaCl 2.Quartz inclusions from (d) display lowsalinities (0.5 to 5.5 eq. wt % CaCl 2)(Na>Mg>Ca>Fe>K>Ba>Sr) at Th TOT(L)between 105to 160 ° C, and high salinity (8.9 to 19.5 eq. wt %CaCl 2) at Th TOT(L)ranging from 150 to 187 ° C. Salinityresults from (e) display a group from 0.1 to 6.5 eq.wt % NaCl (Na>Mg>>Fe>K> Ca>Sr>Ba)(Th TOT(L-V)145 to 193 ° C) and between 12.6 and 20.5 eq. wt %CaCl 2(Th TOT(L-V)130 to 234 ° C); some intermediatevalues are also observed. Secondary inclusions invein types (b), (c) and (e) have the lowest salinityvalues of 64% Fe)consists of: (1) medium- to high-salinity (9 to 25 eqwt% CaCl 2) and medium to high temperature brines(Th 105 to 193 °C), and (2) low- to medium salinityTOT(

O41European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 100In-situ Laser ICPMS analyses of pre-, syn-, and post-gold hydrothermalfluids in the Kambalda Gold Camp, Yilgarn craton, Western AustraliaPetersen, K.J.*, Hagemann, S.G.*, Neumayr, P.*, Walshe, J.**, Banks, D.*** and Yardley, B.**** Centre for Exploration Targeting & pmd*CRC, SEGS, The University of Western Australia** CSIRO Exploration and Mining, ARRC, 26 Dick Perry Av, Kensington, Western Australia 6151*** University of Leeds, UKThe Yilgarn craton hosts several of the moststudied Archean orogenic gold deposits in the worldbut still presents challenges for the understanding ofthe complex geometry of hydrothermal fluid flow andthe (micro)-chemical evolution of hydrothermal fluidsthat played a role in the formation of these deposits.This abstract presents preliminary chemicalcomposition data on the different hydrothermal fluidsin the Kambalda gold camp using the in-situ Laserablation ICPMS (LA-ICPMS) technique. The aim ofthis study is to characterize the hydrothermal fluidspre-, syn- , and post-gold mineralization.At the camp scale, oxidized (sulphide-oxide)alteration assemblages are characteristic for the orezones in the Victory and Revenge deposits. Highgold grades are located at the boundary betweenoxidized and reduced assemblages. Three mainstages of hydrothermal alteration assemblages aredefined based on cross-cutting relationships andreplacement textures: Stage 1: pre-Au, exo-skarntype alteration, epidote - magnetite - chalcopyrite± quartz ± pyrrhotite; Stage 2a: syn-Au, proximalpyrrhotite - carbonate - amphibole; distal biotite± albite ± quartz ± arsenopyrite ± pyrite ± sphalerite;Stage 2b: syn-Au, proximal albite - carbonate - pyrite- gold/silver ± magnetite ± hematite ± quartz; distalbiotite - chlorite; Stage 3: post-Au, quartz veins withrestricted quartz - carbonate - chlorite ± pyritealteration zones that crosscut all earlier alterationsstages.LA-ICPMS analyses were conducted onprimary FI’s assemblages trapped in veins andbreccia associated with all alteration stages. Theresults are presented in Table. 1.Skarn-related hydrothermal fluids appear to beunrelated to the gold-bearing fluids and represent anearlier magmatic-hydrothermal event.Table. 1. Microthermometry and LA-ICPMS resultsof fluid inclusions from pre-, syn-, and post-goldmineralization.Distal reduced fluids are characterized by verylow H 2O, high amounts of CH 4+ N 2± CO 2, and saltsand metals when compared to fluids in the proximalzone. Within the ore zone, fluids are composed ofearly possibly pre-Au, H 2O-NaCl and later, possiblysyn-Au, CO 2– H 2O fluids. Given the oxidized sulphideoxide-goldassemblage in specifically high grade goldshoots and the lack of CO 2in the reduced fluids, it isproposed that the distal oxidized fluid conduitscontain abundant CO 2and possibly SO 2. Late stagequartz veins, with H 2O-NaCl rich fluids, crosscut allprevious hydrothermal alteration zones and are,therefore, interpreted to be emplaced post-goldmineralization. In the absence of evidence for phaseseparation, the precipitation of Au is possibly causedby: 1) fluid titration; 2) mixing of distal reduced fluidwith a “postulated” oxidized CO 2rich fluid (presentlynot detected). The CO 2-rich fluids within the ore zoneare relatively salt- and metal-poor and are, therefore,interpreted to represent “spent” fluids, i.e., they weretrapped after precipitation of their metals.100

O42European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 102Gaining insights on magma evolution using melt inclusion data andthermodynamic modeling: two eruptions from Campi Flegrei(Campania, Italy)Fedele L.*, Cannatelli C.*, Spera F.**, Bohrson W.***, De Vivo, B.****, Lima, A.****, and Bodnar R. J.** Department of Geosciences Virginia Tech, 4044 Derring Hall (0420), Blacksburg, VA 24061 USA** Department of Earth Sciences and Institute for Crustal Studies, University of California, Santa Barbara,CA 93106 USA*** Department of Geological Sciences, Central Washington University, Ellensburg, WA 98926, USA**** Dipartimento di Scienze della Terra, Università di Napoli Federico II, 80134 Napoli, ItalyWhile thermodynamic modeling alone cannotunravel all the details of magma crystallization andevolution, it provides a method to test differentevolutionary scenarios and helps to constrain physicaland chemical parameters. We used the thermodynamicmodels built into the MELTS software (Ghiorso andSack, 1995; Asimov and Ghiorso, 1998) to study twoeruptions from Campi Flegrei: Fondo Riccio (FR, 9.5ka) and Minopoli 1 (Mi1, 11.1 ka). Fondo Riccio wasan explosive strombolian eruption that occurred nearthe center of the Campi Flegrei caldera, whileMinopoli 1 was primarily hydromagmatic and occurredalong the regional fault system in the northern portionof the caldera. The present work is part of a broadereffort, beginning with a detailed investigation of theCampanian Ignimbrite (Fowler et al., 2007), whosefinal goal is to reconstruct the whole evolutionaryhistory of the Campi Flegrei volcanic field byinvestigating its eruptive events using a combinationof melt inclusion data and thermodynamic modelling.MELTS simulates magma evolution throughequilibrium or fractional crystallization, and melt andsolid assimilation (both adiabatic and isenthalpic).MELTS requires as input the chemical composition ofthe primitive magma, hence we selected two homo genizedmelt inclusions (MIs) in olivine, with the highestMg content to represent the parental magma forFondo Riccio and Minopoli 1. Despite the potentialdrawbacks, mainly due to their susceptibility to postentrapmentmodifications, MIs provide a betterapproximation of parental magma compared to bulkrock data.We carried out several isobaric, fractionalcrystallization simulations in MELTS, based on recentresults obtained applying MELTS modeling to theCampanian Ignimbrite (Fowler et al., 2007), toconstrain the physical and chemical parameters ofthe eruptions. The simulations were conducted byvarying initial water content and f O2buffer. Resultswere compared with the observed major elementcompositions of crystals, bulk rock and homogenizedMIs in olivine and clinopyroxene to evaluate theextent to which each simulation reproduced obser vationsunder the imposed physico-chemical conditions.Best-fit simulations showed that Fondo Riccio andMinopoli 1 parental magmas were likely trachyandesiticmelts, whose compositions are approximated by thechemistry of MIs in olivine (FR → SiO 246.8, MgO9.45 %; Mi1 → SiO 247.8, MgO 11.5 %), whichevolved mainly through fractional crystallization at0.15 GPa (~ 5 - 6 Km depth), buffered along the QFM+1 (quartz-fayalite-magnetite), and had an initial H 2Ocontent of ~ 3 wt%.The results from MELTS also highlighted thatfractional crystallization alone cannot fully explain thecompositional range of some of the minerals found inthese rocks. To improve the quality of fit betweenobserved and modelled data, we also carried out aseries of simulations to test the hypothesis that themagma assimilated small amounts of country rock.Best-fit trends suggest that assimilation of ≤ 10 %skarns and foid-syenites likely occurred.REFERENCESGhiorso M.S., Sack R.O. (1995) Contrib. Mineral.Petrol. 119:197-212Asimow P.D., Ghiorso M.S. (1998) Am. Mineralogist83:1127-1131Fowler S.J., Spera F.J., Bohrson W.A., Belkin H.E.,De Vivo B. (2007) J. Petrology 48: 459 - 493.102

O43European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 104The fluid evolution of the Motzfeldt intrusion – constraints on agpaitegenesisSchoenenberger, Johannes*, Markl, Gregor**Institut für Geowissenschaften, Universität Tübingen, Wilhelmstr. 56, 72074 Tübingen, GermanyAgpaitic rocks belong to the most fractionatedrocks worldwide and are characterised by (Na+K)/Al> 1.2 and Zr-Ti-silicates like eudialyte and areenriched in elements like Nb, Ta, REE, Th and U upto economical values (e.g. Sørensen, 1997). Untilnow, the processes leading to the formation ofagpaitic rocks and the importance of a fluid phase intheir evolution is a matter of scientific debate.The Motzfeldt intrusion in the mid-ProterozoicGardar Province (South Greenland) can serve as anexample to constrain the transition from miaskitic toagpaitic rocks. The intrusion comprises six intrusivephases (Emeleus & Harry, 1970; Jones, 1984). SM1to SM5 crystallised miaskitic rocks consisting offeldspar, nepheline, Fe 2+ -rich mafites with commonsecondary fluorite (±calcite) veins. Only SM6 consistsof agpaitic rocks with Fe 3+ -rich pyroxene, feldspar,nepheline and eudialyte.In order to constrain the composition ofmiaskitic vs. agpaitic fluids, fluid inclusions wereinvestigated in primary fluorite and nepheline andhydrothermal fluorite and quartz. Most inclusions arefound along trails and are of secondary origin, whilefew inclusions in nepheline are interpreted asprimary.Inclusions in the miaskitic units are typically oflow salinity Br >SO 4and K > Mg > Ba > Sr. The Cl/Br ratios definetwo groups: one between 70 and 120 similar to otherGardar intrusions (see abstracts by Graser et al.,Koehler & Markl, this volume) and the other between260 and 360 which are close to modern seawater.δD and δ 18 O values of inclusion water clusteraround today’s meteoric water line. δ 18 O (VSMOW)and δ 13 C (PDB) of the inclusions’ CO 2revealed twogroups: (1) δ 13 C -11.6 to -17.4‰; δ 18 O 19.3 to 30.6‰;(2) δ 13 C -2.5 to -5.8‰; δ 18 O 28.5 to 42.7‰. The firstgroup is typical of samples associated with carbonateminerals whereas the second group withoutassociated carbonates shows δ 13 C mantle values.The relatively high δ 18 O values are attributed to lowtemperature equilibration with the inclusions’ water(Richet et al., 1977). The δ 13 C of the inclusions’methane define a narrow range between -27.2 and -30.9‰.The isotopic composition shows no differencesbetween the miaskitic and the agpaitic units.Therefore, we assume that the occurrence of CO 2inthe miaskitic rocks (as calcite daughter minerals) andCH 4in the agpaitic rocks is solely attributed todifferentiation (within-magma redox) processes ordecreasing temperature (e.g. Ryabchikov & Kogarko,2006). The occurrence of CO 2is linked with the Fe 2+ -rich mineral assemblage whereas CH 4is associatedwith Fe 3+ -rich minerals indicating that a coupledredox-process could be responsible for the formationof the Motzfeldt agpaites.REFERENCESEmeleus, C.H., Harry, W.T. (1970) Meddel. Grønl.186.Jones, A.P. (1984) Min. Mag. 48: 1-12.Richet, P., Bottinga, Y., Javoy, A. (1977) Ann. Rev.EPSL 5: 65-110Ryabchikov, I.D., Kogarko, L.N. (2006) Lithos 91:35-45.Sørensen, H. (1997) Min. Mag. 61: 485-498.104

O44European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 106Isotopic, major, minor, and trace element geochemistry of late stagefluids in the Ilímaussaq alkaline complex, South GreenlandGraser, Gesa*, Potter, Joanna**, Koehler, Jasmin* and Markl, Gregor**Institut für Geowissenschaften, Eberhard-Karls Universität, Wilhelmstr. 56, 72070 Tübingen, Germany**Department of Earth Sciences, The University of Western Ontario, London, Ontario N6A 5B7, CanadaThe persodic, 1.16 Ga old Ilímaussaq intrusionin South Greenland consists of alkali granites,syenites, and agpaitic nepheline syenites, whichintruded successively as four separate magmabatches at the contact of the early Proterozoicbasement granites, basalts and sandstones. TheIlímaussaq rocks are cut by late-magmatic veinsconsisting of albite, aegirine, ussingite(Na 2AlSi 3O 8(OH)), fluorite and, very rarely, quartz.The oxygen isotopic composition of theminerals indicates different origins for the quartzveins: while the vein in alkali granite is orthomagmatic(8.5‰), the veins in augite syenite (~10‰) are eitherderived from fluids that entered the intrusion from thegranitic country rocks or they formed by digestion of,or reaction with, sandstone xenoliths in this rock unit.While albite and aegirine in the veins do not containfluid inclusions suitable for investigation, ussingitecontains pure hydrocarbon gas inclusions, fluorite,saline brine inclusions of primary and secondaryorigin, and quartz, predominantly primary andsecondary NaCl-dominated saline brine inclusionswith up to 29.7 wt% NaCl equiv.or CH 4-H 2O-NaClmixtures. These fluids are interpreted to reflect thefluids in equilibrium with the late-stage melts atIlímaussaq.The carbon and hydrogen isotope compositionof the included methane resembles the signature ofthermogenic methane (δ 13 C = –28 to –43‰; δD = –121 to –176‰), but the higher hydrocarbons alsoshow features typical of abiogenically derivedhydrocarbons (e.g. 13 C-depleted in relation to theCH 4). The carbon and hydrogen isotope compositionof methane in ussingite is similar to former analysesof Ilímaussaq methane by Konnerup-Madsen (2001)with δ 13 C values between –3 and –6‰ and δD values~–121‰, indicative of a magmatic origin.Ion chromatography of fluid inclusion leachatesfrom the late-stage veins revealed Cl/Br ratios ofabout 100. As such values seem to be typical ofperalkaline magmatic rocks at least in the GardarProvince of South Greenland (Koehler et al. andSchoenenberger et al., this volume), they aresuggested to represent a geochemical fingerprint,typical of Gardar magmatic fluids. In addition, theymay characterize the Cl/Br ratio of the lithosphericmantle from which the alkaline melts are derived. Thegeochemical composition of the late-stage aqueousfluids shows some variability, but is typified bydissolved NaCl and minor amounts of CaCl 2, KCl, Fand Br.REFERENCESKonnerup-Madsen J. (2001) Geology of GreenlandSurvey Bulletin. 190: 159-166106

O45European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 108The many contributions of Edwin Woods Roedder (1919-2006) to fluidand melt inclusion researchBodnar, Robert J.Department of Geosciences, Virginia Tech, 4044 Derring Hall, Blacksburg, VA 24061, USAOn August 1, 2006, the fluid inclusioncommunity suffered a great loss with the passingEdwin Woods Roedder. During the past 150 years,starting with the classic work of Sorby (1858), manyresearchers have made significant contributions tofluid and melt inclusion research, but none havesurpassed Ed Roedder in terms of the impact hiswork has had in this research area.Ed Roedder was born on July 30, 1919, inMonsey, New York. He received his BA degree fromLehigh University in 1941, his Master’s degree fromColumbia University in 1947, and the PhD fromColumbia in 1950. From 1941-46 he worked as aResearch Engineer for Bethlehem Steel Corp. Aftercompleting his PhD he joined the faculty at theUniversity of Utah from 1950-1955. In 1955 he joinedthe U.S. Geological Survey and remained there untilhis retirement in 1987. He continued to be an activeparticipant in research and conferences related tofluid and melt inclusions until his passing at the ageof 87.During his career, Ed Roedder contributedmore than 300 scientific publications. His firstpublication that mentions fluid inclusions was anabstract with the title “Composition and significanceof fluid inclusions in minerals”that was published in1951. In 1962 Roedder published a paper in thepopular science magazine Scientific American thatincluded the first high-quality color photographs offluid inclusions in minerals. In addition to his manypublications related to ore deposits, Ed Roeddermade important contributions in many other areas. In1965, Roedder published an extensive review of theoccurrence of liquid CO 2-bearing fluid inclusions inolivine-bearing nodules and phenocrysts from basalts.This paper was one of the first to emphasize theimportance of carbon dioxide in deep crustal andmantle environments. Roedder was also one of thefirst to recognize the importance of melt inclusions tostudy igneous processes, and he applied hisknowledge to study melt inclusions in lunar samplesthat were returned to Earth by the Apollo missions.And, as early as 1957 Roedder was concerned withthe safe storage of radioactive waste, and hiscontributions to this societally-relevant and importantscientific issue continued to his final days.Finally, any summary of Ed’s many publicationsand contributions to the field of fluid and meltinclusions would be incomplete without mention ofthe book Fluid Inclusions, published as Reviews inMineralogy Volume 12. To date, there have been 62Reviews in Mineralogy (now the Reviews inMineralogy and Geochemistry Series) volumespublished. Volume 12, by Ed Roedder, contains 644pages and 2002 citations to the published literatureand remains the only single-authored volume in theseries. Over 6,500 copies of Fluid Inclusionshavebeen sold, ranking it among the top 5 of all Reviewsin Mineralogy and Geochemistry volumes. Although ithas been over 2 decades since this volume waspublished, it is still considered to be “the Bible” of fluidinclusion research and is must reading for anyserious student of fluid inclusions.Ed Roedder received numerous awards inrecognition of his research, including the ExceptionalScientific Achievement Medal from NASA (1973);Werner Medal from the German MineralogicalAssociation in 1985; Roebling Medal from theMineralogical Society of America in 1986; PenroseMedal from the Society of Economic Geologists in1988; the Sorby Medal at the European CurrentResearch on Fluid Inclusions Conference in 1993. In2002, the inaugural Roedder Medal was presented toEd Roedder at the workshop on the application ofmelt inclusions to volcanic problems that was held atSeiano di Vico Equense, Italy.Ed Roedder will certainly be missed by thoseof us who study fluid and melt inclusions, but he willnot be forgotten.108

O46European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 110The concentrations and fluxes of gold in subaerial hydrothermalsystems of New Zealand and Papua New GuineaSimmons, Stuart F.* and Brown, Kevin L.*** School of Geography, Geology and Environmental Science, University of Auckland, Private Bag 92019,Auckland Mail Centre, Auckland 1142, New Zealand** GEOKEM, P.O. Box 95-210, Swanson, Waitakere 0653, New ZealandWe designed and constructed a titaniumsampler for geothermal wells to obtain deep (~1 km)high temperature (200 to >300 °C) samples ofhydrothermal solutions for analysis of precious andrelated trace metals by ICP-MS. We sampled sixmeteoric-water dominated hydrothermal systems inthe Taupo Volcanic Zone (TVZ), New Zealand, andthe magmatic-water dominated Ladolam hydrothermalsystem, Lihir Island, Papua New Guinea (Simmonsand Brown, 2006). By combining the concentrationdata with the rate of hydrothermal upflow, we alsodetermined gold fluxes for these systems (Fig. 1).The results illuminate the main factors controlling therate of gold deposit formation.Fig. 1. Concentrations and fluxes of gold inhydrothermal systems; B=Broadlands, K-Kawerau,L=Ladolam, M=Mokai, N=Ngatamariki,R=Rotokawa, and W=Wairakei.The TVZ is a young (

O47European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 112Paleohydrology and source of fluids of the Kremnica low-sulfidationepithermal Au-Ag depositKodera, Peter*, Lexa, Jaroslav** and Fallick, Anthony E.**** Faculty of Natural Sciences, Comenius University, Mlynská dolina, 842 15 Bratislava, Slovakia** Geological Institute, Slovak Academy of Sciences, Dúbravská cesta 9, 840 05 Bratislava, Slovakia***Scottish Universities Environmental Research Centre, East Kilbride, Glasgow, UKThe famous Neogene Kremnica deposit issituated on marginal faults of a resurgent horst,associated with rhyolite magmatism. The system ofepithermal veins is dominated by major N-S trendingtranstension fault (“1 st system”), accompanied bysecond order structures, including a largecomplementary “2 nd vein system”. The 1 st system is3.3 km long and >1.2 km deep. Au is present aselectrum in quartz and pyrite in microscopic (in 1 stsystem) or bonanza-type form (2 nd system). About 3km S of the 1 st vein system mineralization continuesin the environment of rhyolite volcanites as low gradequartz-chalcedony veinlets with stibnite. It isaccompanied from N to S by extensive zones ofalteration with kaolinite, illite, I/S and smectite,respectively, locally with limnic/lacustrine silicites(Vel’ký et al. 1998).Fluid inclusion (FI) microthermometry showedsystematic decrease in Th values from ~260 °C to~210 °C on the 1 st vein system from N to S. Samplesfrom the central part showed evidence of boiling offluids at 175 or 200 °C; for S parts at ~130 °C, whichindicates paleodepth of 89 or 164 m and 25 to 50 m,respectively. Average salinities along the 1 st veinsystem are

O48European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 114Magmatic fluids in high-sulfidation epithermal veins overprinting aporphyry copper system: Stable isotope study of pyrite-hosted fluidinclusionsKouzmanov, Kalin* , **, Vennemann, Torsten***, Putlitz, Benita***, Baumgartner, Lukas***, Skora, Susanne***and Heinrich, Christoph A.***Department of Mineralogy, University of Geneva, rue des Maraîchers 13, 1205 Geneva, Switzerland**Institute of Isotope Geochemistry and Mineral Resources, ETH Zentrum, Clausiusstrasse 25, 8092 Zurich,Switzerland***Institute of Mineralogy and Geochemistry, University of Lausanne, BFSH-2, 1015 Lausanne, SwitzerlandTelescoping and transition, in space and time,is a typical feature of porphyry-style and epithermalvein mineralization in subvolcanic intrusions. TheMiocene porphyry Cu-Au deposit of Rosia Poieni(Romania) shows an early porphyry Cu-Au veinstockwork associated with potassic and phyllicalteration zones, overprinted by high-sulfidationepithermal veins with advanced argillic alteration.Up to several millimeter sized primary fluidinclusions hosted by idiomorphic pyrite crystals fromthe high-sulfidation epithermal veins have beenstudied by scanning electron microscopy, IRtransmitted light petrography and X-ray tomography.Volume calculations based on the X-ray tomographystudy reveal that in some samples the fluid inclusioncavities occupy 10-15 % of the volume of the hostcrystal.Crushing under vacuum has been used toextract the hydrothermal fluids from several pyriteand quartz samples from the high-sulfidation veins,as well as two samples of porphyry-stage hydrothermalquartz. The fluids have been analyzed for theirhydrogen isotopic composition. The oxygen isotopiccomposition of the fluids was determined using theisotopic composition of the host quartz or, in the caseof pyrite-hosted fluid inclusions, of the quartzcoexisting with the pyrite. A temperature of 580 °C forthe porphyry fluids and 320 °C for the epithermalfluids has been applied based on oxygen isotopethermometry and fluid inclusions microthermometry(Figure 1).The fluid processes at the porphyry toepithermal transition at Rosia Poieni were dominatedby magmatic fluids, as revealed by the magmaticsignatures of both, porphyry and epithermal fluids.Both fluids show an extreme depletion in δD comparedto typical hydrous magmas and other porphyrydeposits. The low δD values are most probably dueto magma degassing in an open system duringporphyry and epithermal mineralization.Fig. 1. Isotopic composition of porphyry-stage andepithermal fluids from the Rosia Poieni Cu-Audeposit, compared to liquids associated with K-alteration from variety of porphyry deposits (fromHedenquist et al. 1998).REFERENCEHedenquist J.W., Arribas A., Reynolds T.J. (1998)Econ. Geology 93: 373-404114

O49European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 116The Searchlight Mining District: Linking low sulfidation epithermalmineralization with an underlying granitic pluton using fluid inclusionsLledo, Haroldo L.*, and Cline, Jean S.** Department of Geoscience, University of Nevada Las Vegas, Las Vegas, Nevada, USA 89154-4010Epithermal deposits constitute the secondmost important source of gold in the United States.Though an accepted model for this type of depositexists, the relationships between these hydrothermalsystems and underlying magma chambers are poorlyunderstood. The Searchlight Mining District is arelatively small, but high-grade gold district located inthe Colorado River Extensional Corridor, an area thathas undergone a high degree of extension during theMiddle Miocene. Low angle extensional faults havetilted the district as much as 90 degrees to the westexposing a near complete cross section from uppervolcanic rocks on the west, through epithermal veinscutting older volcanic rocks, and into underlyingplutonic rocks to the east. The exposed rocksrepresent an almost continuous cross section ofabout 13 km of paleodepth (Bachl, et al., 2001). Thisextraordinary exposure provides a rare opportunity tostudy in detail a low sulfidation epithermal systemand to examine the link with the underlying magmachamber.The Searchlight Mining District consists of aset of Au-bearing veins with minor Cu, Ag, Pb, andZn. These veins are hosted predominantly in MiddleMiocene plagioclase-phyric trachydacite porphyry,trachyandesite, volcanic breccia, and locally in quartzmonzonite, and are distributed above and cross-cutthe roof of the Searchlight pluton. District depositsproduced about 250,000 ounces of gold from 1902-1962 (Callahan, 1939). The primary metallic mineralsare native gold, chalcopyrite, specular hematite,galena, sphalerite, and pyrite. The primary alterationminerals around the deposits are illite, montmorillonite,kaolinite, quartz, hematite and locally adularia.The deep parts of the epithermal system(eastern side) are characterized by high base metalcontent and mineralogy consists of quartz, specularhematite, chalcopyrite, galena, sphalerite, pyrite, andnative gold. In contrast, the shallow part of theepithermal system (western side) is characterized bylow base metal content, and mineralogy consists ofquartz, native gold, electrum, and native silver.Fluid inclusion microthermometry wasperformed on quartz in mineralized samples fromdeep (Quartette Mine) and shallow parts (SearchlightParallel Mine) of the epithermal system. All observedand evaluated fluid inclusions are two-phase liquidand vapor inclusions, and all evaluated inclusionscomprise fluid inclusions assemblages. Primaryinclusions were recognized by their presence ingrowth zones and consistent phase ratios; secondaryinclusions lie along healed fracture planes. Fluidinclusions in the deeper veins containing specularhematite and base metal minerals homogenize at290 to 320 °C, with most inclusions homogenizingbetween 300 and 310 °C. Fluid inclusion salinitiesare low and range from 3.4 to 0.9 wt% NaClequivalent, with most inclusions exhibiting salinitiesbetween 1.7 and 1.2 wt% NaCl equivalent. In contrast,fluid inclusions in shallow veins located approximately400 meters higher in paleoelevation than deep veins,and which contain gold and silver with no specularhematite and nil to low base metal mineralshomogenize from 190 to 220 °C; salinities are verylow and range from 0.5 to 0 wt% NaCl equivalent.Fluid inclusion studies indicate that the deepand shallow veins containing different metals formedfrom two distinctly different fluids that may have beengenerated by discrete events, or which may haveevolved through fluid mixing with meteoric waters.REFERENCESBachl, C., Miller, C., Miller, J., Faulds, J. (2001) GSABull. 113, no.9: 1213-1228.Callaghan, E. (1939) USGS Bull. 906-D: 136-188.116

O50European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 118On deep subduction fluids: the fluid and solid multiphase inclusions ineclogite-facies mineralsScambelluri, Marco*, Pettke, Thomas** and Van Roermund, Herman L.M**** Dipartimento per lo Studio del Territorio e delle sue Risorse, Università di Genova, Italy** Institute of Geological Sciences, University of Bern, Switzerland*** Faculty of Earth Sciences, University of Utrecht, The NetherlandsMantle metasomatism and magmatism atconvergent margins are enhanced primarily by fluidphases released from the subducting plates andfluxing the overlying mantle. The role of fluids in thiscycle has been increasingly emphasized in the lastdecade, with considerable input from studies of high-(HP) and ultrahigh-pressure (UHP) eclogite-faciesrocks. These may preserve remnants of thesubduction fluids as primary inclusions in HP minerals,representing unique records of fluid processes at 50-200 km depth. Here we discuss field-based studieson slab dehydration and fluid-rock reaction at theslab-mantle interface.The serpentine breakdown is a majordehydration episode in slabs, releasing several wt%water. Chlorite harzburgites of the Betic Cordillera(Spain) record such an event, retaining the antigoritebreakdown fluid in primary multiphase inclusions(olivine, magnetite, chlorite, apatite, aqueous liquid).The inclusion trace element compositions measuredby LA-ICPMS are enriched in large ion lithophileelements (LILE: Rb, Ba, Cs, Sr), B and Li relative tothe high field strength elements (HFSE: Ti, Nb). Thisfluid shares relevant analogies with arc magmasignatures. Such fluids may interact with sedimentaryor granitic layers in the slab, producing either hydrouspartial melts, or silicate-rich supercritical liquids,viewed as the supreme transport agents carrying thefull range of elements expected in arc magmasources in the mantle. The fate of these slab fluids inthe mantle is yet unconstrained, due to a lack ofrepresentative samples. For this purpose, studies ofUHP orogenic garnet peridotites (which maycorrespond to mantle wedge materials sliced in thesubducting plates) enable an understanding of fluidperidotiteinteractions across the slab-mantleinterface.The UHP garnet orthopyroxenites from Maowu(Dabie-Shan, China), are former garnet harzburgitesaffected by the reactive flow of silica-rich agentssourced from felsic slab reservoirs. The reactionproduced orthopyroxene, garnet and a residualaqueous fluid trapped in primary solid multiphaseinclusions in garnet. The inclusions have negativecrystal shapes, contain a number of hydrous silicatephases with constant volume ratios. Their traceelement compositions are enriched in light rare earthelements (LREE) and LILE. This case-studyapproximates the interaction between sedimentderivedsupercritical liquids and/or melts with mantlewedge peridotites and demonstrates that the agentsreleased from slabs are highly reactive in the mantle,thus having limited mobility. Rather, their reactionwith ultramafic lithologies evolves a metasomaticaqueous fluid able to travel in the mantle wedge.Signs of fluid mobility in ultradeep mantle arerecorded by the UHP garnet pyroxenites of WesternNorway. These rocks are slices of mantle wedgeinfiltrated by COH silicate subduction fluids at 200 kmdepth, as attested by veins filled with phlogopite andmajoritic garnet, the latter hosting polyphaseinclusions filled by homogeneous aggregates ofpyroxene, phlogopite, carbonate, spinel and locallymicrodiamond. High-P minerals have LILE and LREEenriched signatures characteristic for crustalmetasomatism, and display equilibrium trace-elementdistribution. This implies that recycling of crustalcomponents via fluid phases in the mantle operatesdown to at least 200 km depths in subductionsettings. The integrated study of the trace elementcomposition of UHP mineral phases and of hostedpolyphase inclusions is a promising target for futureresearch, adding novel constraints to the fluidmediatedcrust-to-mantle element recycling.118

O51European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 120Fluid evolution of the igneous Varberg-Torpa charnockite-granitecomplex, SW SwedenVan den Kerkhof, Alfons M.*, Harlov, Daniel ** and Johannsson, Leif **** Geowissenschaftliches Zentrum der Georg-August-Universität Göttingen, Goldschmidtstr. 3, 37077Göttingen, Germany**GeoForschungsZentrum, Section 4.1 Experimental Geochemistry and Mineral Physics, Telegrafenberg,14473 Potsdam, Germany***Department of Geology, University of Lund, Sölvegatan 12, S-22362 Lund, SwedenThe 1.4 Ga Varberg-Torpa charnockite-granitecomplex is located in the vicinity of the town ofVarberg on the southwest coast of Sweden ca. 100km south of Göteborg. The Varberg charnockite(Opx-Cpx-Bt-Amph-Gt-Plag-Kfs-Qtz, with accessoryFAp, Zrn, Mt, Ilm, Py, Cp ±Po, ±Rt) is interpreted asa magmatic charnockite coupled with in situdehydration of the local regional amphibolite-faciesgranitic gneisses in the immediate surroundings ofthe intrusion (Quensel, 1950; Hubbard, 1989). TheTorpa granite is both continuous and synmagmaticwith the Varberg charnockite and, minus the pyroxenes,has a similar chemistry and mineral assemblage.It also contains several small charnockiteencla ves. P-T estimation using Gt-Opx Fe-Mg exchangethermometry and Gt-Opx-Plg-Qtz baro metryof both the igneous and metasomatically derivedcharnockite indicates temperatures of 650–700 °Cand pressures of 800 MPa during emplacement andcrystallization of the charnockite-granite body.The earliest recognized fluids consist of H 2O-CO 2mixtures (water volume fraction = 0.2-0.7) andare possibly of magmatic origin. They are preservedin the most pristine charnockite and characterized byhigh partial CO 2densities (up to 1.0 g/cm 3 for watervol. frac. = 0.7). Magmatic fluids in the Torpa granitecorrespond with aqueous-carbonic inclusions with anestimated bulk composition (mol%) ofH 2O(73)CO 2(25)NaCl(2); the salinity of the solutes ingranite is generally higher than for the charnockite(typically 14-20 wt% NaCl-eq.).The majority of fluids in the charnockite,however, are found as carbonic and aqueous fluidinclusions. These inclusions are mainly found inquartz, but also in plagioclase, garnet, and inpyroxene. The carbonic inclusions make up 40 - 90%of the total fluid inclusion inventory and consist ofalmost pure CO 2with only minor or no CH 4(and/orN 2). Charnockitic inliers located far within the TorpaGranite contain essentially the same fluids as theregular charnockites with relatively well-preservedearly inclusions. Aqueous inclusions with 0-8 wt%NaCl-eq. are found only in quartz and show evidencefor large-scale (re)trapping during exhumation.Incidental higher salinities with Ca-prevalence areassumed alteration fluids which formed duringalbitization.Compiled homogenization temperatures forthe carbonic inclusions show clear frequency maximaat ThCO 2(L) = ca. -11 °C, +3 °C, +15 °C and +25 °C,corresponding to densities of 0.99, 0.90, 0.82, and0.70 g/cm 3 , respectively. Early carbonic inclusionsare best preserved in garnet, plagioclase and apatite(in order of subsequent lower CO 2densities), whereasinclusions in pyroxene are badly preserved. However,the highest CO 2densities of 1.08-1.10 g/cm 3 arefound in quartz (Th -31 to -36 °C) and may originatefrom the granulite facies conditions. This observationconfirms the experimental results of Vityk and Bodnar(1998) that a small number of fluid inclusions inquartz mostly survive extreme fluid over- or underpressures.The Th-frequency maxima may correspondto fluid retrapping (decrepitation) during an isothermalretrograde PT path.REFERENCESHubbard F.H. (1989) Lithos 23: 101–113.Quensel P. (1950) Arkiv för Mineralogi och GeologiVol 1, nr 10: 227–332.Vityk M.O., Bodnar R.J. (1998) Contrib. Mineral.Petrol.132: 149-162.120

O52European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 122Infrared imaging of H 2O concentrations in nominally anhydrousminerals containing fluid inclusions, using synchrotron radiationFrezzotti, Maria Luce*, Tecce, Francesca**, Perucchi, Andrea***, Ferrando, Simona**** and Compagnoni,Roberto*****Dipartimento di Scienze della Terra, Università di Siena, Via Laterina 8, Siena, 53100 Italy.**CNR-IGAG, c/o Università Roma 1 La Sapienza, P.zzale A. Moro 5, Roma, 00195 Italy***CNR-INFM Coherentia, Sincrotrone Trieste, Strada Statale 14, Basovizza (Trieste), 34012 Italy**** Dipartimento di Scienze della Terra, Università di Torino, Via V. Caluso 35, Torino, 10125 ItalyInfrared synchrotron radiation has been appliedto recognize and calculate “H 2O” (that is, dissolvedhydrogen) in the nominally anhydrous minerals(NAM’s) olivine, orthopyroxene, clinopyroxene, andgarnet containing water-bearing fluid inclusions toexamine the budget of water during mantle processes(i.e. metasomatism, and deep subduction). Thebrightness of synchrotron generated radiation allowedus to collect maps of total water concentrations, andto distinguish among different water species, includingOH - groups, and molecular H 2O. Infrared maps havebeen collected from distinct rocks from two localities:i) spinel peridotites enclosed in alkali-basalts of theEthiopian plateau (Injibara), and ii) whiteschists ofthe Dora-Maira UHP metamorphic complex (Alps). IRanalyses were carried out at the new infrared beamlineSISSI (Source for Imaging and SpectroscopicStudies in the Infrared) operating at the synchrotronlaboratory ELETTRA in Trieste, Italy.In Injibara mantle peridotites, water con centrationsare lower in olivine than in orthopyroxeneand clinopyroxene. The distribution of water is heterogeneous:the concentrations of water species arehigh both in the inner parts of the crystals and closeto fluid inclusion trails, whereas they are generallyvery low far from these zones (Fig. 1). Likewise, ingarnet from the Dora Maira whiteschists, zoning inwater concentrations follows the distribution of multiphasesolid inclusions, indicating that some water islikely to have diffused from inclusions into the hostgarnet.Present study confirms the role of NAM’s asreservoirs of significant water in the Earth’s mantle,and further suggests that fluid inclusions may play amajor role in controlling the complex distribution ofconcentrations of water species within the singlecrystals.100 µmFig. 1. Up: Microscope image of olivine andorthopyroxene in peridotite. Down: Infrared image ofwater distribution in the same area, which shows thehighest water concentrations located near the fluidinclusion trails.122

O53European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 124Drastic changes in fluid nature and source during late diagenesis(celestite-quartz veins) of the eastern part of the Paris basin: evidencefrom Raman spectroscopy and isotope geochemistryPierron Olivier*, Cathelineau, Michel*, Boiron, Marie-Christine*, Fourcade Serge**, Richard Laurent **G2R, Nancy University, BP 239, 54506 Vandoeuvre-les-Nancy, France**Geosciences Rennes, UMR 6118, 35042 Rennes Cedex, FranceOxfordian clay-rich formations from the easternpart of the Paris Basin display in some strata(especially those close to spongolite layers) abundantmicrocavities or bioclasts, as well as some connectedmicrofractures almost completely filled with a specificmineral assemblage made of the following succession:amorphous silica, euhedral quartz, celestite, andeuhe dral calcite (Fig. 1). This assemblage is foundalso in septaria from other clay-rich Liassic formations(Toarcian, Domerian). Generally considered as theproduct of early diagenesis, these minerals can beconsidered in the present case as the witnesses of aspecific change in the nature of the flow regime at theinterface between low-permeability argilite and limestoneaquifers during later processes.Quartz0.5mmCelestiteSparite 1Cel.QuartzF. I.40 mFigure 1: Back-scattered electron image of thecelestite-quartz-calcite assemblage filling a bioclastin the Oxfordian shales from the Meuse-HauteMarne underground laboratory area, with indicationof the location of the fluid inclusions within the latestgrowth band of quartz, in which celestite inclusionsare also observed.Fluid inclusions in this mineral assemblage arescarce and of poor quality (small size, flat inclusions),which makes any microthermometry measurementsextremely difficult. The use of Raman spectroscopyfor chlorinity measurements (Dubessy et al., 2002)has been therefore essential for small-size inclusionsin which the ice melting temperature was unobtainable.The precipitation of the minerals appearsrelated to a change in the nature of the interstitialfluid, namely: i) a drastic change in chlorinity from2 mol/kg in quartz fluid inclusions down to muchlower values around 0.2 mol/kg in calcite fluidinclusions, ii) a different fluid origin, as the δ 18 O-values of the saline fluids hosted by quartz (δ 18 O ~32‰) are calculated at around 0‰ (35 °C), whilethose of diluted fluids in equilibrium with calcite (δ 18 O~ 21‰/SMOW) are estimated at around -5.5 to -3.5‰, a decrease that can be ascribed to a significantinput of meteoric water.The δ 13 C-values of late calcite are close tothose of the host limestones, indicating a local sourceof carbon. Similarly, the 87 Sr/ 86 Sr ratios of bothcelestite and late calcite (0.706950–0.707000) arewithin the range of those of the host limestones, inagreement with a local source of strontium. Therefore,the studied celestite-quartz-calcite assemblage isconsidered to have been crystallized during a stageoccurring after the maximal burial, accompanied bychanges in the nature of the interstitial fluids, withbrines being diluted or replaced by a significant componentof meteoric fluid. The latter fluid is thought tobe responsible for the main porosity reduction of theMesozoic limestones from the eastern part of theParis basin. Possible situations for a meteoric fluidinvasion include: i) limestone aquifers directly connectedto surface waters and brines in the overlyingformations, and/or ii) channelling of water fromdeeper zones in the basin (Trias), through the regionalfault system.REFERENCESDubessy, J., Lhomme T., Boiron, M.C., and Rull,F.(2002) Appl. Spectrom. 56: 99-106.124

O54European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 126Analysis of stable isotope properties of fluid inclusion waters:development of method and a case studyDublyansky Yuri* , **, Borsato Andrea***, Frisia Silvia***, Dallai, Luigi**** and Spötl Cristoph** Leopold-Franzens-Universität, Innrain 52, Innsbruck, 6020 Austria** Institute of Geology and Mineralogy, SB RAS, Koptiuga 3, Novosibirsk, 630090, Russia*** Museo Tridentino di Scienze Naturali, Via Calepina 14, Trento, 38100 Italy**** CNR-Ist. Geoscienze e Georisorse, Via Moruzzi 1, Pisa, 56124 ItalyAn analytical line for studying the isotopiccomposition of fluid inclusion waters was designed atthe MTSN (Trento, Italy) and assembled at the IGG-CNR (Pisa, Italy).The line, operating in continuous He flowmode, comprises a custom-made electromagneticcrushing cell, a gas interface with cryogenic trap, anda Thermo Finnigan TC/EA unit (glassy carbon pyrolysisreactor and a gas chromatographic column).The line was connected, via a ConFlo III open-splitinterface, to a Thermo Finnigan Delta Plus XP massspectrometer.To prevent adsorption of water, the linewas heated to 150 °C. Calibration by injecting referencewaters into the crushing cell showed the reproducibilityof δD measurements to be better than±5‰.In a test study, we analyzed specimens ofeuhedral calcite from solutional cavities in the TriassicDolomia Ladinica and Dolomia Principale (Mezzolombardo,Trentino, Italy). Calcite was deposited astwo consecutive phases characterized by evolvingcrystal morphology. The homogenization temperatures(T T h’s) for early scalenohedral calcite ranged between58 and 70 ºC, whereas late rhombohedral-prismaticcalcite contained only monophase aqueous inclusions.The isotope properties of the two calcite phases arerespectively: δ 18 O cat(–17 to –20‰ and –9 to –11‰V-PDB) and δ 13 C cat(2.0 to 2.7‰ and –6.0 to –7.5‰V-PDB). The contents of trace elements (P, Mn, Sr, Y,Ba, Zn and Pb) are also distinct in these two calcitephases (ICP-MS analysis).The content of water trapped in inclusions wasfound to be low, ranging between 0.05 and 0.25 μl/g-CaCO 3. The δD values of waters changed from –68to –76‰ in early to –83 to –86‰ V-SMOW in latecalcite. Coupled with δ 18 O watvalues (calculated fromδ 18 O catand T h’s using the fractionation equation ofKim and O’Neil, 1997), the data indicate twoisotopically distinct sources of mineral-formingsolutions. Interestingly, on the δ 18 O-δD graph theearly, higher-temperature waters plot close to theMeteoric Water Line (within ±1‰ δ 18 O-band), whereaslater, relatively low-temperature waters exhibitsubstantial positive δ 18 O-shift (Fig. 1).Fig. 1. Evolution of isotope properties of fluidinclusion waters in calcites from Mezzolombardo,Italy. Local Meteoric Water Line is shown along withthe δ 18 O ± 1 ‰-band.Studies of the stable isotope properties of fluidinclusion waters show great promise for paleo-hydrogeologicalstudies as they can provide inde pendentconstraints on the paleo-hydrogeological models,particularly on sources of paleo-waters.The new version of the line built at InnsbruckUniversity includes a cryo-focusing unit, which willallow determination of both δD and δ 18 O of inclusionwater from a single extraction.REFERENCESKim S.-T and O’Neil J.R. (1997) Geochim.Cosmochim. Acta 61: 3461-3475.126

O55European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 128The fluids of the giant selenite crystals of Naica (Chiuhahua, Mexico)Garofalo P.S.*, Günther D.**, Forti P.*, Lauritzen S.-E.***, and Constantin S.****Department of Earth Sciences, Università di Bologna, Piazza di Porta S. Donato, 1 I-40127 Bologna, Italy**Laboratory of Inorganic Chemistry, ETH Hönggerberg, HCI, CH-8093 Zürich, Switzerland***Department of Earth Sciences, University of Bergen, Allegaten 41, N-5007 Bergen, NorwayThe caves located within the Pb-Zn mine ofNaica (Chiuhahua, Mexico) in a depth range between–130 m and –290 m below entrance level constitutea unique karstic environment. The distinctive characteristicsof these caves (i.e., Las Espadas, LosCristales, Ojio de la Reina, and Las Velas) are thelack of direct interconnection with the surface, anactual groundwater temperature of ca. 53 °C, and thepresence of exceptionally big selenite crystals (>10 min length). The conditions that controlled the growthof single gypsum crystals in such an environmenthave been the object of recent work (García-Ruiz etal., 2007). Here, we report the preliminary results ofan ongoing multidisciplinary study (“Naica Project”,lead by Speleoresearch & Films and La VentaExploring Team) that considers the vertical extent ofthe cave system, and that is aimed at determining thegenesis of these crystals. U/Th dating of the core ofa crystal from one deep cave (Los Cristales) hasdetermined a corrected age of 34.5±0.82 ka.Fluid inclusions are abundant at Naica, occurin all the studied crystals, and are commonly big(>200 µm). In the deepest, clear and twinned crystals,they are typically found along crystallographic planes.In the shallowest Las Espadas cave (Fig. 1), inclusionsoccur both at the transparent core (Area 1) and alongthe dark rims of zoned crystals, where Pb-Mn oxidesand hematite/goethite inclusions occur as well (Areas2-3). In all occurrences, the trapped fluid is mostlyone-phase (L) at T lab, and only occasionally twophase(L-V). Solid phases (i.e., gypsum and oxides)are found as well, but do not show constant phaseratios with the L and V phases. Microthermometricdata have been collected for seven representativefluid inclusion assemblages (n tot=344) from severalcaves, and show the presence of two aqueous fluidswith distinct salinity: one in the range of 5-6 wt%NaCl equiv.(Area 1), and the other between 7 and 8wt% NaCl equiv.(Area 2). The higher-salinity fluid andthe darker zones are found only in the crystals fromLas Espadas. Eutectic melting has been determinedin the lower-salinity assemblages to be between –30and –27 °C.In the deepest sections of the cave system(Ojio de la Reina), T hoccurs in the 55-56 °C rangewithin single assemblages, which is undistinguishablefrom the data obtained at the core of the Las Espadascrystals (Area 1), but slightly higher than the mode ofthe T hdistribution in the outer dark zones (Area 2).Fig. 1. Fluid typologies within the gypsum crystalsand microthermometric dataIn contrast with the previous work carried outat Naica, our results show that (1) the giant crystalsgrew from fluids that were more saline at shallowdepths; and (2) crystal growth was faster thanpresently estimated. We speculate that the climaticchanges occurring during gypsum growth (< 1 Ma)controlled the composition of the source fluid andhence growth kinetics. Future isotopic dating andinclusion microanalysis will show the composition ofthese fluids as a function of cave location andcrystallization time.REFERENCESGarcía-Ruiz J. M., Villasuso R., Ayora C., Canals A.,Otálora F. (2007) Geology. 35: 327-330128

O56European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 130Temperatures in sulfide oxidation zones: microthermometry ofmonophase aqueous fluid inclusions and stable isotope systematicsGilg, H. Albert*, Krüger, Yves**, Stoller, Patrick***, Frenz, Martin***, Boni, Maria**** and Ziemann, M.******Lehrstuhl für Ingenieurgeologie, TU München, Arcisstr. 21, D-80333 München, Germany**LFA - Labor für Fluideinschluss-Analytik, Cäcilienrain 3, CH-3007 Bern, Switzerland***Institut für Angewandte Physik, Universität Bern, CH-3012 Bern, Switzerland****Dipartimento di Scienze della Terra, Università di Napoli “Federico II”, I-80134 Napoli, Italy***** Inst. für Geowiss., Univ. Potsdam, 14476 Potsdam, GermanyHere we present the first geological applicationsof a new technique that uses femto second laserpulses to selectively induce bubble nucleation inindividual metastable monophase all-liquid inclusionswithout causing any irreversible volume expansion(Krüger et al. European Journal of Mineralogy, inpress). The beam of an amplified Ti:sapphire laser(800 nm) is coupled to a microscope that is equippedwith a heating-freezing stage and focussed onto thefluid inclusions using a conventional 100x/0.80 longworking-distancemicroscope objective. The inclusionsare held at +4 °C and single pulses of appropriateintensity are sufficient to reliably induce bubblenucleation in the inclusions. The method yields areproducibility of homogeni zation tempera tures thatis better than 0.2 °C.We applied this new technique to studytemperatures in oxidation zones of Pb-Zn sulfidedeposits and compare the microthermometric resultsto those derived from stable isotope data. It is stillunclear whether minerals in supergene oxidationzones form at normal ambient temperatures or atunusually high temperatures of more than 30 °C dueto exothermic sulfide oxidation reactions orsuperimposed hot-spring systems. We focus here onthe enigmatic willemite-bearing non sulfide Zn depositsof Belgium and Portu gal. Willemite deposits aregenerally considered to form in specific hydro thermalor metamorphic environ ments.The nonsulfide Zn deposits of Eastern Belgiumformed by replacement of a Post-Variscan MVT-stylesulfide mineralization hosted in Visean lime stones intwo successive stages: an early willemite stage anda later hemimorphite-smith sonite-cerussite stage.About 80% of the fluid inclusions in hemimorphiteare all-liquid and only 20% of the total populationare liquid-vapor inclusions with homogenizationtempera tures ranging from 80 to more than 190 °C.The two-phase inclusions do not form consistent fluidinclusion assemblages (FIAs), but are likely to resultfrom stretching or leakage due to sample preparation.The monophase all-liquid inclusions can be groupedin two types of FIAs. The para genetically earlier setof primary FIAs (Type A) displays homogenizationtempera tures ranging from 20 to 27 °C and icemelting temperatures of 0.0 ± 0.2 °C, while a later setof FIAs (Type B) has homo genization temperaturesof 6 to 30 °C with two modes around 10 °C and 25°C, and lower ice mel ting temperatures of –0.2 to –1.6 °C.Stable oxygen isotope data of smith sonite andcerussite that formed together with hemimorphiteyield tempera tures of 6 to 22 °C, in equilibrium withlocal Cretaceous paleometeoric water compositions.The Preguiça deposit in Southern Portugal ischaracterized by a 90 m-thick hematite-rich gossanwith abundant willemite, calcite, dolomite, cerussite,descloizite, and very minor smithsonite that formedby oxidation of a metamorphosed sulfide orebody inCambrian dolomites. Willemite at Preguiça containsno visible fluid inclusions. Sparry dolomite, however,has abundant primary pure aqueous liquid inclusionswith consistent homogenization tempe ra tures of 22to 27 °C.This preliminary study clearly shows that thenew method of laser induced bubble nucleation inmetastable aqueous all-liquid inclusions yields veryuseful thermometric data from minerals forming closeto the earth’s surface and may also be used inpaleoclimatology. We found no evidence forabnormally high temperatures (>30 °C) in any of theinvestigated nonsulfide Zn-Pb deposits in Europe.This PDF version of the abstract has been corrected following printing of the conferencevolume, acccording to errata submitted by the authors.130

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 132Abstracts ofPoster Presentations132

P1European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 134Interpretation of fluid inclusions that homogenize by halitedisappearanceBecker, Stephen P.*, Bodnar, Robert J.**Department of Geosciences, Virginia Tech, Blacksburg, VA 24061, USAHigh salinity (>30 wt. % equivalent NaCl) fluidinclusions are common in many geologic environments,including magmatic hydrothermal systems associatedwith porphyry copper mineralization. At roomtemperature these inclusions contain liquid, vaporand halite ± other solid phases. During heating fromroom temperature, halite-bearing inclusions maydisplay one of three modes of homogenization (Fig.1): A) halite dissolution (Tm halite) first followed byshrinkage and disappearance of the vapor bubble(Th L-V), B) simultaneous disappearance of the vaporbubble and halite crystal, and C) vapor bubblehomogenization followed by halite dissolution. Datafor the H 2O-NaCl system are available to allowinvestigators to interpret microthermometric data forinclusions that homogenize by modes “A” and “B”,but PVTX data necessary to interpret data from type“C” inclusions are scarce, having only been determinedfor 40 wt. % NaCl. Using the synthetic fluid inclusiontechnique, we have determined the relationshipbetween Th , Tm, and pressure along the haliteL-V haliteliquidus for inclusions that homogenize by halitedisappearance. The experimental data cover therange Th L-V≈ 150-500° C and Tm halite≈ 275-550° C.Experimental data obtained in this study havebeen applied to previously published data for naturalinclusions from a range of geologic environments.During this process, it became apparent that mostpublished data could not be re-evaluated in terms ofthe new PTX data for H 2O-NaCl because the fluidinclusion data were not collected and reported withinthe context of Fluid Inclusion Assemblages (FIA).Most of the published data for halite-bearing inclusionsthat homogenize by halite disappearance do notreport data for individual FIAs exhibiting consistentmicrothermometric behavior. Instead, most studiesreport data as ranges of homogenization temperatures,or plotted on ambiguous histograms or scatter plotsof Th L-Vvs. Tm halite, or scatter plots of Tm halitevs.salinity. Furthermore, comparison of the range ofscatter of many of these published data suggeststrapping pressures in excess of 300 MPa, aninterpretation inconsistent with geological observationsthat indicate a shallow crustal origin for porphyrycopper mineralization. This discrepancy may beattributed to violations of “Roedder’s Rules” in manycases, associated with heterogeneous trapping,necking down, stretching, and water loss.Fig. 1: Homogenization sequence of inclusions thathomogenize by modes A, B, and C.134

P2European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 136Precision of thermal history reconstruction with fluid inclusionsFall, András*, Bodnar, Robert J.* and Reynolds, T. James***Department of Geosciences, Virginia Tech, 4044 Derring Hall, Blacksburg, VA 24061, USA**FLUID INC., 1401 Wewatta St., #PH3 Denver, CO 80202, USAFluid inclusions are time capsules that offerinformation on the conditions of mineral precipitation.Different generations of inclusions in mineralsrepresent specific fluid events and temperatureconditions and are often used to determine thethermal history of geologic environments (Roedder,1984). However, the precision to which the thermalhistory can be constrained using fluid inclusions ispoorly understood.Fluid inclusions provide useful micro thermometricdata only if fluid inclusion assemblages arestudied (FIA) (Goldstein and Reynolds, 1994). An FIAdefines a group of fluid inclusions that were trappedat the same time, implying that all the inclusionswithin an FIA were trapped at the same temperatureand pressure, and all trapped a fluid of the samecomposition (Bodnar, 2003). Assuming that theinclusions represent the original trapping conditionsand there has been no post-entrapment reequilibration,all inclusions in an FIA should have the same homogenizationtemperature (T h). However, fluid inclusionsassumed to be trapped at the same time frequentlyshow a variation in T h. If fluid inclusions within an FIAwere trapped at the same temperature and pressurethe best precision achievable is on the order of ±0.5 °C to ± 2 °C. This variation, as has beendocumented with both synthetic and natural fluidinclusions, is due to the fluid inclusion size factor thatarises from the surface tension and absolute size ofthe vapor bubble in the inclusion. During heating theinclusion reaches that absolute minimum bubble sizewhere the vapor bubble can no longer maintain theinternal pressure in the bubble, and homogenizationoccurs. Smaller inclusions reach the minimum bubblesize earlier and will homogenize at a lower temperaturethan larger inclusions.The precision with which the T hof an FIA canbe determined will vary depending on the geologicenvironment were the FIA is formed. These factorsmay include, besides fluid inclusion size, naturaltemperature and pressure fluctuations during andafter formation of an FIA, physical properties of thehost mineral, as well as sample collection andpreparation, and thermal gradients during T hmeasurements.Fluid inclusions in fluorites (MVT deposit,Cave-in-Rock fluorospar district, Southern Illinois)show average T hranging from 142.1 °C to 156.1 °Cwith standard deviations ranging from 0.26 forsecondary FIAs to 3.16 for primary FIAs trappedalong growth zones of fluorite. These variations are aresult of inclusion size for the secondary FIAs, andinclusion size and natural temperature fluctuation forthe primary inclusions. Similar variations can beexpected for other MVT’s, although some influencefrom host mineral physical properties has to be takeninto account.Preliminary data on metamorphic lode-golddeposits show average T hranging from 86.5 °C to308.6 °C and standard deviations from 1.1 to 28.8.For a metamorphic environment, where large temperatureand pressure fluctuations are expected, postentrapmentreequilibration of fluid inclusions significantlyaffects T hvariations.The precision with which T hvariations can bedetermined will be examined in other geologic environmentsthat include deeper magmatic hydrothermalsystems, porphyry copper deposits, epithermal deposits,and diagenetic systems.REFERENCESBodnar, R.J. (2003) MAC Short Course v. 32: 1-8.Goldstein, R.H and Reynolds, T.J. (1994) SEPMShort Course v. 31: 199 p.Roedder, E. (1984) Rev. in Miner. v. 12: 251-290.136

P3European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 138GEOPROFI: An evolutionary software to calculate inclusion isochoresfrom equations of statePernot, Nelly* and Dubois, Michel*** CNRS - Délégation Languedoc Roussillon, 34293 Montpellier CEDEX 5, France** UMR 8110 “PBDS”, Université de Lille 1, UFR Sciences de la Terre, 59655 Villeneuve d’Ascq, FranceGEOPROFI (“GEOthermobarometry based onPROperties of Fluid Inclusions”) is a new softwareable to calculate temperature (T) and pressure (P)properties (isochores) of fluid inclusions usingavailable Equations Of State (EOS). The followingconstraints have guided the authors for the conceptionof the GEOPROFI software:• To provide a working environment including anergonomic graphic interface (fields and buttons)• To provide a unique tool for the treatment of alarge variety of fluid compositions• To include the treatment of the major componentsand mixtures of natural fluid systems. GEOPROFIcurrently includes 11 constituents: water (H 2O),various salts (NaCl, KCl, MgCl 2and CaCl 2) andgases (CO 2, CH 4, N 2, H 2S, O 2and H 2)• To include the treatment of the data by a largevariety of published EOS. All EOS applicable tothe system (presently 20) are treated simultaneouslyand the choice is automatically made by thesoftware as a function of the nature of constituentsand the field of validity of the model• To offer to the user the possibility to include newEOS. The database was designed to include anynew EOS, not initially present in the database orto be developed in the future.• To display a graphic interface with therepresentation of all calculated isochores in a T–Pspace.The software is written in the object-orientedJAVA language. This choice will permit GEOPROFIto run both in WINDOWS and Mac OS environmentsand is particularly adapted for graphical devices.An EOS is a mathematical function of P, T, bulkmolar volume ( V) and composition (generallyexpressed in terms of mole fractions x i). In fluidinclusions, V and x i iare constant and are requiredas input data for EOS calculation. The only exceptionis the case of the EOS of Zhang and Frantz (1987),where P-T properties are calculated fromhomogenisation temperature (Th) and salt molality.The temperature range in which the calculationwill be made is introduced in a new window, as wellas the minimum and maximum temperature of thecalculation domain, and the temperature step.When all input variables are entered, eachEOS of the database is evaluated. All EOS are codedin a separate database and are interpreted by asyntactical interpreter. The database includespresently about 20 EOS. Each EOS is codedaccording to an identical general structure: name ofthe authors and reference, T range of applicability, Prange of applicability, general mathematical formulasof the equation in a text format, which includes one ortwo levels of variable dependency.The fluid composition and the P-T range ofapplicability are evaluated for each EOS. A givenEOS is accepted if all the constituents whose molefractions are not zero belong to the constituent list ofthe EOS. The temperature range is selected bycomparing the T range specified by the user and theT range of validity of the EOS.A T-P diagram is then provided in a newwindow. Each applicable EOS yields a particularcurve with a different colour. Possibilities of selectingpoint co-ordinates along isochores, as well as T-Ppairs in forms of a table, is offered. T-P pairs can bestored in text files for exportation to other software.REFERENCESPernot N. (2002) Internal report, University of Lille.47 p.Zhang Y.-G. & Frantz A. (1987) Chem. Geol. 64,335-350.138

P4European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 140SoWatFlinc – a program for the computation of accurate fluidproperties in the system H 2O-NaClDriesner, T.*, Heinrich, C.A.**Institute of Isotope Geochemistry and Mineral Resources, ETH Zurich, Clausiusstrasse 25, 8092 Zurich,SwitzerlandSoWatFlinc is an interactive computer programbased on our recent development of an accurateempirical model for the phase relations (Driesner &Heinrich, 2007), volumetric properties, enthalpiesand heat capacities (Driesner, 2007) for phases inthe system H 2O-NaCl.The program allows computations for typicalfluid inclusion research purposes, i.e., salinities fromfreezing point depressions or final dissolution ofhalite, the subsequent determination of density fromthe homogenization temperature, and the computationof isochores for the given inclusion to 5000 bar.In addition, tables for the T-P-X coordinates ofphase boundaries (Fig. 1) can be generated(isothermal and isobaric sections through the V+L,V+H, L+H boundaries, T-P-X coordinates for curveson the V+L+H surface and for the critical curve, etc.)for graphical representation in standard graphicsprograms.Finally, fluid phase state and properties(density/molar volume, specific enthalpy, mass andvolume fractions of phases) and their respectivederivatives with respect to T, P, and X can be queriedfor a given T-P-X coordinate.Fig. 1: 3D plot of phase relations in the system H 2O-NaCl, generated from curves that were computedwith SoWatFlinc.REFERENCESDriesner T., Heinrich C.A.. (2007) Geochim.Cosmochim Acta. (in press)Driesner T. (2007) Geochim. Cosmochim Acta. (inpress)140

P5European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 142Synthetic fluid inclusions in rutile: a new technique to study mantlefluidsBali, Eniko*, Audétat, Andreas** Bayerisches Geoinstitut, Universität Bayreuth, Universitätstrasse, 30, Bayreuth, 95447 GermanyExperimental studies concerning the majorand trace element composition of hydrous fluidsmigrating in the mantle or released from a subductedoceanic crust are technically challenging. Currentlyused methods include the weight-loss technique(e.g., Newton and Manning, 2002) and the diamondtrap technique (e.g., Stalder et al. 2001; Kessel et al.2005), which both have a number of advantages anddisadvantages.Here we follow a new approach by trappingfluids at mantle conditions in rutile, and analyze theirmajor and trace element content by LA-ICP-MS.Rutile is a perfect mineral for this purpose becauseits solubility in aqueous fluid is relatively low (e.g.:Audétat and Keppler, 2005), but still high enough toallow crack-healing, and because it does not containmost of the elements of interest (except for HFSE).Major advantages of this method include: (i) it isapplicable to a large range of P/T-conditions, (ii)there are no limitations regarding the complexity ofstarting materials that can be used, and (iii) identicalbatches of the same fluid can be sampled numeroustimes.The method is currently being tested on thesystem quartz-H 2O and olivine-enstatite-H 2O, forwhich reliable data are available from weight-lossexperiments (Manning, 1994; Newton and Manning,2002).Rutile is loaded into Pt/Rh capsules, togetherwith fine grained minerals (e.g., enstatite, olivine,quartz) and 15-25 μl aqueous solution containing1000 ppm of Cs and Rb, the latter serving as internalstandards for the LA-ICP-MS analyses. Experimentsare carried out in 200 t piston cylinder apparatus,using pure salt assemblies and stepped graphiteheaters. Run conditions are approached along a fluidisochoric path, and then held for 4 hours to threedays.In order to produce fluid inclusions that containequilibrium fluid and are large enough for LA-ICPMSanalyses we loaded rutile in different ways. The firstattempt was to load rutile single crystals with a roughsurface and trap the inclusions in superficialirregularities by overgrowing newly formed rutile on it.This method yielded high number of elongated,negative crystal shaped inclusions after 60 hours ofexperimental duration but the size of the inclusions isusually below 10 μm, which is not appropriate for LA-ICPMS analyses. Second, we loaded cubes ofsintered, cracked rutile into the capsules. Fluidinclusions formed after 4 hours in SiO 2-H 2O system,they are 20-40 µm in size, which is appropriate forLA-ICP-MS analyses. However, inclusion compositionscover a wide range from low SiO 2-concentrations tothe equilibrium composition. This suggests that thehealing of submicrometer wide cracks in rutile is veryquick as soon as the fluid contains significant amountsof dissolved solids. These results suggest that it isnecessary to postpone crack-healing and form theinclusions in a controlled way. For this purpose ~30-40 μm large, in diameters and ~100-120 μm deepholes were drilled in the loaded rutile single crystals.This allows to control the inclusion size and on theother hand a 30-40 μm wide “crack” needs more timeto heal providing a possibility for the fluid to equilibratebefore entrapment.REFERENCESAudétat, A., Keppler, H. (2005) Earth Planet.Sci.Let.232, 393-402.Kessel, R. Schmidt, M.W., Ulmer, P., Pettke, T.(2005) Nature, 437, 724-727.Manning, C.E. (1994) Geochim Cosmochim Acta,58, 4831-4839.Newton, R.C., Manning C.E. (2002) GeochimCosmochim Acta, 23, 4165-4176.Stalder, R., Ulmer, P., Thompson, A., Gunther, D.(2001) Contrib.Mineral.Petrol. 140, 607-618.142

P6European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 144An Experimental Investigation of PGE Solubilities in Basalt – Vapour –Brine – Oxide – Sulfide AssemblagesBell, Aaron S. and Simon, Adam C.Department of Geoscience, University of Nevada Las Vegas, Las Vegas, NV 89154-4010, U.S.A.Two models for the formation of layered maficintrusion-hosted platinum group element (PGE)deposits have been proposed: the sulfide settlingmodel (Campbell et al., 1984) and the aqueous fluidorthomagmatic model (Boudreau et al., 1986). Thesulfide downers model proposes that sulfide crystalsor immiscible sulfide melts scavenge PGEs and thengravitationally settle to the bottom of the melt column.This model has been criticized for not addressing theubiquitous stratigraphic offsets of PGEs in mostdeposits (Fig. 1). The aqueous fluid uppers model isbased on apatite Cl/F ratios in numerous PGE-richlayered mafic intrusions (LMIs) which are inferred tosuggest that the melts exsolved Cl-rich aqueousfluid(s) during crystallization. These aqueous fluidswould scavenge metals from the melt and thenascend upwards through the crystal mush wheredeposition occurs owing to changes in the intrinsicf O2, f S2, f H2S, fHCl , P and T of the melt-fluidsystem. Currently no thermodynamic data exist thatallow for the critical evaluation of the plausibility ofthe proposed aqueous fluid based mechanism forPGE deposit formation.In this study, we are examining experimentallythe capacity of exsolved magmatic volatile phases toscavenge Pt, Pd, Cu, and Au from a basalt melt.Experiments are being performed at 1150 ºC and 200MPa in sulfur-free and sulfur-bearing assemblages.The effects of f O2and f S2are being explored byvarying f O2from magnetite-hematite to quartz-fayalite-magnetiteand buffering at f S2 pyrrhotite-Iss andIss-bornite. Run temperatures will be steppeddown systematically in 100 ºC intervals to elu ci dateparti tioning in a melt – supercritical aqueous fluidassem blage and at € lower T a melt – vapor – brineassem blage; hence, the relative scavenging capacityof each aqueous fluid phase will be constrained.Experi ments will be carried out in the following assemblages:1) dolerite melt + magnetite + aqueous fluid(10 wt.% NaCl eq with molar Na:K:H set to unity); 2)dolerite melt + magnetite + Iss + pyrrhotite + aqueousfluid; 3) dolerite melt + magnetite + Iss + bornite +aqueous fluid; and dolerite melt + magnetite + Iss +pyrrhotite + aqueous fluid (HCl free); 5) dolerite +magnetite + Iss + bornite + aqueous fluid. Thesephase assemblages will allow us to constrainthermodynamically the effects of temperature, f O 2 ,f S2, f H 2 S and f HCl on the partitioning behavior of Pt,Pd, Cu and Au at conditions appropriate for theformation of LMI-hosted PGE deposits. Aqueousfluids will trapped at run conditions as synthetic fluidinclusions in either quenched experimental glassesor in pre-fractured chips of quartz or orthopyroxene.LA-ICPMS analysis of the synthetic fluid inclusionswill evaluate the metal abundances in the equilibratedaqueous phase.REFERENCESBoudreau AE, Mathez EA, McCallum IS. (1986),Journal of Petrology, 27, 967-968.Campbell IH, Naldrett AJ, Barnes SJ. (1983),Journal of Petrology 24, 133-165.144

P7European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 146A bi-axial loading testers equipped heating microscope stage:Investigation on stress controlled decrepitation crackSekine, K. and Hayashi, K.Institute of Fluid Science, Tohoku University, 2-1-1, Katahira, Sendai, 980-8577, JapanHeating fluid inclusions above its initialmicrothermometric homogenization temperaturevalue is generally referred to as overheating.Overheating treatment of a fluid inclusion finallyresults in formation of fractures from the inclusionwall and explosive advection of its fluid in responseto high internal pressure in the inclusion. Thisdecrepitation behavior of inclusions has been utilizedfor releasing trapped fluids from host minerals.On the other, the decrepitation has beenwidely studied in relation to preservation characteristicof inclusions as a record of the fluid environment. Forexample, overheating at one atmosphere confiningpressure condition leads to stretching and/ordecrepitation and the deformation behavior dependson physical properties of inclusion host minerals (e.g.Ulrich and Bodnar, 1988). In addition, re-equilibrationlaboratory experiments of synthetic fluid inclusionsrevealed formation of dislocations at immediatevicinity of inclusions walls, which serve as potentialconduits for preferred leakage of water (e.g. Bakkerand Jansen, 1994).It is frequently assumed that microcracksformed by decrepitation (referred to as decrepitationcracks hereafter) is likely to propagate along inherentmechanically weak planes such as healed crackplanes; however, the brittle failure in the decrepitationstill remains unclear. Considering similarity ingeometric appearance with hydraulic stimulationwhich is often carried out in boreholes, the initiationand propagation behavior of the decrepitation cracksare expected to be controlled by stress state aroundthe inclusion. Supposing the inclusion in compressivestress field, the decrepitation cracks will extend in thedirection of compressive maximum principal stress.Conversely, the decrepitation cracks propagatingfrom round to sub-round shaped fluid inclusionsassociated with no irregular stress concentrationhave possibilities to give insights into micro-scaleregional stress around inclusions. For testing theabove mentioned idea, we have built a heatingmicroscope stage equipped with bi-axial loadingtesters (Fig. 1).Our bi-axial loading heating microscope stagewas designed to use doubly polished 5 x 5 x 0.2 mmthin section. Two spring load testers were builttogether with a heating cell, which allows the sectionto be forced up to 2 kgf and heated up to 600° Ctemperature condition.Decrepitation experiments are planned toexamine relationship between given stress statesand decrepitation behaviour in terms of thedecrepitation crack orientation and the internal fluidpressure. Multipurpose use of the stage is anticipatedas the stage provides microscopic information onfailure under elevated temperature conditions.Fig. 1. Photograph of the bi-axial loading heatingmicroscope systemREFERENCESUlrich, M. R., Bodnar, R. J. (1988) Econ. Geol. 83:1037-1046.Bakker, R. J., Jansen, J. B. (1994) Contrib. Mineral.Petrol. 116: 7-20.146

P8European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 148Experimental constraints on element mobility from subductedsediments using high-P synthetic fluid/melt inclusionsSpandler, Carl*, Mavrogenes, John** and Hermann, Jörg***Institute of Geological Sciences, University of Bern, Bern, CH-3012, Switzerland**Research School of Earth Sciences, Australian National University, Canberra, 0200, AustraliaVolatile and element recycling through subductionzones is fundamental to arc magma-genesis,continental crust formation and the geochemicalevolution of the mantle. Nevertheless, the nature andcomposition of mobile phases that are liberated fromsubducting slabs are poorly known. We haveperformed a series of hydrothermal piston-cylinderexperiments to determine the composition of representativefluids and fluid/melt/rock interaction insubduction zones (Spandler et al., 2007). Experimentswere conducted under H 2O saturated conditions at2.2 GPa over a temperature range from 600-750 ºC.The experiments contained synthetic, trace-elementdopedpelitic starting material and fractured quartzchips to trap and preserve synthetic fluid/meltinclusions (Fig. 1). Pelite residues from the subsolidusexperiments (600 ºC to 650 ºC) consist of an eclogitefaciesmineral assemblage including quartz, phengite,epidote, rutile, garnet, amphibole, apatite, and zircon.Coexisting hydrous fluids are expected to becompletely buffered for trace elements by this mineralassemblage. At 2.2 GPa the wet solidus for the peliticstarting material is located at 675 ºC (±10 ºC) andhydrous fluid and melt coexist as immiscible phasesat least up to 750 ºC (Fig. 1b). Residue phases in thesuper-solidus experiments (700-750 ºC) are garnet,rutile, and zircon, which suggest that HREE andHFSE are retained in slab residues even during veryhigh degrees of H 2O saturated melting.Analysis and quantification of trapped fluidinclusions from the experiments by LA-ICP-MSindicate that subsolidus hydrous fluids released fromsubducted sediments have relatively high LILEcontents compared to REE and HFSE, but overallare remarkably dilute. Total solute contents areapproximately 5 wt%, of which >75% is SiO 2andaround 15% is Na 2O+Al 2O 3. The experimental resultsare used to show that subducting sedimentary rocksdo not undergo significant element loss duringmetamorphic dehydration up to eclogite facies.Furthermore, we suggest that subsolidus fluids aretoo dilute to significantly contribute to arc magmasdirectly. Rather, sediment-derived hydrous melts arelikely to be the most important agent for transferringslab component to arc magmas; a condition thatrequires slab surface temperature to be 700 ºC orhigher at sub-arc depths.Fig 1. Synthetic fluid and fluid+melt inclusionstrapped in quartz during experiments. (a) Highdensity fluid inclusion from experiment conducted at2.2 GPa and 650 ºC (i.e., at subsolidus conditions).Note the cluster of daughter minerals. (b) Largeinclusion consisting of mixed fluid + melt with a trailof smaller fluid + melt inclusions from an experimentat 2.2 GPa and 700 ºC (i.e., at supersolidusconditions).REFERENCESSpandler C., Mavrogenes J. & Hermann J. (2007)Chem. Geol. 239: 228-249.148

P9European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 150A new look at old data: microthermometric data of a fluorite veinCanals, Àngels*, Piqué, Àngels* and Grandia, Fidel***Departament de Cristal.lografia, Mineralogia i Dipòsits Minerals, Facultat de Geologia, Universitat deBarcelona, C. Martí i Franquès s/n, 08028 Barcelona, Spain.**Enviros Spain S.L., Pg. de Rubí 29-31, 08197 Valldoreix, Barcelona, Spain.Bimodal distribution of microthermometric datafrom a fluid inclusion assemblage has beentraditionally interpreted as trapping of two distinct,non-coeval fluids. Fluid inclusion data from the RigròsF-(Ba) vein were interpreted in that way by Canals(1989). This vein is hosted by a Late-Hercyniangranodiorite in the Catalan Coastal Ranges, and itformed during the Late Jurassic – Early Cretaceousrifting episode in the E Iberian basin (Sm-Nd fluoritedating = 137 ± 25 Ma; Piqué et al., 2007).Microthermometric data was interpreted by Canals(1989) as the succession of two fluids: an early brinewith Th ~110 ºC and salinities ~22 eq. wt. % NaCl,and a later one, mainly present on the center of thevein, with higher Th (from 160 to 230 ºC) and lowersalinity (~17 eq. wt. % NaCl). She found odd theabsence of the late fluid as secondary fluid inclusionsin earlier fluorites.A new petrographic study by means ofcathodoluminiscence (CL) microscopy has revealedthe existence of two distinct stages of fluoriteprecipitation (Fig. 1). Although the second generationof fluorite can be accompanied by little amounts ofquartz and/or carbonates, the distinction of fluoritegenerations is not possible under the regularmicroscope. Taking into account this parageneticsequence, new microthermometric data have beenobtained (Fig. 1).Due to the characteristic morphologies offluorite II inclusions, angular and elongate, a newlook at the old drawings allowed us to realize thatsome of the inclusions measured twenty years agobelong to this generation. Moreover, the highest Thmeasured corresponds, in many cases, to inclusionsthat were first frozen prior to measuring Th. Therefore,plastic deformation, due to ice crystals, could haveoccurred so all these data have been now finallyrejected.The microthermometric data from fluorite II,which shows a wide range in salinities (22.5 to 0 eq.wt. % NaCl) at μm scale and fairly constant Th (~90ºC), can be interpreted as dilution of already existinginclusions in the former fluorite I, when a fresh fluidcaused the recrystallization of fluorite I to fluorite II.The salinity of new inclusions would be a function ofthe proportion of the fluids involved, which in turnwould be constrained by the presence or absence,size and density of the former inclusions in fluorite I.Fig. 1. Scheme and photomicrography of fluorite Iand II in CL and microthemometric data.REFERENCESCanals À. (1989) Bol Soc Esp Mineral 12: 283-293Piqué À., Canals A., Grandia F., Fuenlabrada J.M.,Banks D.A. (2007) SGA Dublín.150

P10European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 152Oil-bearing fluid inclusions associated with the Palaeoproterozoic Oklonatural fission reactors, GabonDutkiewicz, A.*, Ridley, J., S. C.** George, S.C.***, Mossman, D. J.**** and Volk, H. ****** School of Geosciences, University of Sydney, Sydney, NSW 2006 Australia**Department of Geosciences, Colorado State University, Fort Collins, CO 80523-1482, USA***Australian Centre for Astrobiology, Macquarie University, Sydney, NSW 2109, Australia****Department of Geography, Mount Allison University, Sackville, NB, E4L A7, Canada*****CSIRO Petroleum, P.O. Box 136, North Ryde, NSW 1670, AustraliaThe 2.1 Ga FA Formation sandstone of theFranceville Basin at Oklo in Gabon is noted forhosting the only known natural fission reactors in theworld (Naudet, 1991) and one of the most significantearly Precambrian accumulations of marine organicrichshales (McKirdy and Imbus, 1992). Hydrocarbonsexpelled from the shales are likely to have played akey role in concentrating uranium to levels sufficientto initiate nuclear chain reactions ca. 1968 ± 50 Ma(Gauthier-Lafaye and Weber, 1989; Nagy et al.,1991) and in facilitating effective containment ofuranium and fissiogenic isotopes at Oklo (e.g., Nagyet al., 1991). However, evidence for migration andgeneration of liquid petroleum has been limited toobservations of kerogen and solid bitumen within thereactors and surrounding rocks (Mossman et al.,1993) and to cursory observations of rare hydrocarbonbearingfluid inclusions (Mathieu and Cuney, 1998).Here, we report the discovery of widespread oilpreserved inside aqueous and carbonic fluidinclusions in a quartz pebble conglomerate from thevicinity of a reactor zone within the main uraniumdeposit at Oklo. The oil occurs within H 2O and CO 2-dominated inclusions trapped in syntaxial quartzovergrowths and intragranular and transgranularmicrofractures in detrital quartz. The presence of oilinside brine inclusions indicates that oil, brine andCO 2interacted with each other prior to trapping.Textural relationships and microthermometry suggestthat the initial entrapment of oil occurred first duringdiagenesis at ca. 115 to 200 °C soon after depositionof the sequence at ca. 2.1 Ga and later during ahydrothermal event at 200 to > 285 °C linked to theoperation of the reactors ca. 1.98 Ga. The highmaturity oil is non-biodegraded and contains hopane,2α-methylhopane, terpane and sterane biomarkersof bacteria, cyanobacteria and eukaryotes. Traceamounts of C 30n-propylcholestanes indicate acontribution from marine algae. The oil was likelyderived from conformably overlying marine blackshales that were deposited during the Great OxidationEvent.REFERENCESGauthier-Lafaye, F. and Weber, F., 1989. Econ.Geol., 84: 2267-2285.Mathieu, R. and Cuney, M., 1998. In: D. Louvat andC. Davies (Editors), Nuclear Science andTechnology, pp. 111-121.McKirdy, D.M. and Imbus, S.W., 1992. In: M.Schidlowski, S. Golubic, M.M. Kimberley, D.M.McKirdy and P.A. Trudinger (Editors), Early OrganicEvolution: Implications for Mineral and EnergyResources. Springer-Verlag, Berlin, pp. 177-192.Mossman, D.J., Nagy, B., Rigali, M.J., Gauthier-Lafaye, F. and Holliger, P., 1993. Int. J. Coal. Pet.,24: 179-194.Nagy, B. et al., 1991. Nature, 354: 472-475.Naudet, R., 1991. Oklo: des réacteurs nucléairesfossiles. Paris: Collection du Commissariat àl’Energie Atomique, p. 695.152

P11European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 154Fracture cementation of the Baksa Gneiss Complex, Pannonian Basin:Traces of paleofluids of extremely diverse originFintor, K.*, Tóth, T. M.* and Schubert, F. **Department of Mineralogy, Geochemistry and Petrology, University of Szeged, Szeged, H- 6701, HungaryInvestigation of fracture systems and thesubsequent cementation processes of rock bodiesare very important in many aspects, for example influid mining, geothermics or nuclear waste deposition.The Baksa Complex (BC) is a polymetamorphicbasement complex located in the southwestern partof the Pannonian Basin. The Baksa-2 well exploredthe BC over a thickness of 1200 m. Predominantly,the metamorphic rocks of the complex consist ofgneiss, mica schist with amphibolite, marble anddolomarble interbeddings.The aim of this study on one hand is to attemptto differentiate between the brittle deformation eventsand define the relative sequence of the fracture fillingminerals. On the other hand we try to determine theevolution of the paleofluids by analyzing fluidinclusions. Our investigations were made on thesamples from the upper 800 m of the Baksa-2 well.In the studied section three vein generations with thefollowing mineral sequences could be distinguished:Type I vein: ab+kfp+chl+ cc1,Type II vein:pi±czo+chl+pyr+cc2, Type III vein: qtz+cc3.In the Type Iveins feldspar thermometry(Nekvasil and Burnham, 1987) calculations show thatfeldspars (ab+kfp) were formed between 250–330°C. Chlorite was formed in the 280–320 °C temperatureinterval according to chlorite thermometry(Cathelineau, 1988). In the cc1 phase, aqueousinclusions of unknown genesis homogenise into theliquid phase between 90 and 140 °C, and show quiteconstant final melting temperatures at about –15 °C.In the Type II veins primary aqueous fluidinclusions in epidote and clinozoizite homogenisefrom 340 down to 180 °C and represent a very lowsalinity fluid (0.2–0.5 mass% NaCl eq.). The chloriteformingcondition is between 160–280 °C, based onchlorite thermometry (Cathelineau 1988). The Al 3+ /Fe 3+ in the octahedral position of the epidote structureand the T hvalues of the fluid inclusions decreasefrom the crystal cores to the rims. These observationssuggest that minerals of the Type IIveins precipitatedby decreasing temperature. The low homogenizationtemperatures (90–140 °C) of the fluid inclusions ofthe cc2 also support the above-mentioned observation.The measured T m(Ice) values (–26.7 to –16.8 °C)indicate high dissolved salt concentrations.In the Type IIIveins the quartz-hosted fluidinclusion assemblages (FIA) are arranged alongparallel growth zones. The T hvalues of the FIAs varybetween 70–130 °C but in the outermost zone arebetween 50–90 °C. The dissolved salt content is highin each fluid inclusion (T m(Ice): –27 to –19 °C). Thesalt concentrations that were calculated from themelting temperature of hydrohalite and ice phasesshow NaCl-dominant salt compositions (20.1–25.6mass% NaCl) with a minor amount CaCl 2(1.5–6.0mass% CaCl 2). Another characteristic feature of thisFIA is the significant amount of CH 4and N 2detectedin the vapor phase by Raman microspectroscopy.The fluid inclusions of the cc3 phase showhomogenization temperatures between 130 and180 °C. The T m(Ice) data (–25 to –22 °C) indicatehigh salt concentrations similar to the fluid inclusionsof the quartz phase.The propylitic mineral assemblages of Type Iand II veins indicate an identical origin of the two veingenerations. The microthermometric and mineralchemistry data suggest formation of this system froma low salinity hydrothermal environment duringdecreasing temperature. The chemical characteristicsof the paleofluids of the Type III veins suggest thepossibility of communication between the fluidsystems of the crystalline basement and the overlyingsediments.REFERENCESNekvasil H. and Burnham C. W . (1987)Physicochemical Principles. 500 p.Cathelineau M. (1988) Clay Miner. 23: 471-485154

P12European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 156Hydrocarbon inclusions in quartz – questions and answersJarmolowicz-Szulc, Katarzyna**Polish Geological Institute, Rakowiecka 4 , 00-975 Warsaw, PolandThe present paper will focus on fluid inclusionand isotopic studies of a special variety of hydrocarbonrichquartz crystals called “Marmarosh diamonds”,aiming at the problem of quartz as a tracer ofhydrocarbon fluid migration.These characteristic quartz crystals occur inthe Carpathians in veins and fissures. Their formationhas been studied for about a century in Europe(Tokarski, 1905). Although a lot has been alreadydone and explained, a lot of questions, however,remain.Fluid inclusions of microscopic sizes occur inquartz sampled in the SE of Poland, in the Carpathians.The newest occurrence reported consists of quartz inthe tectonic mélange zone, which has been recentlydistinguished and mapped (Jankowski andJarmolowicz-Szulc, 2004).The Marmarosh diamonds from the Westernand Eastern Carpathians contain both hydrocarbonand aqueous inclusions. This type of the quartz (Fig.1) occurs in euhedral, transparent crystals of idealcrystal habit and perfect reflection (Karwowski andDorda, 1986). The inclusions are either of primary orof secondary origins. The primary ones may bedivided into three groups of different phase-states,being either homogeneous or heterogeneous. Solidinclusions of various bitumens are also present. Theiramount is occasionally so high that the crystalsdisplay macroscopically a black colour. The liquidinclusions (mostly in the external growth zones) arefilled with one or two immiscible fluids. Gas inclusionscontain methane, pure and/or with some admixturesof heavier hydrocarbons or nitrogen. The heterogeneousinclusions contain variable ratios of phases,e.g. gas and liquid hydrocarbons plus aqueoussolution; gas and heavy hydrocarbons, aqueoussolution and solid bitumens, etc. (Jarmolowicz-Szulc,2004; Jarmolowicz-Szulc and Dudok, 2005).The Marmarosh diamonds sampled in differentregions in the Carpathians show distinct differencesin their fluid inclusions. However, a common featureis their co-existance with carbonates and organicmatter. Taken together, their features point to theprocess of migration of complex aqueous-hydrocarbonfluids. These paleofluids were rich in water, lighthydrocarbons (methane) and heavy hydrocarbons(oil) and in some localities also in carbon dioxide. Theveins and the melange zones where they occur werethe paths of fluid migration.The question is, what is the exact relationbetween these three components? Is the bituminoussubstance in the inclusions the same as that fillingthe empty space? Last but not least, is the quartz inthe rocks with the texture of block-in-matrix acharacteristic phenomenon for the mélange zones orfor the whole region?Fig. 1. The Marmarosh diamond from PolandREFERENCESJankowski L., Jarmolowicz-Szulc K. (2004) Pol.Geol. Soc. LXXV Conf. Abstr.: 122.Jarmolowicz-Szulc K. (2004) Appl. Min. 2: 827-829Jarmolowicz-Szulc K., Dudok I.V. (2005) Geol.Quart. 49: 291-304.Karwowski L., Dorda (1986) Min. Pol. 17:3-12.Tokarski J. (1905) Kosmos 30: 443-468.156

P13European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 158Colloid solutions within fluid inclusions in chalcedonyProkofiev, V. Yu.*, Melnikov F. P.**, Selector S. L.***, Ezhov A. A.** and Trubkin N. V.** IGEM RAS, per. Staromonetny 35, Moscow, 109017 Russia, vpr@igem.ru** Lomonosov Moscow State University, 119899 Moscow, Russia*** Frumkin Institute of Physical Chemistry and Electrochemystry RAS, Leninsky pr., 31–4, 119991,Moscow, RussiaIt is generally believed that colloid solutionscannot exist for extended periods in nature, owing totheir energetic metastability. Therefore, when studyingfluid inclusions (FI), scientists usually search only forsigns that colloids may have existed in the past,rather than for the colloids themselves. However,chemists recognize the concept of colloid particle“stabilization” in aqueous solutions under the influenceof various factors. It is now well known that in thepresence of certain stabilizers, colloid particles canbe maintained for long periods without undergoingcoagulation. For example, sulphurous compoundsand silica sols can operate as stabilization factors incolloidal systems.This report presents results of a study of FI inchalcedony from amygdules in Triassic basalts at theoptical-quality icelandic-spar deposit of Gonchak,Siberia. Melnikov et al. (1999) described these FI asrelicts of colloid solutions. The FI are between 30 and100 µm in diameter and they contain a liquid and agas bubble. The structure of the zones around all thecavities differs from that of the chalcedony, and thedifferences are obviously connected to FI formation.Analysis of the walls of the FI by scanningelectronic microscopy (JSM5300 instrument) hasshown that they consist of amorphous silica,occasionally with traces (a few wt.%) of Cl, Fe, Ca,Na, K and S. Fluorescence imaging of the FI wascarried out in the CPMOH of the University ofBordeaux 1, France. In a number of inclusions, aheterogeneous pattern of fluorescence was foundthat indicates the presence of films of differentcompounds. Examination of the chalcedony surfacesclose to and far from the FI by atomic-force microscopy(Solver Pro ATM) has revealed their structuraldifferences.The behaviour of the FI during microthermometry(Linkam THMSG-600 stage) is of greatest interest.Upon cooling, the solution in the inclusions freezesand becomes dark and eventually opaque attemperatures between –60 and –80 ºC. Upon heating,the first signs of a liquid appear in the temperatureinterval between –60 and –35 ºC. These temperaturesmay correspond to the eutectics of NaCl- and CaCl 2solutions. The ice melts between –10.1 and –19.7 °C,pointing to salinities in the range of 15.0 to 22.2 wt%eq. NaCl. Most of the FI homogenize to liquidbetween 70 and 160 ºC. After cooling from T h, thegas phase reappears in the form of numerous smallbubbles, which gradually coalesce into one largebubble. During slow cooling the small gas bubblesmay remain separate for 5 to 10 minutes beforecoalescing. Such behaviour cannot be observed intrue aqueous solutions. Rather, it is characteristic ofviscous colloidal systems in which micelles interferewith the merging of the gas bubbles. Apparently, asilica sol is present in the inclusions. Some of the FIhomogenize at higher temperatures (up to 380 ºC)and in these, only one large gas bubble reappearsupon cooling. The destruction of the silica sol attemperatures above 200 ºC may be the reason forthis effect.The above evidence suggests that colloidsolutions may be preserved in fluid inclusions withoutcoagulation for more than 100 million years. Theprecise physicochemical nature of the silicic-acidmicelle stabilization factor and the chemicalcomposition of the stabilizing compound are the mostimportant problems to study further in these FI.158

P14European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 160PVTx modelling of fluid inclusions in diamond quartz crystals from theSierra Madre Oriental, Southeast MexicoRamos-Rosique, Aldo*, Levresse, Gilles*, Tritlla, Jordi* and Jiménez Sandoval, Sergio***Centro de Geociencias, UNAM, Campus Juriquilla, 76230 Juriquilla, Queretaro, Mexico**CINVESTAV, Libramiento Norponiente No. 2000, 76230 Juriquilla, Queretaro, MexicoDoubly terminated quartz crystals usuallynamed “Herkimer Diamonds” occur in fractures inLate Jurassic-Early Cretaceous dolomitizedlimestones from the petroliferous province of Cuencadel Sureste in southern Mexico´s Sierra MadreOriental. The Sierra is a mountain belt formed duringthe Laramide Orogeny from Late Cretaceous – EarlyTertiary. The main source rocks for organic matter inthe oil fields are Tithonian shales and mudstones(Muir, 1938)Thermodynamic modelling of hydrocarboninclusions was performed using the homogenizationtemperature (Th) measured by microthermometry,and the degree of gas bubble filling (gas vol. %)measured by confocal scanning laser microscopy(CSLM). For aqueous inclusions the method uses thehomogenization and last melting temperature (Tm) inaddition to the molar fraction of methane quantifiedby Raman microspectrometry (Pironon et al., 2002).The procedure reconstruct the isopleth and theisochore for both aqueous (Peng & Robinson, 1976)and hydrocarbon fluid systems (Thiery et al., 2000),and the intersection of the two isochores in a P-Tdiagram represent the best approach to the trappingconditions.Aqueous inclusions. Only one primary inclusionwas observed present in petrographic associationwith hydrocarbon inclusions. Th = 135º C, Tm = -1.8º C, or 3.03 wt% eq. NaCl. Raman analysesindicate the presence of CH 4, in a concentration of0.3 molal. No CO 2has been detected. No aqueousinclusions are observed in fractures.Hydrocarbon inclusions. The Th of primaryintra-crystalline inclusions shows a distributionranging from 109 to 132º C with a maximum at130º C. In fractures crossing the whole crystal,inclusions show a Th homogeneous distributionranging from 116 to 120º C. CSLM volumetricreconstructions of both primary and secondaryhydrocarbon-bearing inclusions indicate a gas vol. %ranging from 10 to 20% and 8 to 15% respectively.There are numerous one-phase methane inclusionspresent in fractures, as indicated by the strong picksin Raman spectra that reveal the presence of this gasunder high pressures.All these data has been used to model thePVTx conditions for quartz precipitation using the PITsoftware (Thiery et al., 2000). The PT minimumconditions for the hydrocarbon primary inclusions are120º C and 180 bar. The minimum trapping conditionscalculated for the aqueous inclusion is 135º C and825 bar. The isochores of both systems will neverintersect. So we can assume that they are not inequilibrium.The PT trapping conditions of the inclusions infractures could not be determined due to the lack ofaqueous inclusions. The minimum PT conditions arecalculated at 120º C and 210 bar, which are verysimilar than those calculated for the intra-crystallinehydrocarbon inclusions, and confirm as the highmethane density inclusions present in fractures, thepost trapping re-equilibrium of the intra-crystallinehydrocarbon inclusions.Therefore we propose to consider the minimumcrystalization PT conditions to be at least comparablewith the aqueous inclusion PT minimum trappingconditions (135º C and 825 bar).REFERENCESMuir, J. M. (1938) The Science of Petroleum, vol. 1,Oxford Univ. PressPeng, D.Y. & Robinson, D.B., (1976) Industrial andEngineering Chemistry, 15, 59-64.Pironon, J., Grimmer, J.O.W., Teinturier, S.,Guillaume, D., Dubessy, J., (2002). PACROFI VIII,Halifax, Canada, Abstract.Thiéry, R., Pironon J., Walgenwitz F, Montel F,(2000) Jour. Geochem. Exp. 69-70, 701-704.160

P15European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 162Traces of hydrocarbon migration recorded by pore-filling analcime of afractured metabasalt complex, HungarySzabó, B.*, Schubert, F.* and Tóth, T. M. **Department of Mineralogy, Geochemistry and Petrology, University of Szeged, Szeged, H-6701, HungaryThe Kecel Basalt Formation is located in thesouthern part of the Pannonian Basin (Hungary). Asa result of periodic submarine eruptions, theintensively altered metabasalt layers have beenintercalated by thick marl layers of the Late MioceneEndrod Marl Formation. This latter stratigraphic unitis regarded as one of the most important hydrocarbonsource rocks in the area. Due to the high fractureporosity of the basalt some parts of the formation aregood reservoirs. The study area was explored by 21boreholes, which penetrated the metabasalt between2200 and 2900 m depth. The core samples are oftencrosscut by a usually completely filled fracturenetwork, in which three distinct vein types can bedistinguished.The subvertical Type 1 represents the oldestgeneration of fractures. The infrequent, narrow veinsare filled by weathered basaltic material → calcite 1(Fig. 1). The non-fluorescent calcite 1 shows a welldevelopedantitaxial texture (Bons, 2000), and itcontains solid inclusions from the wall rock due to thecrack-seal mechanism.The dense fracture network of Type 2iscemented by the following minerals: prehnite →calcite 2 → calcite 3 → laumontite. The prehnitecrystals exhibit core-rim textures defined by fluidinclusions. The primary aqueous fluid inclusions ofthe core zone homogenise into the liquid phasebetween 130 and 175 °C. The secondary aqueousfluid inclusions - cross-cutting the inner zone – consistof H 2O–CH 4, and they homogenize between 130 and140 °C. The calcite 3 phase shows a yellowishfluorescence colour under UV excitation, and containsmany one-phase (L) and two-phase (L+V) aqueousfluid inclusions randomly distributed.The Type 3 shows similar appearance to theType 2, but occurs only sporadically in the samples.The veins are cemented by analcime → heulandite→ stilbite phases. The temporal sequence of theanalcime-hosted fluid inclusions is the following:early primary aqueous (L+V) → pseudosecondaryaqueous (L+V) → intermediate primary yellowfluorescent hydrocarbon (L+V/L) → late primaryaqueous (L+V) and blue fluorescent hydrocarbon(L+V). The early primary and the pseudosecondaryaqueous inclusions in analcime homogenize between120 and 150 °C, and the late primary hydrocarboninclusions between 105 and 145 °C. The heulanditephase also contains a lot of liquid-dominated aqueousand blue fluorescent hydrocarbon inclusions, but thestilbite phase lacks of fluid inclusions.Fig. 1 Mineral sequence of the veins.By combining fluid inclusion microthermometrywith modelling the P-T stability fields of vein fillingminerals by the WinDomino software package, areliable evolution of the basaltic reservoir can besketched. It is shown that only the cementation of theType 3veins contains hydrocarbon inclusions. Thisbehaviour suggests that, although the whole basalticcomplex was extremely fractured, there existed onlycertain communicating subsets in the complicatedfracture-system of the reservoir. Accordingly, only thewells which penetrate Type 3 fractures are productivetoday.REFERENCESBons P. D. (2000) Formation of veins and theirmicrostructures. J. of the Virtual Explorer, 2162

P16European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 164Healed microcracks in late Variscan granites – comparison between theNE Bavarian Basement and the Harz Mountains (Germany)Hennings, Sibylle*, Vollbrecht, Axel*, van den Kerkhof, Alfons M.* and Hein, Ulrich F.**Geowissenschaftliches Zentrum der Georg-August-Universität, Goldschmidtstr.3, D-37077 GöttingenFabrics of healed micro-cracks in quartz andmicro-thermometric data of related secondary fluidinclusions reveal significant differences between late-Variscan granites of the NE Bavarian Basement andof the Harz Mountains. These differences concernthe inferred crack mechanisms and driving forces,the composition of the trapped paleo-fluids as well asthe estimated P/T conditions of crack formation.Micro-structural data of several granites fromNE-Bavaria uniformly indicate that healed cracks inquartz are preferentially arranged in a zone aroundthe crystallographic c-axis, i.e., normal to the directionof maximal thermal contraction (Vollbrecht et al.,1994a). Accordingly, the considered micro-crackscan be classified as mode I (extensional) cracks(e.g., Lawn & Wilshaw, 1975). At the regional scale,these extensional micro-cracks display a preferredorientation which can be well correlated with the late-Variscan stress field (Vollbrecht et al., 1994b).This implies that grains with a suitablecrystallographic orientation with respect to theregional stress field were preferentially affected bythermal cracking. The cracks are decorated bysecondary aqueous inclusions of low salinity. Theintersections of their isochores with probablegeothermal paleo-gradients indicate depths between5 and 10 km for micro-crack formation (Vollbrecht etal., 1991).In consequence we conclude that microcrackingin quartz occurred during late-Variscancooling of the granites during uplift, and that (internal)thermo-elastic stress, i.e. shrinkage of the hostcrystal, was the main driving force. Low-salinity H 2O-NaCl fluids were the dominant geo-fluids during thisstage.In contrast, our first results of a study carriedout on the Brocken granite of the Harz-Mountainsshows crack propagation preferentially along therhombi of quartz, i.e. along crystallographic planes oflow surface energy. Moreover, the cracks displayirregular curved shapes and escape features whichpoint to a mode II (shear) type (e.g., Lawn & Wilshaw,1975). This agrees with their bulk orientation almostparallel to WNW-trending strike-slip faults, whichwhere active during post-Variscan (Alpine) tectonics.The cracks are decorated by secondary aqueousinclusions of moderate salinities and complex H 2O-NaCl-CaCl 2compositions. If the corresponding isochoresare related to geothermal gradients assumedfor the Cretaceous, P/T estimates for crack formationrange between 6 and 2 km.The data suggest that micro-cracking occurredin response to (external) tectonic stresses at highercrustal levels during the Cretaceous (Hennings,2006).Micro-cracks which may be related to thermalcracking have not been observed in the Harz granite,so far. One probable explanation is that the coolingrate was significantly lower than for the Bavariangranites. Therefore, a release of internal thermoelasticstresses could be achieved by other processes,such that thermal stresses did not reach criticalvalues for crack initiation.REFERENCESHennings, S. (2006): unpubl. B.Sc. thesis, Univ.Göttingen: 32 pp.Lawn. B.R., Wilshaw, T.R. (1975): Fracture of BrittleSolids. Cambridge University Press: 204pp.Vollbrecht, A. et al. (1991): J. Struct. Geol.13/7: 787-799.Vollbrecht A. et al. (1994a): Textures of GeologicalMaterials. DGM Informationsgesellschaft Verlag,Oberursel: 345-352.Vollbrecht, A. et al. (1994b): Sci. Drilling 4: 233-241.164

P17European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 166Fluid-rock interaction along a crustal shear zone: results from a fluidinclusion study on the Filali unit, Rif chain (Morocco)Tecce, Francesca*, Rossetti, Federico**, Olivetti, Valerio** and Bouybaouenne, Mohamed L. **** IGAG- CNR, Roma, Italy** Dipartimento di Scienze Geologiche, Università Roma Tre, Roma, Italy*** Département de Géologie, Faculté des Sciences , Université deRabat, Rabat, MoroccoReconstruction of deformation history duringthe changing P-T conditions associated with burialand exhumation of an orogenic terrane necessarilyrequires an integrated approach aimed at definingrelationships between deformation microstructures,metamorphism and fluid-rock interactions. Veins areone of the most visible manifestation of fluid flowduring orogenic complex formation. In this context,the study of fluid inclusions hosted in the mineralsfilling the veins may provide clues to the tectonothermalhistory and inferences on the paleo-fluidcirculation associated with orogenic construction.The Rif of northern Morocco and the Betics ofsouthern Spain represent the western termination ofthe Alpine orogenic system, resulting from theMesozoic-Cenozoic plate convergence betweenAfrica and Eurasia. In the internal Rif, the effects ofthe Alpine orogenic evolution are clearly documentedin the Septides units. These consist of two majormetamorphic complexes: an upper one made of HP/LT rocks and a lower one made of Barrovian-type,amphibolite-to-granulite grade sequences andperidotites. Still debated is the timing and tectoniccontext during coupling of the two metamorphiccomplexes.The Fillali unit is a part of the lower Septidesand consists of several kilometres thick sequence ofheavily sheared micascists and minor gneisses lyingbetween the overlying HP/LT units and the underlyingHP/HT domain. Sheared rocks have a moderate tostrongly developed mylonitic foliation and a mineralstretching lineation trending NW-SE, which formedduring D 2-D 3. Shear sense is systematically top-tothe-N/NWand the metamorphic conditions vary fromandalusite to sillimanite-K-feldspar grade. Ductileshearing was accompanied by extensive fluidcirculation and infiltration as attested by the widespreaddevelopment of composite quartz-andalusitevein arrays in the exposed rock sequences.Three main generations of quartz veins havebeen recognized, and classified as pre- (V1), syn-(V2) and post- (V3) kinematic relative to the shearfabric. These veins are interpreted as incrementallydeveloped during progress of the shearingdeformation. The V1 and V2 veins show commonrecrystallization textures (core and mantle structures),mainly assisted by GBM and SR. Present are alsohealed microfractures that either terminate at lobategrain boundaries or cut the grain boundaries. In theV3 veins, microfracturing and the effects of pressuredissolutioncreep are instead common. Fluidinclusions are abundant along the grain boundariesand in the healed microfractures. Two main types offluid inclusions have been distinguished: (i) Type-A,consisting of L+V (CO 2+H 2O), V-rich fluid inclusions,mainly distributed along the grain boundaries; and (ii)Type-B, two-phase L+V, L-rich (H 2O+NaCl) inclusions,occurring both along the grain boundaries and alongthe trails. In the V3 veins only Type-B is present.Homogenization temperatures between L and Voccur between 250 and 350 °C, except for the V3samples which show lower Th values (110–150 °C).Representative isochores show that vein segregationoccurred during transient and fluctuating (fromlithostatic to hydrostatic) fluid pressure conditionsaround the background paleogeothermal gradient of25-30 °C/km. Using these constraints, the dataindicate that shearing started within the sillimanitefield (0.4–0.5 GPa and 500–600 °C) and accompaniedprogressive exhumation of the Filali unit duringcontinuous shearing. The similar kinematics and themarked increase in the metamorphic grade of theupper Septides when approaching the Filali unit,suggest that shearing likely operated duringcontinental collision in a regime of viscous heating.166

P18European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 168Oxygen fugacity and CO 2– N 2fluid inclusions as remnants of fluid andgeodynamic evolution of the Ribeira Fold Belt, SE BrazilBento dos Santos, Telmo M.*, Munhá, José M. U.*, Tassinari, Colombo C. G.**, Noronha, Fernando M.***,Guedes, Alexandra***, Fonseca, Paulo E.****, Dias Neto, Coriolano** and Dória, Armanda****Centro/Depart. de Geologia, Universidade de Lisboa, C6, 3º, Campo Grande, 1749-016 Lisboa, Portugal**Instituto de Geociências, Universidade de São Paulo, Rua do Lago, 562 – Butantã, 05508-080, SP, Brazil***Centro de Geologia, Universidade do Porto, Rua do Campo Alegre, 687, 4169-007 Porto, Portugal****LATTEX, Universidade de Lisboa, C6, 2º, Campo Grande, 1749-016 Lisboa, PortugalThe studied São Fidelis - Santo António dePádua (SFSAP) sector, located in central RibeiraFold Belt, a Neoproterozoic granulitic belt along theSE coast of Brazil, comprises abundant migmatiticgneisses (kinzigites and khondalites) and charnockites,as well as their deformed counterparts (blastomilonites)that resulted from late shearing and exhumation atthe end of the Panafricano – Braziliano Orogeny.The use of extensive methodology, namelyfluid inclusion (FI) microthermometry, Ramanspectroscopy, x-ray diffraction, mineral chemistryanalysis and oxygen fugacity modelling, provided thefollowing results: i) Magnetite-Hematite ƒO 2estimatesrange from 10 -17.799 to 10 -11.538 bar for the determinedmineral temperature range of 656 to 896 ºC (Bentodos Santos et al., 2005); ii) charnockites show ƒO 2above the QFM buffer (QFM +1), while blastomilonitesand migmatites have ƒO 2at QFM–1, implying thatthe SFSAP sector rocks experienced ƒO 2decreaseas temperatures dropped; iii) 5 main types of fluidinclusions were observed, from oldest to youngest: a)N 2(94 to 95 mol%) – CH 4(5 to 6 mol%) FI; b) CO 2and CO 2-N 2(0 to 11 mol%) high to medium density(1.01 – 0.59 g/cm 3 ) FI; c) CO 2and CO 2-N 2(0 to 36mol%) low density (0.19 to 0.29 g/cm 3 ) FI; d) CO 2(94to 95 mol%) – N 2(3 mol%) – CH 4(2 to 3 mol%) – H 2Oand H 2O–CO 2FI; and e) late low-salinity H 2O FI; iv)Raman Spectroscopy reveals two graphite types inkhondalites: an early highly ordered graphite cut by adisordered kind. The use of a Raman-based graphitegeothermometer supplied temperature estimatesranging from 333 ºC, for the most disordered graphite,to 449 ºC, for the highest temperature type.Combination of data taken from the previousmethodologies allowed the characterization of fluidand geodynamic evolution of this lower crust segmentin the last stages of the Braziliano cycle. Thus, theRibeira Belt metamorphic fluids evolved fromdominantly N 2-CH 4fluids to dominantly CO 2-N 2fluidsduring granulitic metamorphism at high oxygenfugacities. This evolution occurred via the combinedprocess of CO 2generated by graphite oxidation(Cesare et al., 2005) and CO 2concentration uponwater loss to ascending granitic melts (Bento dosSantos et al., 2006), followed by late ƒO 2decreaseinduced by the influx of water, turning carbonic fluidsinto CO 2-H 2O, and progressively into low-salinity H 2Ofluids.The stated fluid evolution took place due to arapid pressure drop during the late retrogradeexhumation path of the Ribeira Fold Belt. Resultsshow that at about 400-450 ºC the rocks wereexhumed to near surface depths, producing generallylow-density CO 2inclusions, followed by influx ofsurface water. When ƒO 2decreased substantially bymixture of carbonic and water inclusions, graphitedeposited, forming khondalites.REFERENCESBento dos Santos, T., Munhá, J., Tassinari, C., DiasNeto, C., 2005. Ext. Abst. VIIi Congr. Geoq. PALOP,1, 95-100.Bento dos Santos, T., Munhá, J., Tassinari, C., DiasNeto, C., Fonseca, P., 2006. Ext. Abst. VII Congr.Nac. Geol., 1, 241-244.Cesare, B., Meli, S., Nodari, L., Russo, U., 2005.Contrib. Min. Pet., 149, 129-140.168

P19European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 170Fluid inclusion investigations on fissure minerals from the GotthardNEAT base tunnel (Central Alps).Heijboer, Tjerk*, Mullis, Josef**, Amacher, Peter***, Vennemann, Torsten** Institut de Minéralogie et Géochimie, Antropôle, 1015 Lausanne, Switzerland** Mineralogisch-Petrographisches Institut, Bernoullistr. 30, 4056 Basel, Switzerland***GEO-URI, 6474 Amsteg, SwitzerlandAlpine type fissures in the Gotthard base NEATtunnel have been investigated with the aims to:1. Understand the evolution of fluid composition,temperature, pressure and defor-mation duringuplift and cooling of the Central Alps;2. Recognize the origin and fluid flow paths ofmineralising fluids;3. Document the mass transport from the unalteredhost rock into the Alpine fissures under continuouslychanging conditions (Heijboer, 2006);4. Model and understand fluid-mineral equilibria.The Alpine fissures were sampled along theGotthard NEAT base tunnel and cable tunnel fromAmsteg. Microthermometric investigations on fissureminerals yield the following results:1) Aqueous fluids are common in Alpine fissuresfrom the cable tunnel at Amsteg (Heijboer, 2006),in the Gotthard base tunnel between Amsteg andSedrun and south of Sedrun. This is similar to fluidinclusion data of Alpine fissures from the surface(Mullis et al., 1994). These fluids were trapped atretrograde PT-conditions between ≥420 and 250°C and ≥4 and 2.2 kbars. Late tectonic eventsvery locally allowed carbon dioxide enriched fluidsto enter the water dominated hydrothermal system.In Amsteg, these fluids precipitated siderite inalready formed Alpine fissures.2) Carbon dioxide dominated fluids are found inTessin habit quartz found in the tessin area. Thesefluids were trapped in crystals which formed at430 +/- 20 °C and 2 to 3 kbars (Mullis et al.,1994).In the Amsteg area investigations were carriedout (Heijboer, 2006) to solve the aims 2-4 (seeabove). δD values of early to late aqueous fluidinclusion populations are –40 to 80‰ and δ 13 C valuesof small amounts of CO 2in the fluid inclusions are -10‰, which are similar to those of the vein calcite.H-O isotopic values of chlorite are -30‰ and +3.4‰indicating that the mineralizing fluids in the veinswere metamorphic, with possible minor externalcomponents. Quartz-calcite and quartz-chloritemineral pairs all show values in equilibrium with thehost rock. In addition, δ 13 C and δ 18 O isotopic values(-9‰ / +8‰) of the rhombohedral and tabular veincalcite indicate metamorphic fluids equilibrated withthe meta-sedimentary basement.Cl/Br ratios are relatively variable (rangingbetween 0.5 and 4.5) and may therefore indicatechanging local origins of the fluids. Na/K and Na/Liratios were relatively homogeneous (1-10 and 40-200) over the different fluid populations showing onlyminor changes and correspond to temperatures of320 to 250 °C. Very little host-rock alteration tookplace during the mineralization, apart from a smallbleached halo around some parts of the veins. Themajor element compositions of the host rock did notshow significant change.Vein mineralization itself is consistent withhost-rock controlled precipitation. Temporal changesin mineralization from adularia to albite and back toadularia may indicate a short-lived increase in fluidtemperature during further opening of these veinsystems or influx of fluids more rich in Na than thelocal vein fluid, or both.REFERENCESHeijboer, T.C. (2006) PhD thesis, University ofBasel.Mullis, J., Dubessy, J., Poty, B. & O’Neil, J. (1994)Geochim. Cosmochim. Acta., 58, 2239-226.170

P20European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 172The application of fluid inclusions to fluid geochemistry andgeothermobarometry in diagenetic and low-grade metamorphic rocks inthe external parts of the Central AlpsMullis, Josef* andTarantola, Alexandre***Mineralogisch-Petrographisches Institut, Bernoullistrasse 30, 4056 Basel, Switzerland**Institute of Geological Sciences, University of Bern, Baltzerstrasse 3, 3012 Bern, SwitzerlandCareful fabric, host mineral and fluid inclusionanalyses of several hundred localities of the externalparts of the Central Alps enable a critical discussionabout their application to fluid evolution and fluidthermobarometry. For this goal detailed fluid inclusioninvestigations within early (prograde), intermediate(PT-maximum) and late (retrograde) vein, fissure andslickenside systems of hydrocarbon bearing diagenetic,anchi-metamorphic and water bearing epimetamorphic(greenschist facies) terranes weremade. The prograde, peak temperature and retrogradefluid composition and density with theirsuitability for geothermobarometry are discussed.Once trapped, fluid inclusions may re-equilibrateby modification of their composition anddensity. This occurs by stretching, leakage or decrepitationof fluid inclusions when internal fluid pressureexceeds the confining pressure during further burial(McLimans 1987, Bodnar 2003). Furthermore, fluidinclusions might be reset by static or dynamicrecrystallization of the host minerals (Wilkins andBarkas 1978). During retrograde evolution, isothermalpressure drop leads to stretching and decrepitation ofhigh density fluid inclusions (Mullis 1988).Our results indicate that:1. Fluids trapped at an early stage along the progradepath have re-equilibrated due to fluid overpressure,decrepitation and recrystallization of host mineral.Such fluid inclusions do not reflect compositionand density of the fluid trapped during mineralgrowth.2. In some rare cases of very small fluid inclusions,early inclusions may be preserved and reflect theprograde fluid composition and density.3. Hydrocarbon-saturated water-rich and watersaturatedhydrocarbon-rich fluid inclusions formedaround the PT-maximum and during retrogradeconditions are of reliable quality for geothermometry.If the volatile part consists of pure methane,inclusions may be used as both geothermometersand geobarometers (Mullis 1979).4. Care has to be taken with originally high densityfluid inclusions, which were stretched by local andtemporary pressure drops and re-equilibratedduring maximum temperature and retrogradeconditions.5. With increasing metamorphism, thermal crackingof higher hydrocarbons yields methane. Thetransition from the CH 4- to the H 2O-dominatedfluid zone is the result of redox reactions occurringat 270 ± 5° C (Mullis 1987, Tarantola et al. 2007).Typical examples of Alpine fissures formedduring prograde and retrograde conditions wereselected, i.e.: Wellenberg, a candidate location ofradioactive waste repository, Linth valley and others.REFERENCESBodnar R.J. (2003) Mineralogical Association ofCanada, Short Course Series Volume 32: 213-232.McLimans R.K. (1987) Applied Geochemistry 2:585-603.Mullis J. (1979) Bull. Minéral. 102: 526-536.Mullis J. (1987) In Low temperature metamorphism(ed. M. Frey): 162-199. Blackie.Mullis J. (1988) Schweiz. mineral. petrogr. Mitt. 68:157-170.Tarantola A., Mullis J., Vennemann T., Dubessy J.and de Capitani C. (2007) Chem. Geol. 237: 329-357.Wilkins R.W.T and Barkas J. P. (1978) Contrib.Mineral. Petrol. 65: 293-299.172

P21European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 174A fluid inclusion study in thenardite and associated mineralisationsfrom burning coal waste heap, Avion, Northern FranceCoquinot, Yvan* & **, Dubois, Michel*, Masalehdani, M.*, Naze N.* and Potdevin, Jean-Luc**UMR 8110 “PBDS”, Université de Lille 1, UFR Sciences de la Terre, 59655 Villeneuve d’Ascq, France** Mineralogy and Petrology Group, Univ. of Leoben, Austria. Present addr.: Musée du Louvre, Paris,FranceVery few studies reported the occurrence ofsecondary minerals forming around gas vents fromburning coal waste heaps. Gas exhaled from surficialvents and fissures and different soluble mineralsoriginated from cooling gas reveal important informationabout the chemical composition of burningcoal and the possible interaction of the gas with rockand water on its way to the surface prior to exhalation.Previous investigators have identified minerals butnone of them have reported the occurrence oftrapped fluid inclusions in efflorescent salt mineralsoriginated from coal fire gas. At the burning coalwaste heap n°76 in Avion a variety of fumarolerelatedminerals (sulphates, halides and nativesulphur) was identified depositing on the rock debris(Masalehdani, 2006). This work presents the preliminaryresults of the study of fluid inclusions incrystals of sodium sulphate (thenardite) Microthermometrycombined with Raman microspectrometryat low temperature was used to investigate theinclusion properties.The inclusions reach 60 µm in size and occureither as isolated inclusions or as clusters composedof 3 to 15 objects. They can be considered as primaryor pseudosecondary. The main feature of theinclusions is the high variability even in a singlecluster of the vapour filling ratio (Rflv). Rflv rangefrom 0 (pure liquid) to 1 (pure vapour).The eutectic temperature (range -40 to -30 °C),although to be taken with caution, indicates a solutiondominated by Na 2SO 4and NaCl. However, additionalsalt can not be excluded. Ice melting temperatureshave been measured between -24.5 and -23.4 °C.During cooling the formation of a solid has beennoted in some inclusions. The observation of itsdisappearance occurs between +17.3 and +24 °C.The nature of this solid phase could not be determinedoptically and Raman requires additional knowledgeof the salt spectra (mirabilite, heptahydrate).The mineralising fluid was essentially aqueous.No volatile species has been detected (above thedetection limit of Raman). The concentration estimatedfrom microthermometry using phase relationsin the H 2O-NaCl-Na 2SO 4system, is high (probably ashigh as 50 wt%)Homogenisation temperatures are low (lowerthan 150 °C, mainly lower than 100 °C). In surfaceconditions, homogenisation temperatures can be consideredas true trapping conditions. The temperatureof the mineralising fluid is therefore relatively low(lower than 150 °C). This point is corroborated by thepresence of all-liquid inclusions (considered astrapped below 70 °C). All-vapour inclusions andhighly variable Rflv could be interpreted either asresulting from effervescence (but the nature of thegas has not been identified), boiling (but unlikely inthe estimated temperature conditions) or moreprobably a mecha nical trapping of the fluid with air.The brittle character of thenardite can also beresponsible of post-trapping alteration of inclusions.The themardite crystals and probably theassociated mineralisation therefore result from theprecipitation of an aqueous liquid-like fluid of lowtemperature. Additional work is needed, especiallyregarding the consequences of the thenardite tomirabilite transition on fluid inclusions.unidentified solid20 µmFig. 1. Two-phase inclusions in thenardite crystalsREFERENCESMasalehdani M.N.N. (2006) Ph-D thesis, Universityof Lille, France174

P22European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 176The carbonated serpentinites in Tuscany (Italy), a geological analogueof carbon dioxide sequestration: information from fluid inclusions data.Ruggieri, Giovanni*, Boschi, Chiara**, Dallai, Luigi**, Dini, Andrea** and Gianelli, Giovanni***CNR-Istituto di Geoscienze e Georisorse, U.O. di Firenze, Via La Pira 4, 50121, Florence, Italy**CNR-Istituto di Geoscienze e Georisorse, Sede di Pisa, Via Moruzzi 1, 56124, Pisa, ItalyCO 2sequestration by carbonation of magnesiumsilicate minerals is one storage mechanismbeing considered for implementation on an industrialscale. Mineral carbonation binds CO 2into the latticeof carbonate minerals forming stable and environmentallyharmless by-products such as magnesite.This process is considered to be the only method fordisposing CO 2on a geologic time-scale with minorrisk of leakage. Although the reaction has provendifficult to be induced in the laboratory, the rockrecord of the process is ubiquitous in serpentiniteterrains. Fossil mineral carbonation systems, whichoccur as magnesite deposits hosted by intensivelyaltered serpentinites, are well-exposed in Tuscany(Italy). Two main carbonation types, intimately associated,have been observed: (1) metasomaticreplacement of the serpentinites; (2) infill precipitationin stockworks and discrete veins/lodes up to 4 mthick and hundred meters wide.The goal of this study is to investigate thedistribution of characteristic mineralogical transformations,the mobility of major and trace elementsduring the hydrothermal processes, and the chemistryand P-T conditions of mineralizing fluids in order toimprove the knowledge of the in situ mineralcarbonation processes and CO 2sequestration.Preliminary analyses on the Colline pisanearea show that the deposits formed at shallow depthand that they are essentially made by magnesite (upto 80-90 % MgCO 3) with minor amount of quartz,dolomite and iron hydroxides. The mineralogy oftenshows a significant vertical zonation (carbonate- vssilica-rich zone in deeper). Accordingly, petrographicstudies indicate a subsequent precipitation of earlymicrogranular magnesite, comb-textured dolomiteand finally quartz into the veins. This first evidencesuggests that the composition of the hydrothermalfluid changed in time and in space, at micro andmega-scale (?), producing different mineral assemblages.Fluid inclusions suitable for microthermometryhave been observed in both dolomite and quartzcrystals, but not in magnesite. At room temperature,fluid inclusions are one-phase (liquid) or two-phase(liquid+vapour, liquid-rich). Some one-phase inclusionsnucleate a vapour bubble after freezing runs.Primary fluid inclusions confined within growth-zoneboundaries have been observed in both dolomite andquartz. Some inclusions in quartz are secondary and/or pseudo-secondary. Tm iceof inclusions in dolomite(-0.7/-1.1 ºC) differ from Tm iceof the inclusions inquartz (0.0/-0.2 ºC), suggesting that the first are moresaline and/or have a higher CO 2content than thelatter. This agrees with the temporal variation of thehydrothermal fluid evidenced by minerals textures. T hof fluid inclusions in quartz and dolomite (109/195 ºCand 90/156 ºC respectively) are close to the trappingtemperature since the hydrothermal system developedclose to the surface. These temperature rangesfavour the carbonation process, as this process iskinetically enhanced by rising temperature, althoughis thermodynamically limited to 200 ºC (IPCC SpecialReport, 2005).REFERENCESIPCC Special Report (2005), Cambridge Universitypress, Cambridge, New York, 1-62.176

P23European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 178Experimental Raman spectra of salt hydrates in fluid inclusionsBakker, Ronald J.*, Baumgartner, Miriam* and Coquinot, Yvan**Mineralogy & Petrology, Institute of Applied Geosciences and Geophysics, University of Leoben, Peter-Tunner-Str. 5, 8700 Leoben, AustriaThe properties of fluids in crustal and mantlerock, as generally obtained from fluid inclusions, areof major importance in understanding processes thatmay occur in these rocks. Microthermometry is oneof the most important analytical technique to obtainapproximate composition and density of fluidinclusions. In combination with Raman spectrocopy itprovides a tool to estimate the major dissolved saltcomponents in aqueous fluid inclusions. The aim ofthis study is to characterise the Raman spectra ofspecific brines in synthetic fluid inclusions at lowtemperature, to identify salt-hydrate spectra andmetastabilities during microthermometry.The synthesis of the fluid inclusions isperformed in our hydrothermal laboratory, usingexternally heated pressure vessels. Argon is used asa pressure medium. The cracked natural quartzcores were put together with a brine (NaCl 2-CaCl 2-MgCl 2-LiCl) in Au-capsules, which were carefullywelded. Crack-healing occurred at 600 ˚C and variouspressures (86 - 310 MPa) in separate experiments.Subsequently, the quartz cores were cut into 1 mmthick slices and doubly polished. The salinity of thefluid inclusions was checked with microthermometry.A series of experiments was performed withH 2O-NaCl fluids of variable salinity, confirming thehydrohalite spectra from Bakker (2004) at - 180 ˚C:four main peak positions at 3536 cm -1 , 3435 cm -1 ,3421 cm -1 and 3404 cm -1 (±1). Hydrohalite wasdetected in fluids down to 4 mass% NaCl. The peakintensities strongly varied with orientation of thehydrate crystal in the inclusion. Experiments withH 2O-MgCl 2fluids (30 mass% MgCl 2) revealed a morecomplex hydrate spectrum (MgCl 2·12H 2O) thanpresented in Bakker (2004). The main peaks arepositioned at 3511, 3460 and 3400 cm -1 (at -180 ˚C),which is shifted about 5 wavenumbers to lowervalues, due to an improved calibration method. Themain peaks contain numerous shoulders, which candevelop to real peaks in specific crystal orientations(e.g. 3480, 3440 and 3425 cm -1 ). At 3360, 3345,3323, 3216 and 3190 cm -1 relative small and broadpeaks occur. A metastable MgCl 2·6H 2O crystal wasalso observed in this fluid, with sharp peaks at 3532,3502, 3400, 3360 and 3345 cm -1 . The first two peaksclearly diverge in position from the spectrum ofMgCl 2·12H 2O. A series of experiments was performedwith H 2O-CaCl 2fluids of variable salinity. CaCl 2·6H 2Ocrystals were observed in fluid inclusions at lowtemperatures, with peak values at 3432, 3406 and3387 cm -1 . Shoulders can develop to individual peaksat 3412 and 3402 cm -1 depending on crystalorientation. Ternary fluid mixtures of H 2O-MgCl 2-CaCl 2in inclusions develop to a mechanical mixtureof individual salt-hydrate crystals at low temperatures.Both CaCl 2·6H 2O and MgCl·12H 2O can be individuallyanalysed, or give a mixed Raman spectrum at theinterface.The Raman spectra of salt hydrates at lowtemperatures in fluid inclusions in quartz are notmodified by polarization of the laser beam in the hostcrystal (see Baumgartner et al., 2007). The complexityof the spectra requires a systematic analysis bydeconvolution into a variety of peaks, according toGaussian-Lorentzian best-fit curves, in order tocharacterise their shape and development withchanging temperatures.REFERENCESBakker R. J. (2004) Can. Mineral. 42: 1275-1282.Baumgartner M., Bakker R.J., Coquinot Y. (2007)ECROFI-XIX, this issue.178

P24European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 180Fluid inclusion analysis using synchrotron radiationCauzid, Jean a , Bleuet, Pierre a , Martinez-Criado, Gema a , James-Smith, Julianne a,b , Hazemann, Jean-Louis c ,Testemale, Denis c , Proux, Olivier d , Brugger, Joël b , Liu, Weihua e , Rickers, Karen fandPhilippot, Pascal g .aESRF, 38042, Grenoble, FrancebDepartment of Geology & Geophysics, University of Adelaide, 5000, AustraliacInstitut Néel, CNRS, 38042, Grenoble, FrancedLab. De Géophysique Interne et Tectonophysique, UMR CNRS Université Joseph Fourier, 38400 Saint-Martin-d’Heres, FranceeMinerals and Exploration, CSIRO, Clayton, AustraliafHASYLAB at Deutsches Elektronen-Synchrotron DESY, Notkestrasse 85, Hamburg, 22603 GermanygGéobiosphère Actuelle et Primitive, IPGP, Paris, FrancePhoton-matter interactions are powerful meansof investigating electronic organisation of a sample.Bearing no charge nor weight, photons can penetratecondensed matter with little or even no damage. Assuch they are of very high interest for studyingheterogeneous fluids included in mineral matrices.Third generation synchrotrons provide high fluxes ofphotons for focusing, photon energy tuning andmultitechnique detection. We propose an overview ofthe tools suitable for fluid inclusion analyses availableat the ESRF.Current improvements and foreseen evolutionsof the optical devices and detectors at the ESRF willbe shown to clarify the new possibilities they willbring to fluid inclusions studies.Synchrotron Radiation induced X-rayFluorescence (SR-XRF), X-ray Absorption Near EdgeStructure (XANES) and X-Ray Diffraction (XRD)have been applied to liquid and vapour inclusionsfrom the Yankee Lode deposit, Mole Granite, Australia.Each of these techniques provides information on theinclusion chemistry complementary to those obtainedwith more classical analytical methods. Quantificationof the fluid with SR-XRF can be performed throughpunctual (1D), mapping-based (2D) and fluorescencetomography (3D) measurements. SR-XRF imaging in2D and 3D (Fig. 1) provides information on elementaldistribution and concentration inside the fluid, whileXANES spectroscopy gives insight in elementalspeciation (i.e., oxidation state; nature and geometryof aqueous complex). XRD helps in determining soliddaughter phases commonly present in inclusions.Synchrotron-based techniques can be performed insitufrom low- to high-temperature with theimplementation of microthermometric heatingfreezingstage on the experimental end-station. Thisis of great interest for determining elemental speciationat trapping conditons.Fig. 1. Quartz crystal hosting four inclusions: threevapour inclusions and one liquid inclusion. Thereconstruction in three dimensions of the X-raytransmission (top left) shows inclusion positions.The two inclusions at the top of the sample and theone at the botton right are vapour inclusions. Thelast inclusion (bottom center of the sample) is thegas bubble present at room temperature in a liquidinclusion. Concentrations in Fe (bottom left), Cu (topright) and As (bottom right) show that Cu isconcentrated in vapour inclusions, Fe in the liquidone and As is present in both inclusion types.180

P25European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 182High resolution X-ray computed tomography of fluid inclusionsKyle, J. Richard and Ketcham, Richard A.Department of Geological Sciences, Jackson School of Geosciences, The University of Texas at Austin, 1University Station, C1100, Austin, TX 78712, USAHigh resolution X-ray computed tomography(HRXCT) is the industrial equivalent of medical CATscanning and provides a mechanism for nondestructive,in-situ studies of the three-dimensionaldistribution of fluid inclusions within minerals. HRXCTproduces two-dimensional images that reveal theinterior of an object as if it had been sliced openalong the image plane for viewing. A HRXCT imagereflects differences in X-ray attenuation, which isprimarily a function of density and atomic number. Byacquiring a contiguous set of slices, a density map forall or part of a sample volume can be obtained,allowing three-dimensional inspection andmeasurement of features of interest.The University of Texas at Austin HRXCTlaboratory is a NSF-supported multi-user facility thathas been used for the past decade to produceinformation for a wide variety of geological, biological,and material science problems. Descriptions of thefacility, HRXCT principles, and examples ofapplications are available at http://www.ctlab.geo.utexas.edu/. The facility has two subsystems that areused to image geological specimens across a rangeof sizes. Fluid inclusion studies utilize the ultra-highresolutionsubsystem with a 225 kV microfocal X-raysource and an image intensifier detector sampled bya 1024 X 1024 CCD video camera to image samplesfrom 3 to 70 mm in diameter at slice thicknessesdown to 10’s or 1’s of µm. The X-ray source is polychromatic,producing X-rays over a continuum ofenergies from about 30 keV up to the operatingvoltage.HRXCT allows examination of the 3-D locationand shape of inclusions with regard to crystalgeometries (Fig. 1) as an aid in evaluating primaryvs. secondary origin, in preparation for conventionalheating and freezing studies. As the method is nondestructive,it allows examination of fluid inclusionswithin unique samples for which destructive studiesare undesirable. HRXCT can produce valid results forunstable minerals for which heating during samplepreparation or during conventional homogenizationmeasurements might produce questionable resultsdue to fluid inclusion stretching. Precise determinationof the volumes of the vapor phase and the fluidinclusion allows the calculation of an “homogenizationtemperature” that is comparable to those determinedfrom conventional homogenization measurements.Fig. 1. HRXCT slices through a quartz crystal with atwo-phase fluid inclusion. (a) inclusion containingliquid; (b) same inclusion with vapor bubble visible.Resolution limitations of current HRXCTsystems only allow for reliable measurement ofmultiple phases in relatively large fluid inclusions(≥0.1 mm 3 ), but the distribution of much smallerinclusions (

P26European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 184Femtosecond lasers in fluid inclusion analysis:Overcoming metastable phase statesKrüger, Yves*, Stoller, Patrick**, Ricka, Jaro** and Frenz, Martin***LFA – Labor für Fluideinschluss-Analytik, Cäcilienrain 3, Bern, 3007 Switzerland**Institut für angewandte Physik, Universität Bern, Sidlerstrasse 5, Bern, 3012 SwitzerlandMetastable phase states in fluid inclusions arecharacteristic features of microthermometricmeasurements, and they can be extremely helpful forprecise temperature determination of phasetransitions if these cannot be observed directly. Thetemperature cycling method makes use of thetemperature gap between the disappearance and thenucleation of phases due to such metastable phasestates. On the other hand, metastability can alsocause analytical problems when nucleation of, forexample, the vapour bubble, ice or salt hydrates orsalt crystals in supersaturated brines fails to occurand thus prevents microthermometric measu rements.We have developed a new method to overcomemetastable phase states in fluid inclusions usingsingle femtosecond laser pulses. The setup consistsof an amplified Ti:sapphire laser (800 nm) with anominal maximum output pulse energy of 4 µJ and afull-width at half-maximum pulse duration of around330 fs that is coupled into an upright microscope andfocused onto the sample by a conventional 100x/0.80long working distance objective. Additionally, themicroscope is equipped with a heating/freezing stage.This arrangement allows us to repeatedly and reliablyinduce phase nucleation in selected metastable fluidinclusions at different temperatures under microscopicobservation. Subsequent microthermometric measurementscan be performed without moving the sample,making it suitable for routine applications.We applied this new technique to aqueousone-phase (all liquid) inclusions down to 1 µm in sizein quartz, calcite (Fig. 1) and other host minerals toinduce bubble nucleation without causing any irreversiblestretching of the inclusions, and we wereable to determine Th-values as low as 6.1 °C. Themethod was also applied to induce bubble nucleationin the presence of ice in order to determine icemelting temperatures under equilibrium conditions,and to induce nucleation of salt crystals (e.g. halite orhylvite) in supersaturated brines as well as to inducenucleation of ice and salt hydrates at low temperatures.The method of femtosecond laser inducedphase nucleation solves a fundamental problem influid inclusion research and opens the field of lowtemperature environments (4 to 100 °C) to fluidinclusion investigations.Fig. 1. Laser induced bubble nucleation in a primary metastable aqueous one-phase inclusion in calcite atroom temperature. (a) and (b) show the one-phase inclusion and the position of the laser spot before, (c)and (d), after the laser pulse and nucleation of the vapour bubble. (c) and (d) show the thermodynamicallystable phase state at room temperature. Th was determined to be 63.8 °C. (L = liquid phase, V = vapourphase).184

P27European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 186LA-ICP-MS analysis of inclusions: Improved data reduction capabilitiesAllan, Murray M.**, Guillong, Marcel*, Meier, Dimitri*, Hanley, Jacob*, Heinrich, Christoph A.*, Yardley, BruceW.D.*** Department of Earth Sciences, Swiss Federal Institute of Technology, ETH Zürich, Switzerland** School of Earth and Environment, University of Leeds, Leeds, U.K.In this contribution we show a new softwaretool based on MatLab, to reduce data from laserablation inductively coupled plasma massspectrometry (LA-ICP-MS). The software was initiallydesigned at University of Leeds (Allan et al., 2005)and recently improved by collaboration with ETHZürich, specifically for the reduction of melt and fluidinclusion analysis. Special care was taken for thevisualization possibilities of the time dependentsignals. A zoom function and a user selection ofplotted elements are implemented. Integrationintervals are set easily by click and drag. Alternativelyintervals can be entered as the time directly (Figure1).Different quantification approaches for boththe host and the inclusion are implemented: Internalstandard, total oxides and wt% NaCl equivalent withmass or charge balanced correction for salts otherthan NaCl.For the correction of the inclusion signal fromthe host signal, several features are available. It ispossible to choose from the same signal differentintegrals for inclusion and host (matrix). It is alsopossible to choose the host signal from a differentablation. For the matrix subtraction a secondconstraint is needed and can it be chosen from:matrix only tracer, 2 nd internal standard or anequation.Other features were implemented, including adrift correction that can be either in integer timepoints or in real time. A routine to find and removespikes manually is very helpful due to a graphicalinterface.The quantification approaches was taken fromHalter et al. (2002), which deals with the generalcase of partially common elements in host mineraland inclusion, as introduced for melt inclusions incomplex igneous phenocrysts. A range of assumptionsfor internal standardization and host/inclusiondeconvolution can be chosen. Results are reportedand saved to a file readable by excel for further datainterpretation and presentation. Individual projectscan be saved and opened later to change settings.Due to the use of MatLab the program coderemains available for all users and additional features,changes and customization remains possible.However, the MatLab software packet has to beinstalled on every computer used for data reduction.Fig. 1. Graphical interface for the signal integrationREFERENCESAllan M., Yardley B., Forbes L., Shmulovich K.,Banks D., Shepherd T. (2005) Am. Min. 90: 1767-1775Halter W., Pettke T., Heinrich C., Rothen-Rutishauser B. (2002) Chem. Geol. 183: 63-86186

P28European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 188Application of Femtosecond Laser Ablation ICP-MS of fluid inclusionsto the study of ore depositsCourtieu, Clément*, Guillaume, Damien*, Salvi, Stefano* and Freydier, Rémi**LMTG, Université de Toulouse, CNRS, IRD, OMP, 14 Av. E. Belin, F-31400 Toulouse, FranceLA-ICP-MS is now a commonly used analyticaltechnique in the study of fluid inclusions of oredeposits. Unlike typical nanosecond UV laser ablationsystems (ArF or Nd:YAG), the new femtosecondablation systems can provide athermic ablations.One advantage of this is a lower risk of fluid loss dueto thermal shock during opening of the inclusion. Totest this technique, we studies fluid inclusions hostedin quartz from the Trimouns talc-chlorite deposit(Ariège, France).In our experiments, we used a femtosecond Ti:Sapphire 800 nm laser ablation system, following theanalytical protocol outlined by Heinrich et al. (2003).Before ablating the inclusions, we performedpetrographic and microthermometric studies andcalculated Na concentrations to be used as internalstandard. For the LA-ICP-MS analyses we used thefemtosecond laser and an Elan 6000 ICP-MS, withNIST SRM 610 as external standard. Figure 1 is theintegrated signal of a 60µm diameter three-phasefluid inclusion (gas, liquid, NaCl solid). It shows thethree main parts of the signal: ICP-MS noise, signalof the host crystal (pure quartz), and fluid from theinclusion.We could measure the concentration of a widerange of elements within the fluid, including majorcations and anions (e.g., Na, Ca, K, Cl) and minorelements such as Li, Mg, and REE (La, Nd).Repeatability of NIST 610 data were 95% for everyelement studied, except for K (80%) and Cl (50%).We were able to measure a very large range ofconcentrations within a single analysis: from 200,000ppm for major elements like Ca to about 5 ppm forthe Rare-Earth Elements (La).This study validates the use of a femtosecondlaser ablation system used for LA-ICP-MS analysis offluid inclusions and its significance to the study of oredeposits.REFERENCESHeinrich C. A., Pettke T., Halter W. E., Aigner-TorresM., Audetat A., Gunther D., Hattendorf B., BleinerD., Guillong M., and Horn I. (2003) Geochimica etCosmochimica Acta 67: 3473-3497.Figure 1: Typical time-resolved LA-ICP-MS spectra of a quarz-hosted REE-fluid inclusion.188

P29European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 190Advantages of an improved high performance 193 nm laser ablationsystem for the direct analysis of fluid inclusionsKrause, Petra*, Brune, Jan**, Fricker, Matthias***, Günther, Detlef **** CETAC Technologies, 242 Bamburgh Avenue, South Shields, NE33 3HX, UK,** Coherent GmbH, Hans-Böckler-Str. 12, 37079 Goettingen, Germany***ETH Zürich, Institute for Inorganic Chemistry, ETH Hönggerberg, HCl, Zürich, SwitzerlandLaser Ablation ICP-MS has come a long waysince its introduction in the mid-eighties. Whereasthe first generation of laser systems used infraredlasers, modern systems are using UV-lasers atdifferent wavelengths between 266 nm and 193 nm.Quantitative analyses of fluid and meltinclusions in various matrices have been successfulcarried out since the introduction of the 193 nmexcimer laser ablation system (ArF Excimer) [Audetatet al. 1998; Ulrich 1999; Heinrich et al. 2003; Pettkeet al. 2006]. Examples of controlled opening of fluidinclusions to access the entire content of a fluidinclusions have been demonstrated using variousspot sizes and considered as a necessary prerequisitedue to the possible splashing andconsequently loss of liquid [Günther et al. 1998].However, in order to enhance performanceespecially for challenging applications such as theanalysis of fluid inclusions in quartz and fluorites, theGeoLas System has been modified during the lastfew years. A redesign of the GeoLas Pro system withnew homogenizer arrays in combination with a highperformance petrographic Microscope (OlympusBX51TRF) and improved software features havebeen implemented. The current system allowsadjusting fluencies up to 45 J/cm2, which providesufficient energy densities to ablate quartz and othermaterials.This poster will describe the new designfeatures of the GeoLas Pro System and will showseveral examples for direct elemental analysis in fluidinclusions of different materials. New softwarefeatures in context with fluid inclusion analysis will bediscussed.Examples for a “crack-free” ablation ofinclusions in fluorite and other materials will beshown and the detection limits achievable usingdirect ablation of inclusions and step-wise opening ofinclusions will be compared.REFERENCESAudétat, A., Günther, D., Heinrich, C.A., Science,1998, Vol. 279, 2091-2094.Ulrich, T., Günther, D., Heinrich, C.A., Nature, 1999,399, 676-679.Heinrich, C.A., Pettke, T., Halter, W., Aigner, M.,Audetat, A., Günther, D., Hattendorf, B., Bleiner, D.,Guillong, M., Horn, I. Geochim Cosmochim. Acta,2003, Vol. 67, 3473-3497.Pettke, T., Mineralogical Association of CanadaShort Course Series 36 “Melt inclusions in plutonicrocks”, Webster, J.D: (ed), Montreal, Quebec, May15-17, 2006, 51-80.Günther D., Audetat A., Frischknecht R., HeinrichC.A., J. Anal. Spectr., 1998, Vol. 13, 263–270.190

P30European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 192Validation of 213 nm Laser Ablation Inductively Coupled Plasma MassSpectrometry (LA-ICP-MS) for Quantitative Single Fluid InclusionAnalysis: A Calibration StudyVry, Victoria*, Wilkinson, Jamie* and Jeffries, Teresa*** Department of Earth Science and Engineering, Imperial College London, South Kensington Campus,Exhibition Road, London, SW7 2AZ** Department of Mineralogy, The Natural History Museum, Cromwell Road, London, SW7 5BDLA-ICP-MS is a state-of-the-art microanalyticaltechnique that gives excellent spatial resolution andthe capability to determine major, minor and traceelement concentrations in solid samples down to(sub) ppm levels. LA-ICP-MS has been applied to awide range of geological materials (e.g. meteorites,minerals, fossils) and in recent years has beendeveloped for the quantitative analysis of single fluidinclusions trapped within minerals such as quartz.Fluid inclusions pose a significant challengefor calibration methods due to the unusual solid-fluidmatrix composition. For effective calibration, ablation,transport and detection of material from both thestandard and the unknown must be similar and inorder to achieve this, a matrix matched standard istypically required. Currently it is common practice toexternally calibrate fluid inclusions using a combinationof readily available, well characterised standardglasses (e.g. NIST 612). However, the validity of thisapproach has only been confirmed for a limited suiteof elements and the possibility of significant biasexists as a result of contrasting sample and standardmatrix ablation characteristics.This study aims to investigate direct liquidablation as a calibration method for 213 nm LA-ICP-MS analysis using synthetic inclusions calibrated withmulti-element aqueous solutions contained in microwells.Analyses are being carried out at the NaturalHistory Museum, London, using a New WaveUP213AI, 213 nm aperture laser ablation systemlinked to a Thermo Element PlasmaQuad 3 ICP-MS.A range of concentrations of standard solution will beanalysed in order to investigate possible non-linearityin sensitivity and concentration-related fractionationeffects. The goal is to better matrix-match the standardmaterial to that of the fluid inclusions in order toimprove accuracy and reproducibility.192

P31European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 194ExLAM 2000: Excel VBA application for processing of transient signalsfrom laser ablation (LA-ICP-MS) of fluid inclusions and solid phasesZacharias, Jiri* and Wilkinson, Jamie***Institute of Geochemistry, Mineralogy and Mineral Resources, Charles University in Prague, Albertov 6,Prague, 12843 Czech Republic**Dept. of Earth Science and Engineering, Imperial College London, South Kensington, London, SW7 2AZ,UKLaser ablation inductively coupled plasmamass spectrometry (LA-ICP-MS) has become awidely used analytical technique for establishingchemical composition not only of mineral phases, butalso of fluid or solid inclusions trapped in minerals. Inaddition to commercially available software for analyteconcentration calculation, we present a new userfriendlyapplication, for Excel 2000 and higher,developed especially for fluid inclusion and mineralanalyses.ExLAM 2000 is written in Visual Basic forApplications and designed for the processing ofhomogeneous (e.g. mineral) and/or mixed (solid orfluid inclusions trapped in a homogeneous mineralphase) signals from LA-ICP-MS systems.Mathematical formulae included in the code arebased on those derived by Longerich et al., (1996),Halter et al. (2002) and Heinrich et al., (2003), withsome minor modifications.For users, ExLAM 2000 offers the followingbenefits: 1) well known Excel environment and hencea possibility to modify outputs (data and graphs) asneeded; 2) simultaneous data entry [e.g. setting therange of intervals (slices) for blank, mineral andinclusion ablation] and interactive graph viewingmode; 3) multiple calculations with the same samplecan be easily done by copying and modification ofonce defined ablation intervals; 4) data processingcan be stopped any time, data saved and startedagain from any point; 5) set of predefined graphs andplotting options; 6) easy editing of spikes; 7) the VBAExLAM 2000 code is an integral part of each data file,i.e., no special add-in installation is necessary toview/recalculate data on another computer; 8) nocosts (freeware software).ExLAM 2000 is designed for a mixed set ofmax. 30 samples and standards ablated during oneanalytical session. The total number of processedisotopes is limited to 77. Several types of instrumentaldrift corrections are possible. As many as 237standards can be stored and managed in the referencelibrary of standards. Concentrations of isotope internalstandards can be entered in ppm, wt.%, or in wt.%eq. NaCl.This research was supported by the CzechScience Foundation, project GACR: 205/06/0702and by a grant of the Ministry of Education to theFaculty of Science, Charles University(MSM0021620855).REFERENCESHalter, W.E., Pettke T., Heinrich C.A., Rothen-Rutishauser B. (2002) Chem. Geol. 183: 63-86Heinrich C.A., Pettke, T., Halter, W.E., et al. (2003)Geochim. Cosmochim. Acta. 67: 3473-3496Longerich H.P., Jackson S.E., Günther D. (1996) J.Anal. Atom. Spectrometry. 11: 899-904194

P32European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 196The cesium-rich melt from quartz-pollucite lens, Vasin Myl’k pegmatite,Kola peninsula, RussiaBadanina, Elena V. C.*, Gordienko, Vladimir V.*, Thomas, Rainer** and Syritso, Ljudmila F.**Department of Geochemistry, State University of St.-Petersburg, University emb. 7/9, St.-Petersburg,199034 Russia**GeoForschungsZentrum Potsdam, Telegrafenberg, Potsdam, 14473 GermanyHere we present new melt inclusions data on aunique Cs-rich zone in a pegmatite body, Vasin Myl’kon Kola Peninsula, N-W Russia. The lens is composedof pollucite-quartz intergrowth. The origin of thepollucite-quartz mineral assemblage is controversial.For example, it was proposed to represent adecomposed solid solution of a pre-existing SiO 2-richpollucite variety (Gordienko, 1996).The fact that quartz contains primary meltinclusions (MI) implies that the quartz-polluciteassemblage is magmatic. Crystallized melt inclusionsrandomly occur in 1-5 mm drop-shaped quartzgrains. Drop-like grains of quartz contain melt, crystal(CI) and fluid (FI) inclusions. MI have oval, roundedshapes, and are from 10 to 200 µm in size.Daughter crystal aggregate of the MI dominatesover the fluid phase (the latter comprises around10 vol%), and consists of pollucite, K-feldspar andlepidolite. CI are represented by individual grains ofpollucite and Rb-rich (up to 7.9 wt.% Rb 2O) K-feldspar. CI are from 5 to 30 µm in size. FI are of twotypes. Smaller (1-5 micron) single-phase FI spatiallyassociate with MI are possibly syngenetic with them.Larger (up to 20 microns) two-phase L+V inclusionsare randomly distributed in quartz grains.Homogenization experiments on MI in rapid-quenchcold-seal pressure vessels at P = 200 MPa and T =715 °C resulted in homogeneous glasses, sometimescontaining relicts of mica and a gas bubble.Compositions of the quenched glasses were studiedby Cameca SX-50 electron microprobe at the GFZPotsdam.The average composition of the homogenizedglassy inclusions is granitic (64.1 wt.% SiO 2and14.8 wt. % Al 2O 3) with Na prevailing over K (2.9 wt.%Na 2O vs. 1.6 wt.% K 2O), and extremely high in Rb (upto 1.2 wt.% Rb 2O). At the same time, the compositionof the MI differs from the bulk composition of thewhole pegmatite body. However, the concentrationsof SiO 2, Al 2O 3, Na 2O, K 2O, Rb 2O in the average MIare close to those in the quartz-pollucite lenscalculated by Gordienko (1996).In accordance with the Cs enrichment of thelens, MI are high in Cs (up to 4.3 wt.% Cs 2O). HighCs contents compare well with MI of the Malkhanypegmatite field in Transbaikalia (up to 6.45 wt.%Cs 2O in the Oreshnaya pegmatite veins). Notably,pollucite is completely absent from the vast majorityof Malkhany pegmatites. The absence of pollucitefrom Malkhany probably arises from Cs dissipation inlepidolite. Notably, the concentrations of fluorine arevery similar in both geographic localities (up to 2 wt.%F). Also, MI inclusions from the pollucite-quartz lensof the Vasin Myl’k pegmatite are unexpectedly high inW (up to 0.31 wt.% WO 3), although no W mineralshave ever been reported in the pegmatite.The study is supported by grants from theRFBR (No. 05-05-64878), CDRF and GFZ Potsdam.REFERENCESGordienko V.V. (1996) SPb University edition. 270 p.196

P33European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 198Fluid and solid inclusion evidence for late-stage mobility of zirconium,titanium and REE in carbonatite systemsDowman, Emma * Rankin, Andrew* and Wall, Frances*** Centre for Earth and Environmental Science Research, Kingston University, Surrey KT1 2EE, UK**Dept. Mineralogy, Natural History Museum, London SW7 5BD, UKCarbonatites are often associated with anumber of economically-important rare metal deposits,including the bulk of the world’s REE resources.In order to investigate further the role of late-stagecarbonatitic fluids in the genesis of these deposits,studies have been carried out on REE-bearingcarbonatites with well-developed fenitised aureolesfrom Chilwa Island and Kangankunde in Malawi.Mineralogical and fluid inclusion studies werecarried out on fenitised granite-gneiss country rockssurrounding these two complexes. These fenitescharacteristically contain alteration assemblages ofaegirine-augite, sodium-rich amphiboles and turbidfeldspar. The fenitisation process is most intense,and pervasive, close to the intrusive carbonatitecentres. Quartz is usually destroyed during fenitisation,but where the process has been less intense, furtherfrom these centres, the quartz is preserved and partlyrecrystallised. These recrystallised portions providethe opportunity of studying remnants of the originalfenitising, carbonatite-derived fluids.The recrystallised quartz has trapped typicalportions of carbonatitic fluids as mostly secondaryinclusions (c.2-20 microns in size), together withtraces of rare metal mineralisation as evidenced bythe presence of rutile, zircon, apatite, barites andlead (cerussite?) as solid inclusions (c. 100 microns).These traces are closely associated with complexCO 2-rich and alkali chloride-carbonate-bearing brinesin which nahcolite (NaHCO 3), halite, calcite and theREE-carbonate phase, burbankite are commondaughter minerals. Such assemblages are characteristicof late-stage carbonatitic fluids reported frommineralised carbonatite complexes (see review byRankin, 2005).Rutile and fluorapatite are also present astrapped solids within these inclusions, attesting totheir co-evality with the trace mineralization.The presence of late-stage Ti, Zr, Pb and P-mineralisation derived from carbonatitic fluids atsome distance from carbonatite intrusive centressupports previous work on the transport capabilitiesof such fluids (Rankin, 2005). Furthermore, the occurrenceof REE daughter minerals, such as burbankitesuggests that REE-mineralisation, though commonwithin the carbonatites themselves, may also extendfurther out into the country rocks by the action ofthese late-stage ‘carbothermal’ fluids.ABFig 1. A. CO 2-rich brine inclusion with burbankitedaughter mineral (field of view 20 microns) B. Zirconinclusions (dark phase) attached to colourlessfluorapatite crystals in recrystallised quartz (field ofview 80 microns).REFERENCERankin A.H. 2005. Carbonatite-associated RareMetal deposits: Composition and evolution of oreformingfluids – the fluid inclusion evidence.. In:Samson, I. and Linnen, R (eds). Rare ElementGeochemistry and Ore Deposits. Mineralog. Assoc.Canada Spec. Pub., Short course notes v.17, 299-314).198

P34European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 200Fluids associated with episyenitization of the Variscan post-tectonicGerês granite, northern PortugalJaques, Luís*, Noronha, Fernando* / ** and Bobos, Iuliu* / ***GIMEF- Centro de Geologia, Faculdade de Ciências UP, Rua do Campo Alegre 4169-007 Porto, Portugal**Departamento de Geologia, Faculdade de Ciências UP, Rua do Campo Alegre 4169-007 Porto, PortugalThe episyenitization of granite is a widespreadhydrothermal alteration process characterized byalkaline fluids. The process consists of thedequartzification of the granitic rocks due to circulationof alkaline fluids along fracture systems. This processaffects some granites in the European Variscanchain. In some cases, the process is considered tobe spatially associated with U, Sn-W and Aumineralizations (Cheilletz & Giuliani, 1982; Leroy,1984; Cathelineau, 1986).Episyenitic rocks from the Gerês post-tectonicmassif were firstly characterized by Ávila-Martins(1972). Recently, similar occurrences were observedand studied in the Guarda region (Jaques et al.,2005). The Gerês granite shows porphyric andcoarse to medium texture. Episyenitic bodies formcolumnar elongated structures, which arepredominantly controlled by N-S and NE-SW brittlestructures. Along these favourable channels, fluidcirculation has promoted quartz leaching accompaniedby Na + metasomatism, generating the albitization ofmagmatic feldspar. Later, remobilization of Ca +implied a late hydrothermal event, characterized byan epidotization process. This study is focused onsecondary FI occurring as intergranular planes (FIP)in the magmatic quartz from the contact limit betweengranite and episyenitic rocks. We also studied primaryand pseudo-secondary FI from later quartz grains,infilling cavities from altered rocks. FI present in FIPare aqueous, two-phase belonging to the H 2O-NaClsystem. Microthermometric results are similar in FIPwith N-S and NE-SW trends. Tmice varies between–0.1 and –6.1 ºC, which corresponds to lowersalinities (0.18 to 9.34 wt.% eq. NaCl) whereas Thvaries between 148 and 233 ºC. The Th-Tmicerelation indicates a decreasing of Th with salinity ofthe fluid. Primary and/or pseudo-secondary FI presentin later quartz from cavities in episyenites are alsoaqueous, two-phase, H 2O-NaCl fluids. These areinterpreted as more saline with hydrohalite. TmHhvaries from -0.7 to +0.1 ºC. Th ranges from 171 to279 ºC with a mode around 220 ºC. In both cases, novolatile species were detected by micro-Ramananalysis.These results show evidence for the existenceof two main aqueous hydrothermal events leading tothe alteration of the Gerês granite, revealing differentP-T fluid conditions. Preceding FI studies of VariscanW mineralizations spatially associated with the Gerêsgranite indicate temperatures from 290 to 330 ºC anda maximum lithostatic pressure in the interval from 65to 100 MPa (Noronha, 1984). However, late to post-Variscan NNE quartz veins exhibit hypersalineaqueous fluids at P-T conditions lower than 35 MPaand 250 ºC (Guedes & Noronha, 2002). Fieldobservations support that the episyenitization isyounger than the W mineralizations and that it occursafter an epirogenic event. The maximum temperatureinterval expected for the global paleofluid migrationrelated to episyenitization of the Gerês granite mayhave varied between 180 and 300 ºC. A lateralteration stage, corresponding to precipitation ofquartz infilling cavities, is characterized by pressurevalues lower than 50 MPa, under a hydrostaticregime and T below 250 ºC.REFERENCESÁvila-Martins, J. (1972) Pub. Lab. Min. Geo. UP. 83:26.Cathelineau M. (1986) J. Petrol. 27: 945-965.Cheilletz A., Giuliani G. (1982) M. Depos.17: 387-400.Guedes A. , Noronha, F. (2002) Com.IGM, 89: 97-104Jaques L. et al. (2005) XVIII ECROFI – Siena.Leroy J. (1984) Min. Dep. 19: 26-35.Noronha F. (1984) – Bul. Miner.107:273-284.200

P35European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 202Phase composition of melt inclusions in monticellite and niocalite fromcarbonatites of the Oka complex (Quebec, Canada): confirmation ofsilicate–carbonate liquid immiscibilitySokolov, Stanislav V.All-Russian Institute of Míneral Resources (VIMS), Staromonetnyi per. 31, Moscow, 119017 RussiaAccording to modern conceptions, carbonatitemelts could be the products of liquid differentiation ofcarbonatized alkaline magmas. Evidence that thecarbonatites of the Oka complex formed in thismanner is given by Treiman and Essene (1985).These geologic criteria are supported by experimentalresults regarding immiscibility in melilitite-carbonatitesystems (Kjarsgaard and Hamilton, 1989) andsynchronous trapping of compositionally diverseinclusions by minerals crystallizing from layeredmelts (Romanchev et al., 1972).We have studied melt inclusions in monticelliteand niocalite from carbonatites of the Oka complex.Small (up to 3-5 mm) short-prismatic crystals ofmonticellite and smaller (up to 2 mm), accessoryprismatic crystals of niocalite form irregularimpregnations in the calcitic matrix. Primary inclusionsin both studied minerals have subprismatic habitsand sizes up to 50-60 µm in length. The inclusioncavities are filled with polyphase microcrystallineaggregates (90-95 vol.%) and interstitialheterogeneous (gas + liquid) fluids.Investigation of the melt inclusions by electronmicroprobe revealed marked differences in theirphase compositions. Three types of inclusions werefound in monticellite: (I) silicate type – Mn-monticellite,diopside, phlogopite, magnetite, calcite, FeS ss; (II)silicate-carbonate type – Mn-monticellite, diopside,magnetite, calcite, (Na-Ca)-carbonate, (K-Na-Ca)-sulphate-carbonate; (III) carbonate type – Femonticellite,magnetite, apatite, calcite, (Na-Ca)-phosphate-carbonate, (K-Na-Ca)-sulphatecarbonate,(Na-Ca±K)-carbonate. Niocalite containstwo inclusion types: (I) silicate type – diopside,andradite, phlogopite, melilite, monticellite, magnetite,portlandite, calcite; (II) silicate-carbonate type –diopside (or melilite or monticellite), magnetite,calcite, (K-Na-Ca)-sulphate-carbonate, (Na-Ca±K)-carbonate.Type II inclusions in monticellite correspond tothe free melt and are not accidental mixtures of theendmember liquids (essentially silicate andcarbonate), which were trapped by the host mineralsimultaneously. This interpretation is supported bythe approximately similar ratios within these inclusionsbetween predominant carbonate components andsilicate components. Additional confirmations arebased upon differences in mineral associations andchemical compositions of daughter phases fillingcavities of the various inclusion types: 1) Mnmonticellite(types I and II) is replaced by Femonticellite(type III); 2) phlogopite is absent frominclusions of types II and III and diopside from typeIII; 3) apatite and (Na-Ca)-phosphate-carbonates arepresent only in carbonate inclusions; 4) alkalinecarbonatedaughter phases of type III inclusions arecharacterized by greater compositional variety andare enriched in Na and K compared to the sameminerals in inclusions of type II .The above data provide insight into liquidimmiscibility in calcio-carbonatite melts enriched inalkalies, which originated via layering of carbonatizedalkaline magmas at an earlier evolutionary stage ofthe petrogenetic system. These processes resultedin formation of calcite-bearing melilitolites, calcitemonticellite-diopsiderocks and calcite carbonatitesat the Oka complex.REFERENCESKjarsgaard B., Hamilton D. (1989) In: Carbonatites:genesis and evolution. Ed. K. Bell. London: UnwinHyman. P. 388–404.Romanchev B., Kogarko L., Krigman L. (1972)Geokhimia. 8: 1307-1311 (in Rus.).Treiman A., Essene E. (1985) Am. Miner. 70: 1101-1113.202

P36European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 204Ordovician S-type granite and related pegmatite, Sierra de San Luis,Argentina: a fluid inclusion studySosa, Graciela*, Van den Kerkhof, Alfons**, Lopez de Luchi, Mónica ***, Ortiz Suarez, Ariel ** Departamento Geología, Universidad Nacional San Luis, Argentina** Geoscience Centre of the University of Göttingen, Germany*** CONICET, Instituto de Geocronología y Geología Isotópica, INGEIS, Buenos Aires, ArgentinaOrdovician syn-orogenic garnet-biotitemuscovite-granodiorite,granite, and minor biotitetonalitefrom the Sierra de San Luis, Argentina, areclosely associated with barren internal and externalpegmatites. These S-type granitoids (e.g. La Taperaand Paso del Rey) form meter- to km-scale bodieswithin meta-sedimentary schists. Pegmatites makeup variable volume fractions of the plutonic bodies(internal pegmatite) and also form swarms of externalpegmatites around the plutons. Fluid inclusion andcathodoluminescence studies were performed inorder to correlate the fluid evolution of the granitoidsand pegmatites. Furthermore, the results werecompared with rare metal (Sn-Nb-Ta-Li) pegmatites,which are widespread in the Sierra de San Luis(Sosa et al. 2002).The fluid inclusions in quartz, plagioclase andapatite from the granitoids and internal pegmatitescontain low-salinity aqueous solutes of ca. 3-4 wt.%NaCl-eq. The fluid inclusions form clusters andintragranular trails. Primary inclusions are found in allthe minerals. Decrepitated fluid inclusions decoratedwith halos of tiny fluid inclusions indicate implosiondecrepitationand testify to isobaric cooling. Few melt(glass + vapour) inclusions are preserved in quartz,garnet, zircon, apatite and rutile.In contrast, the fluid inclusions in the externalpegmatites show a large compositional variation,including mixtures of H 2O, CO 2±CH 4and salt: Type I(59%) H 2O-CO 2±CH 4inclusions with ~7 wt.% NaCleq.;Type II (23%) aqueous inclusions with ~7% wt.%NaCl-eq. and no detectable CO 2, and Type III (18%)CO 2±CH 4inclusions with no detectable water. CH 4-concentrations are always

P37European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 206Quantitative fluid inclusion gas analysis and interpretation of quartzhostedfluid inclusions from the Pipeline gold mine, Nevada:Application to a Carlin-type depositBlamey N.J.F.* and Norman, D.I.***Department of Chemistry, National University of Ireland, Galway, Ireland**Department of Earth and Environmental Science, New Mexico Tech, Socorro, New Mexico, USA.Quantitative fluid inclusion (FI) gas analysis bymass spectrometry and its inter-pretation is rare,requiring highly advanced skills. Using quantitativegas analyses in mol % and gas ratios, one can distinguishfluid populations, discriminate fluid sources,identify processes, constrain redox, correct isochors,apply gas geothermometry, and provide the key datafor fluid-rock equilibria modelling.The fluid sources and genesis of Nevada golddeposits are hotly debated. Here we examine quartzhostedfluid inclusions from the Pipeline Mine forwhich we have quantitative gas analysis by the coldcrushfast scan method. Fluid inclusions are invariablyaqueous dominated (Th’s 180-230°C) althoughsporadic carbonic inclusions occur (Th’s 295-323°Cat ~2kbar). Salinities are generally 6-8 eq. wt. %NaCl; some samples are hypersaline with 10-25 eq.wt. % NaCl. Sericite associated with the quartz givesa 40 Ar/ 39 Ar date of 92Ma. For a full description ofPipeline mineralisation, see Blamey et al. (in prep).Fluid Sources: Discrimination diagrams basedon CO 2/CH 4vs N 2/Ar, Ar/He vs N 2/Ar, and N 2-Ar-CH 4diagrams have been developed and used to recognisemagmatic, meteoric, and evolved (basinal) fluids. AtPipeline the quartz FI gases have N 2/Ar ratios rangingfrom 500 to 10,000 thus indicating magmatic volatiles.Process recognition: Boiling, mixing, con densation,and equilibrium are recognised using CO 2/N 2vs total gas (mol%). The quartz FI gas data groupedtogether plot with a positive slope on the CO 2/N 2vstotal gas plot whereas individual samples plot inclusters. This indicates condensation of volatiles didnot occur within the deposit but prior to fluids enteringthe deposit.Redox: We therefore use CH 4, CO 2and H 2(mol%) to calculate the fOand fHat the desired2 2temperature. The fHcan also be ascertained by2multiplying the H 2concentration by Henry’s Lawconstants, provided the H 2content exceeds thedetection limit.Isochor Correction: At Th, the pressure withina FI equals the water vapour pressure plus the partialpressures of each gas. Above Th one must calculatethe water-salt isochor then add the gas partialpressures calculated by multiplying the concentrationand Henry’s Law constants for each gas. We showthat the dissolved gases contribute 400-700 bar atTh.Gas geothermometry: The CO 2-CH 4-H 2gasgeothermometer was established by D’Amore andPanichi for low salinity fluids and also applies to fluidinclusions (Blamey and Norman, 2002). For the H 2Sgeothermometer see Blamey (2006).Fluid-rock equilibria modelling: Solubility ofmetals such as Cu, Zn, Pb, Ag and Au may bemodelled within hydrothermal fluids using both thedissolved salt and gas concentrations, the salts beingconstrained by microthermometry. Metal solubility isinfluenced by aH 2S and in some cases redox. Forexample:Au + H 2S = AuHS + ½H 2At Pipeline ore fluid calculated gold solubility is~200 ppb, principally as Au bisulphide complexes.Quantitative fluid inclusion gas analysis is apowerful yet under-utilised geochemical tool. At Pipeline,ore fluids were derived from condensing magmaticvolatiles and entered the deposit at 300°C and2kbar transporting ~200 ppb Au.REFERENCESBlamey N.J. (2006) Stanford Geotherm. WorkshpBlamey N.J.F., Norman D.I. (2002) StanfordGeotherm. WorkshopBlamey N.J.F. et al. (in prep) GeofluidsD’Amore F., Panichi C. (1980) GCA.Norman, D.I., Blamey N.J.F. (2002) StanfordGeotherm. Workshop206

P38European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 208Degassing and silicate-salt liquid immiscibility as an alternativemechanism of magmatic system evolutionSolovova Irina P.* and Girnis, Andrei**Institute of Geology of Ore Deposits, Petrography, Mineralogy, and Geochemistry, Russian Academy ofSciences, 35 Staromonetny, Moscow, 119017 RussiaThe rapid ascent of extrusive carbonatites andalkaline magmas is usually accompanied bydecompression degassing and loss of volatiles(Woolley and Church, 2005). This results in negligiblefractionation and absence of liquid immiscibilityphenomena. In contrast, the development of magmachambers, where mantle-derived melts may be storedat nearly constant temperatures and pressures,provides conditions for extensive fractionation andliquid immiscibility processes. We considered the twoscenarios of the evolution of volatile-rich alkalinemagmas by the example of (I) alkaline mafic ultramaficcomplexes without carbonatites from Germany(Mahlberg melanephelinites) and Russia (alkalibasalts of the Chukchi Peninsula) and (II) carbonatitebearingalkaline complexes of Italy (Monticcio Lake,Vulture Volcano) and Tajikistan (Dunkeldyk Massif).This study was based on the investigation of melt andfluid inclusions in minerals. Phenocrysts from therocks of group I contain melt and abundant CO 2fluidinclusions (Fig. 1a). Minerals from group II rockscontain melt inclusions only. The homogenizationtemperatures of melt inclusions are 1220-1230 °C forgroup I, and 1200-1240 o C for group II. The silicatemelts encapsulated in inclusions in all the complexesare rich in alkalis and show high agpaitic indexesincreasing in the sequence Vulture (0.5) → Mahlberg(0.6) → Chukchi (0.6) → Dunkeldyk (0.9). The meltsfrom group II rocks show very high contents of volatilecomponents (H 2O, CO 2, S, F, and Cl).Phenocrysts from group I rocks often bearhermetic or partly decrepitated CO 2-dominated fluidinclusions (Fig. 1a). These inclusions show significantvariations in fluid density, which suggests complexcrystallization histories at different depth levels (e.g.,for Mahlberg: 0.8 GPa → 0.5 GPa → 0.3 GPa → 0.1GPa → 2 MPa).Clinopyroxene phenocrysts from the fergusiteof the Dunkeldyk complex contain cogenetic silicateand carbonate melt inclusions (Fig. 1b). The carbonateliquid separated at temperatures of >1200 °C andpressures of at least 0.7 GPa. The separation ofcarbonate liquid and subsequent crystallization ofcarbonates and hydrous minerals prevented magmadegassing up to the latest stages of magmacrystallization.Primary silicate, silicate-carbonate, andcarbonate melt inclusions were also found in lateapatite phenocrysts from the melanephelinite ofVulture Volcano. Such inclusion associations suggesta heterogeneous state of magma during the latestage of crystallization. The investigation of rare CO 2fluid inclusions in clinopyroxene constrained thepressure of apatite crystallization as 0.2 GPa.Thus, it was shown that the magmas ofcarbonatite-free alkaline complexes experiencedextensive decompression degassing en route to thesurface. In contrast, volatile components wereretained in the magmas of carbonatite-bearingcomplexes, and their accumulation resulted eventuallyin the separation of carbonatite melts.Fig. 1. Photomicrographs of (a) a partly decrepitatedCO fluid inclusion in olivine (Mahlberg) and (b) a2melt inclusion with silicate and carbonate liquids andgas bubbles in clinopyroxene (Dunkeldyk).REFERENCESWoolley A.R., Church A.A. (2005) Lithos 85: 1-14208

P39European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 210The composition of magmas in the andesitic volcanoes of Kamchatkaand the Kuril Islands: evidence from inclusions in mineralsBabansky, Andrey D.*, Tolstikh, Mariya L.** and Naumov, Vladimir B.***IGEM RAS, Staromonetny per., 35, Moscow, 119017 Russia**GEOKHI RAS, Kosygina st., 19, Moscow, 117975 RussiaMore than 260 melt inclusions were studied inminerals from 31 samples of andesites from thevolcanoes of the Kuril-Kamchatka island arc(Shiveluch, Bezymyannyi, Avachinskii, Karymskii,Dikii Greben, and Kudryavyi). The inclusions werehomogenized at high temperatures, and quenchedglasses were analyzed with electron and ionmicroprobes. The compositions of melt inclusions inphenocrysts of the andesites vary in SiO 2contentfrom 56 to 80 wt %. The concentrations of Al 2O 3,FeO, MgO, and CaO decrease and those of Na 2Oand K 2O increase with increasing silica content. Themajority (~80%) of glasses in the inclusions showdacitic or rhyolitic compositions. However, thecompositions of the silicic melts (SiO 2> 65 wt %) thatformed the andesites are substantially different fromthose producing dacites and rhyolites in TiO 2, FeO,MgO, CaO, and K 2O contents. Highly potassic (3.8-6.8 wt % K 2O) melts with various SiO 2contents (51.4-77.2 wt %) were found in all the volcanoes studied.This suggests a contribution from a material selectivelyenriched in potassium in the generation of magmaticmelts through the whole region. The concentrationsof volatile components in melts differ from volcano tovolcano. The highest H 2O content was detected inthe melts of Shiveluch (3.0-7.2 wt %) and Avachinskii(4.7-4.8 wt %) volcanoes; and melts with much lessH 2O were trapped by the phenocrysts of Kudryavyi(0.1-2.6 wt %), Dikii Greben (0.4-1.8 wt %), andBezymyannyi (

P40European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 212Melt inclusion in the Bacoli eruption, Campi Flegrei (Italy)Esposito, Rosario* **, De Vivo, Benedetto*, Bodnar, Robert J.**, Lima, A.*, Severs, Matthew**, Rolandi,Giuseppe*, Fedele, Luca* **, Cannatelli, Claudia* ***Dipartimento di Geofisica e Vulcanoligia, Università degli Studi di Napoli Federico II, Via Mezzocannone 8,Napoli, 80134 Italy** Department of Geosciences, Virginia Tech, 4044 Derring Hall, Blacksburg VA, 24061 USACampi Flegrei is one of the largest and longestlivedactive volcanic complexes on Earth. Its proximityto Naples and the towns surrounding Pozzuoli Bay(1.5 million inhabitants) necessitates an understandingof its potential volcanic hazard. The area has beenthe site of volcanic activity for more than 60 ka, andcontains many volcanic centers (cinder cones, tuffrings, calderas) some of which have erupted inhistorical times (Monte Muovo and Solfatara). Someof these eruptions have been extremely violent.This study is part of a larger project to identifygeochemical trends that may help to predict the styleand nature of future eruptions in Campi Flegrei basedon melt inclusion (MI). The geochemistry of themagma associated with different eruptions at CampiFlegrei will be characterized. Eight eruptions thatrange from ca. 19 ka to 1538 AD, and representingdifferent eruptive styles have been selected forstuding.The first of the eight eruptions studied wasfrom the Bacoli eruption. It represents a pyroclasticdeposit formed around 14 ka. The volcanic productswere erupted from vent located along the NeapolitanYellow Tuff caldera (the Averno-Capo Misenoalignment).The bulk rock composition of the eruptiveproducts cannot be determined from all rock analysisbecause the rock has undergone pervasive secondaryzeolitization process and because few outcrops exist.Using Raman spectroscopy, the zeolite mineralphilipsite was detected. Because the bulk rockcomposition has been altered the composition of themagma before eruption was determined buy studyingmelt inclusion in phenocrysts from Bacoli eruption.The phenocrysts present in this rock are sanidine(65%), andesine (15%), salite (15%), biotite (4%),Imenite (1%). MIs were studied in sanidine, andesine,and salite. Several different types of MIs wereobserved in all phases. Some MI cointed only glass,others contained glass plus one or more bubbles,and some cotained glass plus bubbles plus crystals.Results of Laser Ablation-inductively coupled plasmamass spectroscopy (LA-ICPMS) and secondary ionmass spectrometry (SIMS) will be presented.212

P41European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 214Study of plagioclase-hosted silicate melt inclusions from the Paleogenedacite of the Zala Basin, Western HungaryHavancsák, Izabella*, Guzmics, Tibor*, Bali, Eniko** and Szabó, Csaba**Lithosphere Fluid Research Lab, Department of Petrology and Geochemistry, Eötvös University, PazmanyPeter stny. 1/c, Budapest, H-1117 Hungary, (http://lrg.elte.hu)**Bayerisches Geoinstitut, University Bayreuth, Universitätsstraße 30 D-95447 Bayreuth, GermanyWe have studied silicate melt inclusions inPaleogene dacitic rocks from the Zala Basin, WesternHungary. Plagioclase-hosted silicate melt inclusionswere used to estimate the composition of the daciticmagma at a certain stage of crystallization, and tostudy the P/T history of their crystallization.The basement of the Zala Basin is built upmostly by Mesozoic sedimentary formations coveredby Eocene sedimentary sequences (Dubay, 1962). Athick effusive and explosive andesitic-dacitic volcanicsequence, which includes the studied Paleogenedacite, is located in the northern part of the ZalaBasin. In this location the younger Eocene sedimentsintercalate with the oldest members of the volcanicsequence (Benedek et al., 2003)The studied dacite has a phorphyritic texturewith high modal proportion of plagioclase andamphibole phenocrysts. Plagioclase is the dominantphenocryst; the size of the crystals is between 0.5and 5.0 mm. They are euhedral, growth zoned, mostlyfresh, but some of them are slightly altered. Plagioclasephenocrysts host a number of silicate melt in clusions.These inclusions are either trapped randomlyor along zones of the host plagioclase. They havenegative crystal shape, and their size varies between20 and 70 μm. Each of them contains colorlesssilicate glass and a large bubble. Post-entrapmentcrystallization can be observed on the walls of thesilicate melt inclusions.The composition of the silicate glass in meltinclusions has been analyzed by microprobe. Theglass phase has a high SiO 2and K 2O content (up to81.04 wt% and 4.57 wt%, respectively). It is stronglydepleted in other major elements, particularly Al, Ca,Mg and Fe. It is classified as rhyolite based on theTAS nomenclature. This composition differs sig ni fi cantlyfrom the dacitic bulk rock that is SiO 2-64.3 wt%,K 2O-1.96 wt%, Al 2O 3-16.3 wt%, CaO-4.9 wt%, MgO-1.78 wt% and FeO-4.58 wt%, in average. We pro posethat this strong difference between the com po sitionsof the glass of the inclusions and the bulk rock is theresult of significant post-entrapment cry stallization onthe wall of the silicate melt inclusions. This processextracted a portion of the Ca and Al from the melt. Thelow totals (ca. 97 wt%) of electron microprobe analysessuggest that there is a significant amount of volatilesin the glass of the silicate melt inclusions.We have conducted heating experiments tostudy phase equilibria and track phase changes in thesilicate melt inclusions, and to gather indirect infor mationon the crystallizing history of the parental magma.During the heating significant phase tran si tions wereobserved between 840 °C and 1065 °C. The glassstarted to melt at 840 °C exsolving a ‘new fluid phase’.We suggest that this phase is dominantly water basedon the experiments of Papale et al. (2006). The glassmelted completely at approximately 1000 °C. Thehomogenization of the ‘new fluid phase’ into the meltstarted at 1050 °C. The initial bubble, observed atroom temperature, was present during the wholeheating experiment without any visible shape or phasetransitions or interaction with other phases.Based on our results, we outline the followingevolution path for the melt inclusions: During coolingof the melt inclusions an H 2O-rich volatile phaseexsolved from the melt. Plagioclase crystallized onthe wall of the inclusion. This process also loweredthe solubility of volatiles in the melt. At ambienttemperature such an inclusion contains H 2O as a freevolatile phase as well as H 2O which remains dissolvedin the silicate melt and hence remains in the silicateglass after its crystallization. We have calculated 2 to4 wt% H 2O-content for the crystallizing magma usingthe method of Sisson and Grove (1993). We assumethat most of the free volatile phase has diffused outfrom the voids that now only appear to be bubblesand from the melt inclusions or has leaked throughlattice imperfections.REFERENCESDubay, L. (1962) Földtani Közlöny. 15-39.Benedek, K. (2003) Ph.D. thesisPapale, P. et al. (2006) Chemical Geology, 229pp.78-95Sisson, TW., Grove TL. (1993) Contr. Min. Pet. 113pp. 143-166214

P42European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 216New results from the study of silicate melt inclusions in the Bakony-Balaton Highland Volcanic Field, Pannonian Basin, Western HungaryKóthay, Klára *, Sharygin, Victor V.**, Török, Kálmán***, Ntaflos, Theodoros**** and Szabó, Csaba**Lithosphere Fluid Research Lab, Department of Petrology and Geochemistry Eötvös University, Budapest,Pázmány P. stny. 1/C, Budapest, H-1117 Hungary**Institute of Mineralogy and Petrography, Koptyuga pr. 3, Novosibirsk, 630090 Russia***Eötvös L. Geophisical Istitute, Kolumbusz u. 17-23, Budapest, H-1145 Hungary****Center for Earth Sciences, University of Vienna, Althan st. 14, Vienna, A-1090 AustriaIn this paper, we show new results of a studyof silicate melt inclusions hosted in olivine phenocrystsfrom alkali basalt occurring in the Bakony-BalatonHighland Volcanic Field (BBHVF), Pannonian Basin,Western Hungary. We examine three volcanoes ofdifferent ages, but formed under the same postextensionalgeodynamic situation related to evolutionof the Pannonian Basin (Embey-Isztin et al., 1993).The studied areas are Haláp (~3 Ma), Kabhegy(~4.5 Ma) and Hegyestu (~6 Ma, Balogh et al.,1986).Regarding the major element composition ofthe host rock of the three volcanoes, Haláp andKabhegy are very similar showing slightly elevatedSiO 2(49 wt%), and low MgO and alkali content incontrast with basalt of Hegyestu, which has lowerSiO 2content and higher MgO and alkali contents.The silicate melt inclusions (smi) show similarcorrespondence. The modal composition andchemical composition of the smi in Haláp andKabhegy volcanoes show more similarities comparedto smi in Hegyestu. Besides the glass andclinopyroxene, the major mineral phase in themultiphase smi of Hegyestu is rhönite. (Fig. 1). InHaláp and Kabhegy Ti-rich amphibole is a commonphase and some smi contain both amphibole andrhönite. A CO 2bubble, apatite, Al-spinel, sulphideblebs, ilmenite, rutile, anhydrite, and carbonate canalso be found in smi in all the three localities. Ilmeniteis more common in Haláp where the groundmass ofthe basalt also contains numerous ilmenite crystals.Raman analysis of fluid phases of smi inHegyestu and Haláp confirm the results of themicrothermometric data, namely that the bubble ispure CO 2, but in some case small amount of CO andCH 4was also detected next to the principal fluidphase.Microthermometric experiments of smi ofKabhegy are presently underway, but smi of Halápand Hegyestu show slightly different thermometricdata. Based on the homogenization temperatures,our results suggest that the smi of Hegyestu weretrapped at higher temperatures (~1270-1300 ºC) thanthe majority of the smi of Haláp (1220-1270 ºC).Some smi of Haláp that have characteristic zonedspinel grains show elevated homogenizationtemperature. These spinels were probably trappedtogether with the melt droplets.Fig. 1. Typical multiphase silicate melt inclusion inan olivine phenocryst from Kabhegy volcano,BBHVF, Hungary. Cpx = clinopyroxene, Amph =amphibole, Rhön = rhönite, Gl = glass, Bub =bubble, Sulph = sulphideREFERENCESBalogh et al. (1986) Acta Mineralogica-Petrographica, XXVIII: 75-93.Embey-Isztin et al. (1993) Journal of Petrology, 34:317-343216

P43European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 218Composition, volatiles and trace elements of melts from a volcanoplutoniccomplex, Kuramin mountains (middle Tian Shan): Evidencefrom inclusions in quartzNaumov, Vladimir * , Kovalenker, Vladimir** and Rusinov, Vladimir***Vernadsky Institute of Geochemistry and Analytical Chemistry, Kosygina 19, Moscow 119991, Russia**Institute of the Geology of Ore Deposit, Petrography, Mineralogy, and Geochemistry, Staromonetny per.35, Moscow 109017, RussiaA distinct spatial association of ore mineralization(Pb, Zn, Au, Ag, F etc.) with Upper Paleozoic (C 3–P 1) magmatism was revealed by the study of thegeology and the mineralogy of the Angren District(Kuramin Mountains, Middle Tian Shan). Nevertheless,some problems of these genetic associations,especially related to the early and high-temperaturestages, are not solved. Thus, we performedcomprehensive melt inclusion studies which led tothe discovery of two coexisting magmatic melts(silicate melt and chloride melt), and the first resultsof their chemical composition, volatile and traceelements content were obtained.Six samples of granite-porphyries andignimbrites were studied. The quartz in these samplescontains silicate melt inclusions, either uniphase(only glass), biphase (glass and gas) or multiphase(glass, gas and daughter crystals). The glass phaseof one of the samples was found to be completelycrystallized, indicating rather slow cooling of thegranite-porphyry dyke in this locality. The inclusionsvary in size (from 5 to 260 μm, the most frequent sizebeing 20 to 70 μm), and the gaseous phase makesup 4.6 to 9.0 vol.%. The solid daughter phases arehedenbergite, biotite (siderophyllite in chemicalcomposition), magnetite (with 3.7 wt.% TiO 2andenriched in Zn and Cu) and fluorite.The first indication of glass fusion upon heatingis observed at 500 to 700 °C by the appearance ofadditional gas bubbles. Usually the quantity ofbubbles (sometimes up to several dozens orhundreds) is a function of the inclusion size. Uponprogressive heating, bubbles in the melt dissolve,daughter crystals melt, and the inclusions homogenizecompletely at 780 to 1080 °C. The acidic inclusions(SiO 2= 70.5 to 76.7 wt.%) are characterized by highpotassium/sodium ratios (K 2O/Na 2O = 1.3 to 2.3),high fluorine contents (up to 0.9 wt.%), chlorinecontents (up to 0.34 wt.%) and sometimes high watercontents (up to 7.2 wt.%).Melt inclusions of two different chemicalcompositions were found in a quartz sample from thegranite-porphyry: the rarer inclusions are of silicatecomposition whereas most of the inclusions arechloride salts. The salt melt inclusions are usuallylocated within intersecting cracks, and at severallocalities within quartz grains we identified coexistingsilicate and salt inclusions. The latter contain isotropiccrystals of NaCl and KCl. These inclusions furthercontain one or more anisotropic crystals and oreminerals occupying about 2 to 7 vol.%. The fluidphase makes up less than 5 to 10 vol.%. Thehomogenization temperature of the salt melt inclusionswas commonly in the range of 680 to 820 °C, with afew homogenizing at even higher T. Freezing of thehomogeneous inclusions inevitably forms aheterogeneous phase mixture with a separate fluidphase within 1 to 2 sec., this being the most distinctivedifference from the silicate inclusions. Upon heating,the overwhelming majority of salt melt inclusions wasfound to leak before their homogenization, especiallyat temperatures about 570 °C.Six melt inclusions were also analysed by ionmicroprobe.218

P44European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 220Spinel-hosted silicate melt inclusions from the Albanian Ophiolite BeltHavancsák, Izabella*, Koller, Friedrich**, Azbej, Tristan*, Nédli, Zsuzsanna* and Szabó, Csaba**Lithosphere Fluid Research Lab, Department of Petrology and Geochemistry, Eötvös University, PazmanyPeter stny. 1/c, Budapest, H-1117 Hungary, (http://lrg.elte.hu)**Department of Geological Sciences, University of Vienna, Geozentrum, Althanstr. 14, A-1090 Vienna, AustriaMelt inclusions in igneous rocks provide usefulinformation about the evolution of composition andprocesses in a magmatic system at a given stage. Inthis work we have studied spinel-hosted melt inclusionsfrom mafic volcanic rocks in the AlbanianOphiolite Belt. These melt inclusions represent thecomposition of the primary magma, since the hostspinel is one of the earliest crystallizing phases. Themain aim of this work is to study the initial stage ofmagmatic evolution in this igneous system. The sig nificance of this study lies in the fact that numerousquestions are still open regarding the petrogenesis ofmafic magmatites and that such spinel-hostedinclusions have been studied previously only rarely(e.g., Kamenetsky, 1996).The Albanian ophiolites are part of a large NNW-SSE-striking ophiolite zone. This ophiolite belt can bedivided into two parts: a western belt and an easternbelt. The western belt consists of MOR-type maficrocks interlayered with subduction related rocks andvolcanosediments. This belt contains rocks that wereformed in a back-arc basin tectonic en viron ment abovea westwards dipping subduction zone (Saccani et al.,2004, Koller et al., 2006). A part of this belt is theStravaj massif from which the mafic rock samples studiedin the course of this work have been collected.These rocks have porphyritic texture. Phenocrystsare euhedral light green clinopyroxenes andthe groundmass consists of silicate glass andplagioclase and clinopyroxene microcrysts. The clinopyroxenes and the groundmass are strongly altered.The size of the phenocrysts varies between 0.5 and7.0 mm, and they contain spinel inclusions. Spinelsappear as opaque grains in the clinopyroxene phenocrystsand in the groundmass with a grain sizeranging from 100 to 300 μm. These spinels are octahedral, and often show petrographic signs of magmaticresorption and host numerous melt inclusions.These inclusions are isometric and often have anegative crystal shape. Their size ranges from 10 to80 μm, and they are trapped randomly in the hostminerals. The inclusions are multiphase; consistingof glass, clinopyroxene daughter minerals and occasionallysulfide blebs.Compositions of the melt inclusions, melt inclusionphases, bulk rock and host spinel have beenanalyzed by electron microprobe. The bulk com positionof the rocks is characterized by a high MgOcontent (up to 14 wt%) and fairly high concentrationsof compatible elements (Cr: 706 ppm, Ni: 468 ppm).The SiO 2concentration is around 46 wt%, Al 2O 3is 14wt%, CaO is 10.5 wt%, Na 2O is 1.7 wt% and TiO 2is0.7 wt% on average. The spinels are characterizedby high Cr 2O 3and MgO content: the estimated Crnumberis between 0.35 and 0.48, and the Mgnumberis between 0.73 and 0.77. The TiO 2contentis low: 0.23-0.28 wt%. The compositions of the glassin the melt inclusions are: 55.1-64.6 wt% SiO 2, 22.4-30.6 wt% Al 2O 3, 4.8-9.6 wt% CaO, and 7.1-4.4 wt%Na 2O. The pyroxene daughter minerals have 47.7-53.2 wt% SiO 2, 6.8-9.2 wt% Al2O3, 18.5-14.4 wt%CaO, and 15.3-21.0 wt% MgO content.A series of heating experiments were conductedusing the furnace technique to homogenize the inclusionsfollowing the method of Kamenetsky (1996).The purposes of the experiments were to obtainsilicate melt inclusions on which the bulk compositioncan be analyzed and to determine their homogenizationtemperatures. This temperature gives a minimumvalue for the crystallization temperature of the hostspinel crystals. The samples were heated to andquenched from 1200 ±20 ºC to 1240 ±20 ºC. Themelt inclusions homogenized above 1200 ºC. Thecomposition of the homogenized melt inclusionsshows 49-51 wt% SiO 2, 5.5-6 wt% Fe 2O 3, 10-11 wt%MgO, 14.5-16 wt% Al 2O 3, 2-2.4 wt% Na 2O and 12-12.7 wt% CaO. This is comparable with the hostmafic melt composition.REFERENCESKamenetsky, V. (1996) EPSL 142. 479-486.Koller, F., Hoeck, V., Meisel, T., Ionescu, C., OnuziK., Ghega, D. (2006) Tectonic Development of theEastern Mediterranean Region, 260. 267-299Saccani, E., Beccaluva, L., Coltorti, M., Siena,F. (2004) Ofiolithi 29, 75-93220

P45European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 222Melt inclusions in the Kermanshah ophiolitic basaltic rocks, WesternIran (Neotethyan Ophiolite)Ahmadi, Mojtaba**Department of Geology, University of Tehran, PO Box 14155-6455, Tehran, IranIn this study we present our project aboutbasaltic melt inclusions (MI) in Cr-spinel crystals inthe Kermanshah ophiolitic basaltic rocks, located inthe north-western part of Iran and belonging to theNeotethyan Ophiolitc System.Melt inclusions (or magma inclusions) aredroplets of magma that became trapped in mineralsduring crystallization. Accordingly, investigations intoMI may provide insight into a wide range of igneousprocesses. Cr-Spinel and its related MI is one of theinteresting subjects in this regard. Kamenetsky (1996)considered the implications of Cr-spinel melt inclusionsfor MORB parental melts in the FAMOUS area.The samples of this project are some Cr-spinelminerals which are related to three basalt samples (3locations) of the Kermanshah ophiolitic basalts.According to the standard approach to MIinvestigations, this study was done in three stages: 1)crystal separation, 2) homogenization of MI by heatingstage (to 1250 °C) and 3) microprobe analyses.Almost all of these basaltic MI can be classifiedas OFB(MORB) type. These MI are high-Al and high-Na in composition. The MgO composition of MI in oneof the samples is very variable (from ~5% to ~10%).The high MgO content of some MI samples showsthat these MI are the same as the parental melts(Table 1).Table1. Major oxide compositions of some meltinclusions in Cr-spinels in the Keramshah samplesSample SiO 2TiO 2Al 2O 3MgO Na 2OKB1-A 52.67 0.88 16.75 9.41 2.81KB1-B 50.37 1.10 19.42 5.91 3.94K1-62A 49.89 0.86 17.83 9.57 2.90Consideration of three other lines of evidenceis useful in this context:1) Chemical analysis of some additional spinelcrystals: Sample SH5D (crystal) has even higher Alcontent (Al 2O 3up to 44 wt%, Cr# 25). The variabilityof chemical results in each of the samples is veryhigh, for example the variability of Al 2O 3in one sampleis so high that one part of the results is near to thehighest MORB recorded in the world (Al 2O 3: 44%) butanother part (side) of the sample is near to the IAB/MORB boundary (Al 2O 3: ~24%).2) There is a debate on the interpretation of thebulk chemical compositions of sub-alkaline basalticrocks related to the Kermanshah Ophiolite Systembetween Ghazi and Hassanipak (1999) and Ahmadi(2001). The basalts are classified either as membersof the OFB group or belonging to IAB.3) Some spinel compositions are more closelyrelated to IAB than to OFB. These crystals and theirMI have not been studied thoroughly until now.Including the above 3 lines of evidence,together with the documented variability of the MIcompositions, we interpret the source of theKermanshah ophiolitic basalts to be a heterogeneousmantle composition.REFERENCESFrezzotti M.-L.(2001) Lithos 55,273-279Ahmadi M. (2001) MSc.Thesis,Univ.Tehran.205 P.Ghazi,A.M. and Hassanipak,A.A.(1999) J. AsianE.S.17-319-332Kamenetsky V. (1996) EPSL 142. 479-486222

P46European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 224Natrocarbonatite melts of the Bol’shaya Tanga carbonatite complex(eastern Sayan, Russia): evidence from melt inclusionsAndreeva, Irina A., Kovalenko, Vyacheslav I.Institute of Geology of Ore Deposits, Petrography, Mineralogy, and Geochemistry, Russian Academy ofSciences, 35 Staromonetny, Moscow, 119017 RussiaThe Bol’shaya Tagna Massif (BTM) is locatedwithin the eastern Sayan province of ultramaficalkaline rocks and carbonatites. It is an isometricbody, 4 km in diameter. Its concentric ring structure isbuilt up by the following succession of rocks: ijolitemelteigite,nepheline and subalkaline syenites(microclinites), picritic porphyrites, and carbonatites.A conspicuous feature of the BTM is the abundanceof syenites and microclinites and extensive fluoritemineralization coeval with the carbonatites.The sample studied is a fluorite carbonatitecomposed of calcite (60 vol%), fluorite (~30%),potassium feldspar (no more than 5%), pyrite (~2-3%), and barite (no more than 1-2%). The calciteshows significant MnO and FeO contents. Carbonateexsolution into Mn-calcite and kutnahorite (dolomitegroupmineral) is common.Primary melt and cogenetic crystallineinclusions were found in fluorite, potassium feldspar,and pyrite. The crystalline inclusions are carbonates(calcite, Na-Ca carbonate, and kutnagorite), fluorite,potassium feldspar, aegirine, columbite, and pyrite.Some calcite inclusions contain ingrowths ofmanganocolumbite with 11 wt % MnO, 9.5 wt % FeO,and 4.6 wt % TiO 2. The inclusions of Na-Ca carbonatescontain up to 44.6 wt % CaO, 18 wt % Na 2O, and 4.5wt % F. This phase has no analogues among naturalcarbonates and is referred to as Na-Ca fluorcarbonate.Its crystal chemical formula is Na 6(Ca 8.3Mn 0.55, Fe 0.15) 9[CO 3] 7(F 2.5OH 1.5) 4. The calculated H 2O and CO 2contents are 1.31 and 29.66 wt %, respectively, andthe total is 101.09 wt %.Melt inclusions in fluorite are completelycrystallized and contain a deformed gas bubble andvarious daughter carbonate, fluoride, and chlorideminerals. Carbonates (calcite, kutnahorite, Nafluorocarbonate, nyerereite, and burbankite) are themost abundant phases. The compositions of daughtercarbonates are identical to those of crystallineinclusions. Nyerereite and burbankite weredocumented in melt inclusions for the first time.Fluorides in the melt inclusions are represented byfluorite and villiaumite. Halite and sylvite wereidentified among daughter minerals. In general, themineral association observed in the fluorite-hostedmelt inclusions is similar to that of the natrocarbonatitelavas of Oldoinyo Lengai (Tanzania).During thermometric experiments (Linkam TS1500), melting of daughter minerals in the meltinclusions began at 280 ° C, and completehomogenization to a salt melt was observed at 520-525 ° C. Subsequent cooling produced a fine-grainedquench aggregate, which was analyzed on an electronmicroprobe by rastering a beam over the whole areaof inclusions. The composition of the salt melt is richin Na 2O (up to 22 wt %) and contains up to 10 wt %CaO, 7 wt % FeO, 4-5 wt % MnO, 3-8 wt % K 2O, 0.6-0.8 wt % SrO, 0.6 wt % BaO, 1.3 wt % Ce 2O 3, 1.65 wt% F, and 1 wt % Cl.The carbonatite melts from the inclusions beara strong resemblance to the compositions ofnatrocarbonatite lavas from Oldoinyo Lengai Volcano.This similarity is strengthened by the fact that thehomogenization temperatures of melt inclusion (520-525 ° C) are very close to the temperatures of OldoinyoLengai magmas measured during the eruption of1988 (544 ° C).Thus, the BTM carbonatites crystallized froman Na-rich carbonatite magma with high contents ofMn, Fe, Ba, Sr, Ce, F, and Cl. Its physicochemicalcharacteristics were similar to those of the OldoinyoLengai lavas. The difference between the chemicalcompositions of rocks and their parental magmaswas attributed to the post-crystallization removal ofsodium carbonates and chlorides with a fluid phase.224

P47European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 226Phase and chemical composition of melt inclusions in baddeleyite fromcarbonatites of the Kovdor complex (Kola Peninsula, Russia)Sokolov, ov, Stanislav V.* and Chistyakova, Natalya I.**All-Russian Institute of Míneral Resources (VIMS), Staromonetnyi per. 31, Moscow, 119017 RussiaThis report presents the results of our study ofprimary melt inclusions in baddeleyite (ZrO 2),a typicalaccessory mineral of calcite carbonatites in theKovdor complex.Baddeleyite occurs as anhedral grains ofvariable morphology and as prismatic crystals (up to1-2 mm long) that are variably transparent (from lightto dark brown) depending on their color. In calcitematrix, baddeleyite forms segregations or intergrowthswith magnetite, forsterite, green phlogopite, apatite.Host-baddeleyite inclusions were studied firstby optical techniques in polished sections and inindividual crystals. Their genetic type, shape, sizes,and phase composition were determined. Thehomogenization experiments were conducted in aheating stage at temperatures of up to 700 °C and inmuffle furnace at 700-900 °C with 25-50 °C heatingsteps. In the last set of experiments, temperaturewas measured with an accuracy of ±10 °C; thesamples were held at each temperature for no lessthan 20 min and were then quickly quenched in air.Inclusions in baddeleyite are prismatic orrounded, range from 10 to 70 µm long, and containabundant crystalline daughter phases (the presenceof fluid is uncertain). The dark colour of the hostmineral prevents their optical identification.The phase and chemical composition of thetrapped inclusions were determined on an JXA-8100Superprobe electron microprobe equipped with anINCA-400 EDS detector. The standards were naturalminerals of known composition, synthetic compounds,and metals.The unheated crystallized inclusions consist ofthe following minerals: forsterite, magnetite,tetraferriphlogopite, apatite, cyrtolite, and carbonates(calcite, dolomite, Na-Ca-carbonate, Ca-magnesite).This phase association shows that SiO 2, CaO, MgO,Fe, P, alkalis, and Zr were contained in the melt.When the inclusions were heated in a heatingstage, crystalline daughter phases were reliablydetermined to melt at a temperature of about 500 °C,and single large inclusions decrepitated attemperatures above 650 °C. Inclusion homogenizationwas attained in the muffle furnace at temperaturesfrom 775 to 850 °C, and the melting of their wallmaterial was observed only at temperatures exceeding900 ° C.The chemical composition of the homogeneousmelts was determined in inclusions in two baddeleyitecrystals (by spot analyses and by scanning overareas of 95 and 68 µm 2 in two relatively largeinclusions). The averages of the four determinationsare in both cases as follows (in wt%): ZrO 22.70–4.15;SiO 211.15–14.56; Al 2O 3< 0.05; MnO 0.10–0.22;FeO t1.48–2.13; MgO 14.04–14.30; CaO 18.93–19.23; SrO 0.58–0.76; Na 2O 6.42–7.48; K 2O 1.58–2.53; P 2O 50.50–2.00; SO 30.30–0.75; total 61.69–64.25.Melt inclusions in the baddeleyite have acarbonate-silicate composition, are enriched in Ca,Mg, alkalis (Na > K), and have notable contents of Zrand Fe. It should be mentioned that baddeleyite andforsterite coexisting in the carbonatites of the Kovdorcomplex are characterized by a similar qualitativecomposition of their melt inclusions (Veksler et al.,1998; Sokolov et al., 1999) in terms of both theassociation of their daughter phases (with the onlyexception of cyrtolite) and the chemical characteristicsof the trapped melt (except Zr).REFERENCESSokolov S.V., Veksler I.V., Senin V.G. (1999)Petrology. 7: 602-609.Veksler I.V., Nielsen T.F.D., Sokolov S.V. (1998)Jour. Petrol. 39: 2015-2031.226

P48European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 228Metasomatic processes in the mantle beneath the Veneto VolcanicProvince (northern Italy): fluid and melt inclusions evidenceBonelli, Rossana* and Frezzotti, Maria Luce**Dipartimento di Scienze della Terra, Università degli Studi di Siena, Siena, 53100 ItalyTertiary alkali-basalts of the Veneto VolcanicProvince (VVP, SE Alps) contain abundant peridotitexenoliths, representing one of the few localitieswhere the lithospheric mantle beneath Italy can bestudied.Previous studies showed that the peridotitesare depleted harzburgites and lherzolites, reequilibratedunder spinel-facies conditions. Beccaluvaet al. (2001) described a pervasive metasomatismcharacterised by variable LREE-enrichment patterns,due to infiltration of alkali silicate basic melts relatedto the Tertiary volcanism, forming glass pockets andveins (pyrometamorphic textures). More recently,Gasperini et al. (2006) suggested two metasomatcevents: 1) an older one induced by slab-derived materialand characterised by crystallisation of amphiboleand mica; and 2) a more recent alkaline metasomaticevent consistent with the Tertiary volcanism of thearea.We have investigated the petrography, mineralchemistry and fluid and melt inclusions of 17peridotites from VVP in order to constrain P-Tconditions of mantle events, to determine the style ofthe metasomatic reactions, and the compositions ofthe metasomatic agents. The studied rocks showdomi nant protogranular and transitional (intermediatebetween protogranular and porphyroclastic) textures;only one sample shows pyrometamorphic features.They consist of a four–phase assemblage: clearolivine (43-70 % vol.), light brown orthopyroxene(20–42 % vol.), green clinopyroxene (5–15 % vol.)and brown spinel (2–8 % vol.). Clinopyroxene in theprotogranular lherzolites show depleted LREE patterns,while those of transitional rocks are characterisedby spoon-shaped REE patterns (La up to 60times chondrite), and variable enrichments in LILE.Two generations of fluid inclusions (1-30 µm)are recognised: 1) Type A (CO 2-rich fluid) are commonlypresent in orthopyroxene, while seldom observedin clinopyroxene and olivine; 2) Type B (CO 2andCO 2-CO fluids) are present only in orthopyroxene.Type B inclusions may contain very small amphibole(

P49European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 230Silicate melt inclusion study in peridotite xenoliths from PannonianBasin, HungaryHidas, Károly1 , Szabó, Csaba 1 , Guzmics, Tibor 1 , Bali, Eniko 2,1 , Zajacz, Zoltán 3,1 and Kovács, István 4,11Lithosphere Fluid Research Laboratory, Eötvös University, Budapest, Hungary2Bayerisches Geoinstitut, Universität Bayreuth, Germany3Department of Earth Sciences, Institute of Isotope Geochemistry and Mineral Resources, ETH,Switzerland4Research School of Earth Sciences, The Australian National University, Canberra, AustraliaPrimary silicate melt inclusions (SMI) inclinopyroxene (cpx) rims and secondary ones inorthopyroxene (opx) along healed fractures from twoequigranular amphibole-bearing spinel lherzolitexenoliths representing the subcontinental lithosphericmantle (Szigliget, Pannonian Basin, Hungary) havebeen studied. These SMI contain CO 2-bearing fluidphase and silicate glass (Fig. 1) at room temperature.The fluids show lower melting temperature than -56.6°C, indicating presence of other fluid componentsbeside CO 2. Furthermore, homogenization of fluidsinto the liquid phase at low T (in the range between-40 – -53 ° C) suggests high density CO 2–rich fluids.Numerous opx- and cpx-hosted SMI (Fig. 1) revealvarious glass-fluid ratio. We have used the LA-ICPMS technique for trace element composition ofthe bulk SMI. Cpx-hosted SMI have major- and traceelementcomposition extremely similar to that of opxhostedones. Primitive mantle normalized traceelement patterns of the SMI show enrichment inincompatible trace elements (LILE, P and LREE)compared to compatible elements, and also shownegative Hf-anomaly.During high-temperature experiments of cpxhostedSMI, the silicate glass started to melt at 850-900 ° C. At 1150 ° C the glass was completely melted,however the fluid phase was not homogenized intothe melted glass. SMI-cpx boundary at 1150 ° Creveals that some cpx from the host dissolved intothe glass in all runs. At 1200 ° C the cpx-hosted SMIdecrepitated without complete homogenization. Incontrast, the opx-hosted SMI, indicating the samemelting features, did not decrepitate at thistemperature.Fig. 1. Silicate melt inclusions in orthopyroxene inperidotite xenolith from Pannonian Basin, HungaryThe glasses range from the basaltictrachyandesite and andesite to phonolitic, accordingto their major element composition. Trace elementdistributions and the high volatile content of the SMIsuggest that the studied melt, which was trapped asSMI, can be a fractionated crystallization product of amafic magma at mantle T-P conditions. The relativelyhigh fluid content (Fig. 1) permits to assume migrationof these andesitic melts along veins or grainboundaries in the mantle, causing significantmetasomatism on reactive mantle minerals. Thedifferent fluid-glass ratios in the studied SMI indicatea pre entrapment phase separation.230

P50European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 232Petrographic and geochemical study of sulfide melt inclusions in uppermantle xenoliths from Tuva (Southern Siberia)Konc, Zoltan*, Hidas, Károly*, Sharygin, Victor V.** and Szabó, Csaba**Lithosphere Fluid Research Lab, Department of Petrology and Geochemistry, Eötvös University, PazmanyPeter stny. 1/c, Budapest, H-1117 Hungary, (http://lrg.elte.hu)**Institute of Mineralogy and Petrology, Siberian Brunch of Russian Academic of Science, Koptuyga prosp.3, Novosibirsk, 630090, RussiaThe main aim of this work is to report detailedthe petrographic and major-element geochemicalfeatures of sulfide inclusions occurring in uppermantle xenoliths hosted in ~440-435 Ma lamprophyredikes in the Tuva Region (South Siberia). Studyingthe upper mantle sulfide inclusions is importantbecause they originated from and bear informationon the ancient lithospheric upper mantle of theregion. Sulfides in xenoliths and xenocrysts havebeen extensively studied previously (e.g. Lorand,1987; Szabó & Bodnar, 1995), however none ofthose represented the upper mantle of such old age.The studied sulfide inclusions and hostxenoliths were collected in the Tuva Region, which islocated between southern Siberia and northernMongolia in Central Asia. This area represents one ofthe oldest members of the Calenodines, and it hasbeen exposed to tectonic processes from accretion(late Vendian), through collision (Cambrian) totransform faulting (Ordovician) (Vladimirov et al.,2005). The lamprophyre melts formed and broughtup the xenoliths in the last stage of the tectonicperiod dominated by transform faulting.We have started our study by selecting sevenxenoliths of harzburgites, orthopyroxene-richlherzolites, olivine-websterites and orthopyroxeniteswith primary sulfide inclusion content for detailedanalysis.The studied primary sulfide assemblages occuras interstitial phases in between mantle silicates andas phases mainly enclosed in orthopyroxenes. Basedon optical microscopy, X-Ray mapping and ScanningElectron Microscopy (SEM), these primary sulfideassemblages consist mainly of 1 to 4 phases,depending on the orientation and exposure of thesections. The primary sulfide mineral phases arechalcopyrite, pentlandite, pyrite and millerite. Afterthe electron microprobe analysis and mass-balancecalculation, the bulk composition of the studiedinclusions were plotted in the MSS (monosulfide solidsolution) and MSS+L Ni,Cu(monosulfide solid solutionand Ni, Cu-rich liquid) field (above 1000 °C) in theS-Cu-Fe-Ni tetrahedron diagram (Kullerud et al.,1969; Craig & Kullerud, 1969). K D3(equilibrium)values (after Fleet & Stone, 1990) were calculatedfrom the Fe and Ni content of the sulfides and theolivine, which show equilibrium between the sulfidesand the coexisting silicates.Under upper mantle conditions and above1000 °C the sulfide melt is present as monosulfidesolid solution (MSS). The sulfide melt cooled slowlyafter the mantle was sampled and as xenoliths weretransported towards the surface by the lamprophyremagma. The first crystallizing phase was chalcopyritearound 970 °C, followed by pyrite and pentlanditenear 300 °C, whereas the last one was milleritebelow 300 °C. The sulfide inclusions of Tuva xenolithsrepresent Ni-rich, relatively ancient “primitive” sulfidemelts.REFERENCESCraig, J.R. & Kullerud, G. (1969) Magmatic OreDeposits: 344-358.Fleet, M.E. & Stone, W.E. (1990) Contributions toMineralogy and Petrology. 95: 336-342.Kullerud, G., Yund, R.A. & Moh, G.H. (1969)Magmatic Ore Deposits: 323-343.Lorand, J.P. (1987) Lithos. 20: 59-76.Szabó, Cs. & Bodnar, R.J. (1995) Geochemica etCosmochemica Acta. 59: 3917-3927.Vladimirov, V.G., Vladimirov, A.G., Gibsher, A.S.,Travin, A.V., Rudnev, S.N., Shemelina, I.V.,Barabash, N.V. & Savinykh, Y.V. (2005) DokladyEarth Sciences. 405: 1159-1165.232

P51European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 234Changes of oxidation state in lower crustal garnet granulites: the roleof CO 2-rich fluidsDégi, Júlia*, Török, Kálmán**, Kodolányi, János*** and Abart, Rainer*****Dept. of Petrology and Geochemistry, Eötvös University, Pázmány P. stny. 1/c, Budapest, H-1117 Hungary**Eötvös Loránd Geophysical Institute of Hungary, Kolumbusz u. 17-23, H-1145 Budapest, Hungary***University of Bern, Institute of Geological Sciences, Baltzerstr. 1-3, CH-3012 Switzerland****Institute of Geological Sciences, FU-Berlin, Malteserstr. 74-100, Haus N, Berlin, 12249 GermanyWe studied mafic garnet granulite xenoliths(garnet, plagioclase clinopyroxene ± orthopyroxene ±Fe-Ti-oxides ± graphite) from Sabar-hegy andSzentbékkálla (Bakony-Balaton Highland VolcanicField, W-Hungary). They were uplifted from the lowercrust by Pliocene alkali basaltic volcanism. Differentmineral assemblages, which occur in the rock,represent different stages of the crustal evolutionduring the formation of the Pannonian Basin. Thegarnet granulite mineral assemblage represents peakmetamorphic conditions (between 1.0-1.5 GPa and850-1050 o C), which was followed by 100-300 o Ctemperature increase and 0.3-0.7 GPa pressuredecrease (Török et al. 2005). In the studied xenolithswe found indications of two processes, which cannotbe explained by changes in P-T conditions, butrequire changes in oxidation state.Primary fluid inclusions, which were capturedin plagioclase, orthopyroxene and garnet during theformation of the garnet granulite mineral assemblagemainly consist of CO 2, but they contain 5-20% COand sometimes graphite also. This CO 2-CO-C fluidsystem occurs only in lower crustal garnet granulitesfrom the two studied localities. Mantle xenoliths andcrustal xenoliths from other localities in this areacontain pure CO 2or CO 2with 3-8% N 2as primaryinclusions. If we assume, that the latter fluids representthe original fluid composition, the presence of graphitein fluid inclusions from Sabar-hegy and Szentbékkállaindicates a local reduction process in the fluid.According to equilibrium thermodynamic calculations,CO is not stable thermodynamically; neither at theconditions of rock formation, nor at room temperature.It could remain stable only kinetically in the fluid, andcould be also the result of the reduction, since theactivation energy of precipitation of graphite fromCO 2is very high.On the other hand, Fe-Ti-oxides in the rockshow a different process. Two type of ilmenitehematitesolid solution can be found as part of thegarnet granulite mineral assemblage, a homogeneousone and an other containing 20-50 % of exsolvedmagnetite lamellae. The first type has about 65-70 %ilmenite content and may represent original ilmenitewhich was in equilibrium with the garnet granulitemineral assemblage. The second type consist ofilmenite-rich (85-95 % Ilm) hematite-ilmenite solidsolution, and Ti-rich magnetite lamellae (Usp 60-65Mt 35-). The exsolution of Ti-rich magnetite in such high40modal proportion can only be derived from theoxidation of ulvospinel-rich magnetite-ulvospinel solidsolution, which could be also in equilibrium with thegarnet granulite mineral assemblage and the firsttype of Fe-Ti-oxides.We calculated relevant oxygen fugacities byusing PERPLEX (Connolly, 1990; Connolly andCesare, 1993). Values for graphite-saturated CO 2at1.25 GPa between 700-1300 o C are consistently 2-3log units higher than the highest possible oxygenfugacities of the original assemblage where the firsttype of ilmenite was in equilibrium with Usp-richmagnetite. In addition, oxygen fugacities relevant forthe second type of ilmenite in equilibrium withmagnetite lamellae are comparable with the valuesfor graphite saturated fluid at 900 o C. Thus theoxidation of Fe-Ti-oxides could be linked with influx ofCO 2-rich fluids.REFERENCESConnolly JAD. (1990) J. Am. Sci. 290: 666-718.Connolly JAD, Cesare B. (1993) J. Metam. Geol. 11:368-378.Török K, Dégi J, Szép A, Marosi Gy. (2005) Chem.Geol. 223: 93-108.234

P52European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 236Fluid regime of the metamorphism in the Kolvitsa gabbro-anorthositemassif (Northeast Baltic Shield): fluid inclusion dataFonarev, Vyacheslav I.*, Vasyukova, Olga V.* and Vapnik, Yevgeny***Institute of Experimental Mineralogy, Russian Academy of Sciences, Chernogolovka, 142432, Russia(fonarev@iem.ac.ru); **Ben-Gurion University of the Negev, Beer-Sheva 84105, IsraelThe Kolvitsa gabbro-anorthosite massif hasbeen studied previously in detail by mineralthermobarometry (Fonarev and Konilov, 2005). Fivehigh-grade metamorphic events related to theparticular P-T-path of metamorphism were revealed.It is shown that the trapping of several populations offluid inclusions was directly related to these tectonothermalmetamorphic events. The following fluidinclusion types were found in meta-gabbroanorthosite:CO 2-rich and aqueous inclusions arecommon, whereas nitrogen and mixed carbondioxide–aqueous inclusions are rare. CO 2-richinclusions occur in quartz and garnet, whereasaqueous inclusions occur in quartz only. Garnet alsohosts mineral inclusions such as calcite, magnesite,and dolomite, and CO 2inclusions with carbonatephases. There are five types of aqueous inclusions:2- -1) low-salinity or Na-K±SO 4±HCO 3(Aq1), 2) KClrich(Aq2), 3) NaCl-rich (Aq3), 4) MgCl 2-FeCl 3-rich(Aq4), and 5) CaCl 2-rich (Aq5) solutions. The salinityof chlorine-bearing solutions is up to 23 wt.% NaClequiv.Three populations of contemporaneousinclusions, trapped during the main metamorphicevents were revealed: i) CO 2-rich (Th mindown to –36.3 ºC), aqueous (Aq5), rare N 2and mixed CO 2–aqueous; M1 (T≤990 ºC, P≤12.4 kbar); ii) CO 2-rich(Th mindown to –35.3 ºC) and aqueous (Aq1 and Aq4);M2-M3 (750≤T≤913 ºC, 8.6≤P≤11.2 kbar); iii) CO 2-rich (Th mindown to –27.8 ºC) and aqueous (Aq1, Aq3,Aq4, and Aq5), rare N 2; M4 (685≤T≤705 ºC, P=7.75kbar). In comparison with other granulite faciesterranes the studied rocks show numerous aqueousinclusions of different salinity and composition. Itseems likely that small-scale fluid heterogeneitieswere present during metamorphic re-crystallization.Aqueous solutions of mainly chlorine-bearingcomposition were of deep primary magmatic sources.During the metamorphic processes they changedtheir composition as a result of local rock-fluidinteractions. Non-equilibrium rock-fluid reactionsdetermined the sharp gradient of fluid compositionsover a distance of meters and even of micrometers.Thus, small-scale heterogeneity of the fluid wastypical for the high grade metamorphic processes.This agrees very well with ideas on the local characterof metamorphic reactions (Korzhinskii, 1959, 1973).The crystallization of solid carbonate phases (upondecrease of temperature) from such fluids, whichwere modified as well by reactions with their hostmineral, is one of the main reasons for the absenceof aqueous inclusions in garnet. Data obtainedsuggest the existence of a single-phase compositefluid during the first stages of metamorphism. Thisfluid was subjected to phase separation at lowertemperature and pressure with the formation ofseparate CO 2-rich (±H 2O) and aqueous phases. Thefluid inclusion data are in good agreement withtextural-mineral features of the studied rocks. It wasshown earlier (Fonarev and Konilov, 2005) that theserocks were characterized by sharp non-equilibriummetamorphic reactions which mainly depended onwhole-rock chemical composition and the rate ofdeformation.This work has been supported by GrantsRFBR 07-05-00292 and 07-05-00891.REFERENCESFonarev V.I. and Konilov A.N. (2005) Int.Geol.Rev47: 815-850.Korzhinskii D.S. (1959) Physicochemical basis ofthe analysis of the paragenesis of minerals. NewYork: Consultants Bureau.Korzhinskii D.S. (1973) Theoretical principles for theanalyses of mineral parageneses. Moscow: Nauka.P. 288236

P53European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 238Fluid inclusions as indicator of fluid migration in the subducting slab:an example from the eclogites of the Raspas Complex, EcuadorHerms, Petra,* Bakker, Ronald J.,** John, Timm *** and Schenk, Volker **Institut für Geowissenschaften and SFB 574, Universität Kiel, D 24098 Kiel, Germany**Dept Appl. Geosciences & Geophysics, Mineralogy & Petrology, Univ. of Leoben, A 8700 Leoben, Austria***Physics of Geological Processes and SFB 574, University of Oslo, 0316 Oslo, NorwayFluids released by subducting plates play amajor role in mass transport and are responsible formetasomatism and partial melting in the mantlewedge above the subduction zone. Fluid inclusionsprovide valuable information about the fluid which isliberated by dehydration processes from thesubducted slab and which trigger and influencemantle melting. Characterisation of this fluid preservedin fluid inclusions can provide an indication whetherthe components of arc magmatism are predominantlyderived from the altered oceanic crust and/orserpentinite or from subducted sediments. For fluidinclusion investigations with the aims characterisedabove, the Raspas Complex, Ecuador, turned out tobe a suitable target. In this area high-pressure rocksconsisting of eclogite-facies serpentinised peridotitesand associated eclogites, metapelites and blueschistsrepresent an ancient oceanic lithosphere. Peakmetamorphic P-T conditions of 20 kbar and 550-600 °C indicate that the eclogite-facies rocks havebeen subducted to a depth of about 70 km (Gabrieleet al. 2003, Eur. J. Min. 15: 977-989). Primary fluidinclusions in eclogite-facies minerals indicate acontemporaneous formation of the inclusions andtheir host minerals at that depth. Investigations offluid inclusions have shown that aqueous low-salinityfluid inclusions with a constant degree of fill (F= 0.8-0.9), containing CH 4and calcite, are omnipresent indifferent eclogite types and minerals, and thus pointto a homogenous fluid composition in the systemH 2O-NaCl-CH 4+(CO 2) during the eclogite-faciesmetamorphism. The dominance of H 2O in the lowsalinityfluid inclusions indicates a high water activityduring metamorphism. The presence of CH 4inaqueous inclusions and the rare existence ofadditional pure methane-ethane-graphite inclusionsin eclogite-facies zoisite veins, representing ancientfluid pathways, point to reducing conditions. Thehomogeneous fluid composition strongly suggests anexternal source of the fluid infiltrating different rocktypes. A fluid infiltration from an external sourceimplies a continuously generated fluid and a highfluid-rock interaction. According to Spandler et al.,2004 (Chem. Geol., 206: 21-42) the element transferfrom the subducting plate to the mantle wedge doesnot simply occur in response to mineral dehydrationand fluid release from the slab, but it needs a highfluid flow and thus intense fluid-rock interaction. Thismakes the investigated eclogitic rocks of Ecuador toa predestinated case study to show what kind offluids may have the potential to be able to enter themantle wedge. Stable isotope investigations of δ 18 Oshall confirm the external fluid infiltration whichshould result in homogeneous δ 18 O values.In a partly serpentinised peridotite, very smallprimary fluid inclusions have been found inrecrystallised pyroxene. From one of these twophaseinclusions (5μm in size), a Raman spectrumcould be obtained, suggesting the occurrence ofmixed hydrocarbons. Such a fluid composition hasbeen analysed already in mantle-derived rocks liketectonised peridotites in ophiolite sequences andperidotite xenoliths in alkali basalts (Sugisaki andMimura, 1994, Geochim. Cosmochim. Acta, 58:2527-2542). At lower pressures, lighter hydrocarbongases such as CH 4are stable. CH 4-H 2O-rich fluids,however, are typically produced during serpentinisationby seawater reaction with ultramafic material (Kelleyet al., 2005, Science 307: 1428-1434).Deserpentinisation of the underlying oceanic mantlecould thus be a realistic source for liberated H 2O andCH 4. This fluid could infiltrate the overlying eclogitefaciessequences and lead to the observedhomogeneous fluid composition in the analysedrocks. Stable isotope investigations might as wellindicate if the fluid originated from associatedserpentinites or eventually from a sedimentarysource.238

P54European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 240Expulsion of fluids from anatectic melts during decompression of HP/UHP garnet-kyanite gneiss from Pohorje Mts., SloveniaHurai, V.* and Janák, M.Geological Institute, Slovak Academy of Sciences, Dúbravská cesta 9, 850 01 Bratislava, Slovakia*e-mail: vratislav.hurai@savba.skThe fluid composition in metapelite from theHP/UHP metamorphic terrane of Pohorje Mountains,Eastern Alps is reported. The lowermost nappe of thePohorje, belonging to the Austroalpine Unit of theEastern Alps, contains micaschists, gneisses,amphibolites, eclogites and ultramafic rocks(serpentinites and garnet peridotites). The eclogitesand garnet peridotites show ultrahigh-pressuremetamorphism (Janák et al., 2004, 2006) related to aLate Cretaceous continental subduction (Thöni,2006).Garnet porphyroblasts in the kyanite-bearinggneiss hosting the UHP eclogites (~3 GPa and 760–830 °C, Janák et al., 2004) contain graphite-richcores rimmed by graphite-absent margins withclusters of primary fluid inclusions dominated byaqueous liquid (55 vol. %). Consistent phase ratiosindicate trapping of a homogeneous fluid.Microthermometric measurements revealed a CO 2-dominated gas with admixture of methane and lowsalinity aqueous phase (

P55European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 242High temperature melting of biotite in CO 2rich environment andformation of orthopyroxene-garnet-plagioclase rocks in the lower crust:A xenolith example from the Bakony-Balaton Highland Volcanic Field(W-Hungary)Török, Kálmán*, Dégi, Júlia** and Marosi, György****Eötvös Loránd Geophysical Institute of Hungary, Kolumbusz utca 17-23, H-1145 Budapest, Hungary**Department of Petrology and Geochemistry, Eötvös Loránd University, Pázmány Péter sétány 1/C, H-1117Budapest, Hungary***Department of Organic Chemical Technology, Budapest University of Technology and Economics,Muegyetem rakpart 3. H-1111 Budapest, HungaryWe studied two composite mafic granulitexenoliths from Mindszentkálla (Bakony-BalatonHighland Volcanic Field, W-Hungary) in order to findevidence on the partial melting, to infer its P-Tconditions and fluid content during partial melting.The Mi-10 sample is a composite maficgranulite xenolith where a garnet-bearing relativelyfine grained mafic granulite is in contact with coarsergrained garnet-plagioclase fels. At the contact of thetwo rock types an orthopyroxene-garnet-plagioclasebearing granulite was observed with high Ti-biotiterelics in garnets. The garnet-bearing mafic granulitecontains plagioclase, clinopyroxene, orthopyroxene,garnet and accessory rutile. The garnet-plagioclasefels contains garnet, plagioclase and accessoryrutile. Primary, single phase fluid inclusions werefound as clusters in garnets, exclusively at thecontact zone.The Mi-19 sample consists of a garnetplagioclasefels and a garnet-orthopyroxeneplagioclasegranulite which contains accessory rutile,ilmenite and biotite. High Ti-biotite is found exclusivelyas relics mostly in orthopyroxene and subordinatelyin garnet. Small single phase primary fluid inclusionsare found only in orthopyroxene with biotite relics.Secondary trails of single phase fluid inclusions werefound in plagioclase and orthopyroxene.Geothermo-barometry used the orthopyroxenegarnet-plagioclase-quartzend member reactions byTWQ 2.02 (Berman, 1991; Berman & Aranovich,1996) and resulted in identical temperature (990-1030 °C) and pressure (1.2-1.3 GPa) estimates forthe two xenoliths. This temperature corresponds wellwith high Ti-biotite melting experimental results ofNair & Chacko (2002).Fluid inclusions in the two xenoliths reveal littledifference. The primary fluid inclusions trapped ingarnet of the Mi-10 sample are high density CO 2-richwith a small amount of N 2(3-8%, according to Ramanspectroscopy) with T h= -40.3 to -55 °C. and T m= -56.7 to -59.1 °C. Primary fluids trapped in the biotiterelic bearing orthopyroxene in the Mi-10 sample arepure high density CO 2with T h= -28.9 to -34.4 ° C. andT m= -56.6 to -56.8 °C. The purity of the CO 2waschecked with Raman spectroscopy.Although calculated isochores record somewhatlower pressure (around 1 GPa at 1000 °C), texturalrelationships indicate that fluids trapped during thepressure and temperature peak, when dehydrationmelting of biotite occurred. Thus the garnetorthopyroxene-plagioclase granulites formed throughpartial melting of former biotite-bearing rocks in CO 2rich environment in the lower crust. Lack of K-feldsparand other K-bearing phases shows that the meltmigrated away and left behind a garnet-rich residue.REFERENCESBerman, R.G. (1991) Can. Mineral. 29: 833-855.Berman, R.G. & Aranovich, L.Ya. (1996) Contrib.Mineral. Petrol. 126: 1-24.Nair, R.& Chacko, T. (2002) J. Petrol. 43: 2121-2142.242

P56European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 244Deciphering superimposed Panafrican and Variscan hydrothermalevents through a fluid inclusion study in relation to deformation: thegold occurrence of Ourika (Western High Atlas, Morocco)Barakat, A. *, Marignac, C.**, Boiron, M.C.*** and Cathelineau, M.**** Faculté des Sciences et Techniques, Département des Sciences de la Terre, BP. 523, Béni-Mellal,Morocco**EMN and CRPG, BP 20, 54501, Vandoeuvre-les-Nancy, France*** G2R, Nancy-Université, CNRS, CREGU, BP 239, 54506, Vandoeuvre-les-Nancy, FranceThe axial zone of the Western High AtlasMountains in Morocco consists of basement rocks,both Palaeozoic and Precambrian, hosting severaltypes of ore deposits and showings (barite, Pb-Zn,Cu, and recently recognized Au, in the Atlas ofMarrakech). Although frequently considered aspanafrican, the high-temperature, low-pressure eventrelated to the earliest mineralizing stage is clearlypost-Pan-African and must therefore be related to theHercynian cycle, and, consequently, gold depositionwas also likely a Variscan event. This event ischaracterised in the Ourika inlier by tectonics (sinistralsets of N110 °E quartz veins) and by circulation ofC-O-H-N fluids that are clearly of the “pseudometamorphic”type, i.e., deep fluids of unknownorigin that were equilibrated at high temperature(≥450 °C) with graphite-bearing rocks (usually,metasediments). On the basis of textural evidencesfor fluid inclusion implosion, and the study of relativechronology of aqueous-carbonic inclusions andductile deformation, the following conclusions arereached: i) the fluid inclusions in quartz Q1 may beinterpreted as recording a trend of sub-isobaricdecreasing temperature, from ca. 400 °C (antekinematic,likely the formation temperature) to ca.260 °C (post-kinematic), spanning the ductile deformationevent. ii) Fluid characteristics and estimatedP-T conditions for the gold stage are similar to thosefound in the Hercynian mineralised veins of thebasement of the Western High Atlas (Tichka area,Bastoul, 1992), or in the late Carboniferous goldbearingveins of Western Europe at the early pyritearsenopyritestage (e.g., Boiron et al., 2001). Twophaseaqueous inclusions homogenising into theliquid phase (Lw), are recognized with two typesaccording to their salinity: i) high-salinity inclusions(Lw a), with Tm ice lower than –10 °C and simultaneouslylow Te, in the –55° to –50 °C range, suggesting thepresence of divalent cations, likely Ca, as confirmedby LIBS (Na/Ca ratiosbetween 0.7 and 3.3, and 0.1and 0.5) and ii) low- to moderate-salinity inclusions(Lw b), with Tm ice higher than –10 °C, and Te closeto that of the H 2O-NaCl system. The Th are variable(115 °–200 °C range). Gold was associated with thelate polymetallic stage and was likely deposited fromthe Na-dominated fluids of low to moderate salinitytrapped in the Lw binclusions. Then, gold depositioncould have resulted from fluid dilution and decreasein temperature (to 180 °C or less), not unlike mostother gold Variscan deposits in Western Europe.Finally, the Ourika gold showings may beinterpreted as rather typical orogenic gold deposits ofVariscan age, being however superimposed on older,possibly late Proterozoic, likely “epithermal” Fe-As-Smineralisations.244

P57European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 246Characterisation of the fluids in black-carbonate lithologies from anauriferous shear-zone (NW Portugal)Dória, Armanda*, Guedes, Alexandra*, Ribeiro, M. Anjos* and Ramos, João, F.***GIMEF, Centro de Geologia, Dep. Geologia, Fac. Ciências, Univ. Porto, Rua do Campo Alegre 687, 4169-007 Porto, Portugal**I.N.ET.I., Rua da Amieira, Apartado 1089, 4466-956 S. Mamede de Infesta, PortugalThe aim of this study is to characterise thefluids and the carbonaceous materials (CM) in nonoutcroppingblack-carbonate lithologies in order toevaluate the lithological control of the fluids, themetamorphic evolution of the area as well as betterconstraining the P-T conditions of fluid circulation.The study has been performed on samplesfrom metasedimentary rocks of drill cores obtainedduring an exploration survey at Três-Minas Romanopen-pits. The metasedimentary sequence consistsof phyllites, quartz-phyllites, black-shales and blackcarbonaterocks of upper Ordovician to lowerDevonian age. The metamorphism affecting the areawas of MT-LP (T=350 to 550 ºC and P = 300 to 400MPa). In the shear-zone sector the sequence showstransition conditions from chlorite to biotite zone.The fluid inclusion studies, (microthermometricand micro-Raman spectroscopy), were carried out inepidote, calcite and quartz from black-carbonate andcalc-silicate rocks and black phyllites. Thecontemporaneous CM was analysed by micro-Ramanspectroscopy (RS) in order to provide a complementarygeothermometer. The use of the RSCM method(Beyssac et al. 2002) was selected for the presentstudy, since it allows estimating temperatures in therange 330-650 ºC (accuracy ± 50 ºC).Preliminary results of FI studies show that thefluids are aqueous (H 2O-NaCl), with an exception ofthe fluids present in quartz from black phyllites whichare characterised by CH 4(H 2O-NaCl-CH 4-±N 2) andCM-bearing fluid inclusions. The fluid inclusionsoccur isolated or in discrete groups in calcite showT m(ice)in the range -4.1 to -2.5 ºC, (corresponding tosalinities of 4.2-6.6 wt% NaCl eq.). In epidote T m(ice)range from -2.3 to -0.1 ºC (0.2-3.9 wt% NaCl eq.). Inall samples the quartz shows a large T m(ice)variationbetween 1.7 to 11.8 wt% NaCl eq. In all aqueous FItotal homogenization (Th), occurs into the liquidphase and lies within the 250-330 ºC range. Theaqueous methane fluid inclusions observed asprimary FI in quartz show a volatile phase dominatedby CH 4(86-100 mol%) with variable quantities of N 2(10-14 mol%). Clathrate melts between about 11 and15 ºC and Th CH4ranges from -96 to -87 ºC. Th rangefrom 300 to 350 ºC.A representative first–order Raman spectraobtained in the different studied samples exhibit agraphite G band at around 1580 cm -1 and defectbands D2 around 1616 cm -1 and D1 around 1332 cm -1. After the deconvolution of the spectra the R2parameter (Beyssac et al. 2002) has been calculatedrepresenting T maxvalues obtained in the range 388-568ºC.The exclusive presence of CH 4-bearing fluidsin black-phyllites points to a lithological control of thefluids. The wide range of temperatures obtained inCM is probably due to several factors that locallyinfluenced the graphitization process: lithologies,structure, shear zones acting as channels thatpromote a local hydrothermal retrograde meta morphism.Further fluid inclusion studies and mineralogicalthermobarometry will be performed in order to providemore information about the origin, circulation andcomposition of the fluids.AcknowledgementsThis work is integrated in the “Centro de Geologiada Univ. Porto” activities, with the financial supportof (POCI 2010).REFERENCESBeyssac O., Goffé B., Chopin C. and Rouzaud J.N(2002) J. Metamorphic Geol. 20: 859-871.246

P58European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 248Peculiar fluids at the origin of orogenic gold deposits in Burkina Faso,West AfricaDubois, Michel*, Salvi, Stefano** and Béziat, Didier****UMR 8110 “PBDS”, Université de Lille 1, UFR Sciences de la Terre, 59655 Villeneuve d’Ascq, France**LMTG, Université de Toulouse, CNRS, IRD, OMP, 14 Av. E. Belin, F-31400 Toulouse FranceAlthough West Africa has a long history of goldproduction, most of the information available in theliterature concerns the large deposits of Ghana,notably the Ashanti mine (e.g., Leube et al. 1990;Amedofu, 1995). Only very little information can befound regarding neighbouring countries (e.g., Milésiet al. 1992). Here we report a synthesis of fluid inclusiondata collected from a number of gold showingsand prospects in Burkina Faso, a country that hostsa large number of mineralized sites, althoughproduction is still only artisanal to a great extent.In Burkina Faso, primary gold mineralization ishosted in Paleoproterozoic greenstone belts, tookplace synchronous with regional metamorphism anddeformation, and is associated to quartz-bearingveins; it is therefore classified as orogenic type(Béziat et al. in review). Two main styles of mineralizationwere recognized: 1) quartz-vein hosted, withgold concentrated within deformed quartz veins; and2) disseminated, where gold is found as disseminatedparticles in alteration halos of albitite-hosted quartzveins. These mineralization styles can occur withinthe same deposit. They are believed to be due to thesame hydrothermal event, and to reflect variations ofthe host lithologies (Béziat et al. in review).Fig. 1. CO 2-bearing inclusions (Type-1)Consistently with this interpretation, we foundthe same populations of fluid inclusions in both stylesof mineralization: 1) a CO 2-rich populations, and 2) aH 2O-CO 2population (Table). The carbonic phase iscommonly accompanied by N 2and CH 4. Type-1inclusions are the most abundant. Both types ofinclusions display variable bulk densities, due tovariable volume fractions of the vapor phase, resultingin highly variable bulk homogenization tem pe ratures.20 µmFig. 2. H 2O-CO 2-bearing inclusions (Type-2)TypeXCO2dCO2ThSalinityWt%mol% g/cm 3 °C1 >90 0.35-1.01 /2

P59European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 250Fluid inclusion and mineralogical studies of orogenic gold deposits inthe Loulo district, Mali, West Africa: criteria for assessing ametamorphic or magmatic originLawrence, David M.*, Rankin, Andrew*, Treloar, Peter* and Harbidge, Paul**.* Centre for Earth and Environmental Science Research, Kingston University, Penrhyn Road, Kingston-Upon-Thames, London, KT1 2EE** Randgold Resources, La Motte Street, St Helier, Jersey, JE1 1BJ, Channel IslandsRecent exploration in West Africa has led tothe discovery of numerous world class orogenic golddeposits that can be comparable on scale to wellknown gold districts in Western Australia and Canada.The Senegal-Mali shear zone and adjacent ground isone of the most productive/prospective regions inWest Africa and includes the Loulo district in westernMali. Deposits here are situated on 2 nd or 3 rd ordersplays off the main shear, a feature common to manyorogenic gold deposits. Within the Loulo district, theGara deposit, quartz-carbonate-hosted, is situatedwithin a folded sequence of quartz-tourmaline alteredgreywacke. The composition of orogenic gold fluids isgenerally well known (low salinity, mixed aqueousand moderately CO 2-rich). Their origin, however, isstill debatable. Fluid inclusion studies at Gara providean excellent opportunity to assess the relativeimportance of magmatic vs. metamorphic processesin the formation of orogenic gold deposits.Preliminary results show a mixture of early andlate (re-crystallisation) inclusions within quartz. Basedon phase proportions at room temperature, fourtypes of inclusions have been recognised. Type 1 aremono-, or bi-phase CO 2-rich inclusions. Type 2 l+vaqueous inclusions. Type 3 are l+v+s aqueousinclusions with several daughter minerals includinghalite. Type 4 inclusions are complex multiphase,mixed aqueous + CO 2inclusions ± daughter minerals,which likely represent the original gold-transportingfluid.Type 1 inclusions are the most common. T m-CO 2values around -56.6 °C agree with laser Ramanstudies that these are pure CO 2(CH 4and N 2absent).T hvalues (to liquid) vary between 0-20 °C indicatingCO 2densities in the range 0.92 to 0.80 g/cc. Theparagenetic relationships and origins of type 1, 2 and3 inclusions are unclear at this stage. They mayrepresent modification after entrapment of type 4inclusions (the original gold-transporting fluid?) orthey may imply that a mixture of fluids (magmatic andmetamorphic) was involved in the transport anddeposition of gold.Fig 1. Monophase CO 2rich inclusions230µmAlthough a definitive assessement of ametamorphic or magmatic origin for the gold at Gararemains questionable at this stage, the appearanceof highly saline daughters implies a magmatic source.EDS analysis of the vein and alteration assemblagemineralogy shows a “granitic” signature with thecommon presence of REE minerals (monazite andxenotime) in veins and abundant tourmaline in thehost rocks. Regional boron anomalies and the spatialassociation with known granitoids also supports thisview. Despite the evidence in support of a magmaticcontribution to the ore-forming system at Loulo, itsrelative importance in relation to a metamorphiccomponent (evident from CO 2–rich inclusions) stillneeds to be confined.250

P60European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 252Fluids associated with early Au-Bi-Te-S and late Au-Ag-Bi-Sb-Pb-Smineralization: an example from the Kasejovice gold district, BohemianMassif, Czech RepublicZachariáš, Jirí*, Šulcová, Barbora*, Hrstka, Tomáš* and Pudilová, Marta**Institute of Geochemistry, Mineralogy and Mineral Resources, Charles University in Prague, Albertov 6,Prague, 12843 Czech RepublicVariscan gold deposits and occurrences in thecentral part of the Bohemian Massif exhibit a closespatial and temporal association with the CentralBohemian Plutonic Complex (CBPC). Mineralizationsshare signs both of orogenic-gold and intrusionrelated-goldtypes of deposits. Some localities exhibitcomplex mineral associations interlinked with latestages of hydrothermal evolution. The Jílové andKasejovice deposits are the ore districts richest in Bi-(Hg-Pb)-tellurides and Bi-Pb-Sb-sulphosalts. To inferP-T conditions of their formation, we performed adetailed optical and electron microscopy coupled withcathodoluminescence (SEM-CL) fluid inclusionmicrothermometry.The Kasejovice district is separated by anarrow, 3–5 km wide and N-S-trending, ore-barrenzone from the Belcice gold district in the east. Thetwo districts are mineralogically quite similar but differmostly in the character of the host rock: metamorphicrocks (Kasejovice) vs. granitic rocks (Belcice), and inrelative abundance of molybdenite and scheelite.Molybdenite of the gold-bearing quartz veins of theBelcice district has been recently dated by the Re-Osmethod at 338 ± 2 Ma (Zachariáš and Stein 2001).Litochleb (1984) and Litochleb and Mrázek(1984) distinguished four mineralization stages at theKasejovice district: quartz stage (wolframite ±scheelite, quartz-1, apatite, rutile, tourmaline,arsenopyrite and pyrite-1); gold-bearing stage (quartz-2, muscovite, chlorite, pyrite-2, pyrrhotite, chalcopyrite-1, molybdenite, native bismuth, bismuthinite, variousBi-Te-S phases and gold-1); base metal “polymetallic”(Sb-bismuthinite, cobellite, Bi-jamesonite, Biberthierite,Bi-andorite, Ag-tetrahedrite, chalcopyrite-2 and gold-2 /electrum/); and calcite stage (calcite,dolomite, pyrite-3).Fluids associated with the formation of earlyquartz gangue are of H 2O-CO 2type with totalhomogenization between 280 and 360 °C (mostly toliquid) and low salinity (

P61European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 254Fluid inclusions in minerals of the Berezovsky orogenic gold deposit,Central Urals, RussiaProkofiev, Vsevolod Yu.* and Baksheev, Ivan A.*** IGEM RAS, per. Staromonetny 35, Moscow, 109017 Russia,** Department of Geology, Lomonosov Moscow State University, 119899 Moscow, RussiaThe Berezovsky mesothermal Au deposit islocated 10 km south of Yekaterinburg, Urals. Thedeposit is hosted by the weakly eroded Berezovskytectonic block, dominated by Silurian and Devonianterrigenous volcano-sedimentary rocks. The centralpart of the block is intruded by granitoids of theweakly eroded Shartash pluton. Numerous graniteporphyry dykes and later lamprophyre dykes cutacross the Shartash granitoids and the sedimentarysequence. Three types of metasomatic rocks andrelated quartz veins occur at the Berezovsky deposit.They are: gumbeite (quartz + potassium feldspar +calcite + dolomite + scheelite + pyrite), propylite(chlorite + epidote + amphibole + albite + quartz +tourmaline + carbonate + hematite), and beresite(quartz + sericite + dolomite + calcite + pyrite)assemblages. Gold-bearing quartz veins are relatedto beresite. Quartz from gold-bearing veins is dividedinto two generations. Early quartz-I is associated withscheelite, whereas quartz-II was deposited alongwith fahlores, aikinite, and native gold.Primary and pseudosecondary fluid inclusions(FI) of 3 to 25 µm in diameter occur mainly asnegative crystals in quartz and scheelite. Two typesof FI were identified on the basis of phase volumerelations at room temperature: aqueous- and gasdominated.Microthermometric measurements showedthat the homogenization temperatures of bothtypes of FI are close. These data, and the texturallocation of the FI, indicate simultaneous entrapmentof all inclusions from boiling fluids.The Table shows microthermometric analyses(obtained with a Linkam THMSG-600 heating/freezingstage) of individual fluid inclusions in quartz andscheelite within ore veins.Table. Analyses of individual fluid inclusions inminerals from ore veinsParameter Assoctiation*1 2 3 4T h(°C) 360 to295330 to290350 to270335 to255T eutectic(°C) –36 to–28–37 to–28–37 to–28–37 to–28T m ice(°C) –11.9 to–8.3–6.2 to–6.1–13.0 to–4.6–9.6 to–5.4T m CO2(°C) –56.7 to–56.6–56.7 to–56.6–57.5 to–56.6–57.4 to–56.6T m clathrate(°C) 5.0 to8.34.1 to6.30.6 to8.89.0 to5.0C NaCl(wt.%) 3.4 to10.77.0 to10.42.4 to14.92.0 to9.0C CO2(mol/kgsolution)5.2 to6.13.9 to4.42.4 to6.33.1 to5.3Pressure(kbar)3.4 to1.62.3 to1.73.4 to1.52.8 to0.8Raman analysis of gas phaseCO 2(mol.%) 99.2 to 99.7 -99.5N 2(mol.%) 0.1 0.5 to0.80.3 -* 1: Gumbeite, 2: Propylite, 3: Q 1+ scheelite, 4: Q 2The collective results indicate that quartz veinsrelated to the different metasomatic assemblageswere deposited from boiling H 2O-CO 2fluids, withsimilar temperatures and salinities, but variablecontents of trace elements. The gold-bearing mineralisedveins formed with only weak vertical variationsin their physicochemical parameters, promoting oredeposition over a significant depth interval. Thissuggests that the lower levels of this deposit mayhave notable ore potential.This study was supported by the IGCP (projectNo 540).254

P62European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 256Fluid inclusion characteristics and isotope analyses of the Savciliebeyit(Kaman-Kirsehir) gold-bearing quartz veins in Central AnatoliaSezerer Kuru, Gülay*and Selda, Bayir***General Directorate Of Minerel Research And Exploration, Ankara, 06520, Turkey**Turkish Petroleum Coorperation Research Center, Geochemistry Deparment Stable Isotope Laboratory,Ankara, 06100 , TurkeyThe Savciliebeyit (Kirsehir) gold-bearing quartzveins are found within the Kalkanlidag Metamorphicsand the Tamadag Metamorphics, which constitute thebasement of the pre-Mesozoic Kirsehir Massif inCentral Anatolia, Turkey. The Kalkanlidag Metamorphicsare composed of augen and banded garnetgneiss-schist, amphibolite-amphibolite schist andmigmatites. The quartz veins contain ore mineralssuch as native gold, hematite, pyrite, pyrrhotine andfahlore.Although quartz veins are divided into fivegroups according to their structures and colours, fluidinclusions within quartz veins have shown similarPVT properties based on microthermometric analyses.Microthermometric and isotope analyses have beenconducted on outcrop samples and drill-core samples,all of which are obtained from groups of five quartzveins. The quartz veins contain both CO 2-rich andwater-rich fluid inclusions. Fluid inclusions havevarying carbon dioxide contents from 10 to 95 mol%and maximum densities of 0.9 g/cm 3 . The fluidinclusions in the quartz veins display two separateranges of homogenization temperatures: one between160 and 380 °C, the other greater than 400 °C. Thesalinity ranges between 20 and 33 wt% NaCl equiv.Oxygen isotope studies (δ 18 O; +10 to +14‰ VSMOW)suggest that metamorphic water contributed to themineralising fluid.It may be concluded that waters in the fluidinclusions represent CO 2-rich metamorphic watersaccording to the microthermometric and isotopeanalyses conducted on quartz veins.256

P63European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 258Fluid evolution and gold deposition conditions of the El-Sid golddeposit, EgyptZoheir, Basem* and Moritz, Robert*** Department of Geology, Faculty of Science, Benha University, 13518 Benha, Egypt** Earth Sciences Institute, University of Geneva, Rue des Maraîchers 13, 1205 Geneva, SwitzerlandThe El-Sid mine, one of several historic goldlocalities in the central Eastern Desert, is consideredto be the largest and richest mesothermal vein-typegold mineralization in Egypt. Gold is confined to asystem of sub-parallel E-W, massive and laminated,milky to greyish quartz veins cutting through thewestern margin of a NS elongated, ~580 Ma old,granitoid pluton and adjacent variably tectonizedophiolitic serpentinite, metabasalt and metagabbro.The gold-bearing quartz veins (~200 m long, av. 1.5mthick, ~27.9 g/t Au) are generally sulfide-rich,carbonate-bearing and contain abundant wallrockselvages of variable size. Ore minerals comprisethree main generations: early pyrite-arsenopyrite±pyrrhotite±chalcopyrite, intermediate coarsegrainedpyrite-arsenopyrite-gold and late sphaleritegalena-gold/electrumassemblages. Gold is commonalong micro-fissures within the sulfide crystals or ininterstitial sites in vein quartz in the laminated quartzveins or associated with galena and sphalerite in latemilky quartz veins. Arsenopyrite thermometryindicates formation temperatures of 343 ±20 °C and315 ±10 °C for the early and intermediate Fe-Assulfideassemblages, respectively.Inclusions of C-O-H fluids, mainly three-phaseaqueous-carbonic (H 2O-NaCl-CO 2±CH 4) two-phaseaqueous (H 2O-NaCl±CO 2) and one/two-phase carbonic(CO 2±CH 4±H 2O) inclusions along intragranularand intergranular trails are common in the mineralizedquartz veins. The early greyish quartz veins are richin aqueous-carbonic inclusions, which are scarce inthe late massive milky quartz veins, in which aqueousinclusions prevail. The laminated quartz veins arerich in carbonic, subordinate aqueous and aqueouscarbonicinclusions. Salinities are generally low (0-7wt% NaCl eq.), especially in the laminated quartzveins, but inclusions associated with base-metalmineralization in the late milky quartz veins, mainlyaqueous, have typically higher salinities (up to 15wt% NaCl eq). The aqueous-carbonic inclusions arecharacterized by variable shapes, sizes, phase ratiosand homogenization temperatures. These variationsare attributed to mixing (dilution) of an initial aqueouscarbonicfluid with meteoric water, during faultreactivation and formation of the laminated quartzveins. Isochoric reconstructions, combined with oxygenand sulfur isotope geothermometry of mineralpairs, indicate P-T conditions for the gold depositionat 320 ±20 °C and 1.3 ±0.2 kbar for early gold+Fe-Assulfide mineralization and at 185 ±15 and 0.5 ±0.2kbar for the late gold-base metal mineralization. Theearly pre-gold sulfides were deposited during theinitial stages of fault development, together with massivequartz filling. Gold deposition was mainly inducedby fluid pressure fluctuation throughout a faultfracturevalve system, as well as destabilization ofgold-bisulfide/chloride complexes during fluid-wallrockinteraction (i.e. sulfidation). A clockwise evolutionpath on the P-T diagram (Fig. 1) likely documentslocal uplift and cooling of the ore fluids.Fig. 1. Isochores for: (a) aqueous-carbonicinclusions in early quartz veins in granite, (b)aqueous-carbonic inclusions in laminated quartzveins in granite, and (c) aqueous inclusions in milkyquartz veins cutting through serpentinite. Insetsshow inclusion types and Raman spectrum.258

P64European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 260Post-Variscan hydrothermal fluids in the Schwarzwald (Germany): fluidmixing without a visible mixing trend in fluid inclusion dataStaude, Sebastian*, Wagner, Thomas* and Markl, Gregor**Institut für Geowissenschaften, Eberhard-Karls-Universität, Wilhelmstrasse 56, Tübingen, 72074 GermanyIn the Schwarzwald district (Germany) about400 hydrothermal vein mineralizations with quartz,calcite, fluorite and barite, most of them post-Variscanin age, crosscut Variscan gneisses and granites.Since Neolithic and Roman times they were exploitedfor iron, copper, silver and other metals. On the wholethey are subeconomic today with just a few exceptions,like the active barite-fluorite mine Clara nearWolfach.In this study we did a combined fluid-inclusion,stable isotope and REE investigation of the gangueminerals. As shown in studies before (Metz et al.1957, Schwinn et al. 2006, Baatartsogt et al. 2007)the veins can be subdivided into Variscan quartzveins with weak salinar fluid inclusions of the H 2O-NaCl-(KCl) type and fluorite-barite-quartz-calciteveins with highly saline fluid inclusions of the H 2O-NaCl-CaCl 2type. Whereas the Variscan veins typicallyshow high formation temperatures around250 °C, the post-Variscan veins mostly are formedbetween 100 and 150 °C at pressures between 200and 500 bar through mixing from a 7 to 8 km deepbrine with meteoric water at the basement-coverunconformity in about 1.5 km depth.We studied some post-Variscan veins fromdifferent localities (e.g. Clara mine, Wenzel depositand veins of the Wittichen area), where multiplegenerations of gangue minerals in the same tectonicregime are present, to detect changes in precipitationhistory. All fluid inclusions have two phases (l+v) witha constant volume fraction of more than 95 % liquidat room temperature. Interestingly, no change infreezing point depression and chemistry of the fluidinclusions could be observed whereas homogenizationtemperatures, REE patterns of different fluoritegenerations and isotopic data of calcite and bariteshow clear differences between them. Thus, therehas to be an obvious time gap between differentgenerations. The source aquifer of the hydrothermalfluids was the same but changed his geochemicalcomposition slightly over time.In the calcite-dominated Wenzel deposit wecould show that the precipitation of the gangueminerals happens due to a change in pH. The ascending,hydrothermal fluid mixed with more alkalineformation water near the basement-cover unconformity.Due to the high salinity of the formationwater, there is no mixing trend in fluid inclusion datavisible.The same observation holds true in all otherstudied mineralizations, even though there is noother evidence for a different cause of precipitation(such as boiling, temperature- and pressure change,etc.). Thus, we suppose that this model explains theprecipitation in the post-Variscan hydrothermal veinsin similar tectonic regimes in the Schwarzwalddistrict.REFERENCESBaatartsogt B., Schwinn G., Wagner T., Taubald H.,Markl G. (2007) Geofluids 7: 123-147.Metz R., Richter M., Schürenberg H. (1957) Beih.Geol. Jb. 29: p.277.Schwinn G., Wagner T., Baatartsogt B., Markl G.(2006) Geochim. Cosmochim. Acta 70: 965-982.260

P65European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 262Fluid-inclusion and stable isotope characteristics of the Arapuçandere(Karaköy-Yenice-Çanakkale) Pb-Zn-Cu deposits, Biga Peninsula, NWTurkeyBozkaya, G.*, Gokce, A.* and Grassineau, N.V.*** Department of Geology, Faculty of Engineering Cumhuriyet University, 58140 Sivas Turkey** Department of Geology, Royal Holloway, University of London, Egham, Surrey TW20 OEX UKThe Arapuçandere Pb-Zn-Cu deposits, minedfor lead-zinc production, are typical examples of thevein type lead-zinc deposits occurring within the BigaPeninsula, with Permian-Triassic metamorphic, Triassicmeta-clastic and meta-basic rocks, Oligocene-Miocene granitoids, Miocene volcanics and Quaternaryterrestrial sediments that crop out in the studyarea.Ore deposits are developed as ore veins alongthe fault zones in the Triassic meta-sandstone andmeta-diabase. Microscopic studies revealed that theore veins contain galena, sphalerite, chalcopyrite,pyrite, marcasite, covellite and specular hematite asore minerals, and quartz, calcite and barite as gangueminerals. According to the macro- and micro-petrographicinvestigations, sulfide minerals were formedat the earliest stage of mineralization and were followedby quartz and calcite crystallization.Fluid inclusion studies showed that the salinity(avg. 18.34 %) was low but the temperature was high(avg. 301 ° C) during the sulfide precipitation stages.In contrast during the crystallization of the quartz, thesalinity (avg. 27.14 % NaCl equiv.) increased and thetemperature (avg. 240 ° C) decreased during thecrystallization of the quartz. During the formation ofsecondary inclusions in quartz, the temperature ofthe fluid seems to have increased but this may bedue to heterogeneous entrapment of the inclusionsby necking processes. The salinity and temperatureof the fluid gradually decreased through the laterepisode of mineralization during the formation ofprimary and secondary inclusions in calcite.Oxygen- and hydrogen-isotopic studies indicatethat the mineralizing fluid contained meteoric waterand that the primary oxygen isotopic compositionwas slightly changed by fluid – rock interaction.There does not seem to be any geologic andgenetic relation between ore veins and Oligo-Miocenegranitoids and Miocene volcanics. The ore and hostrock relation suggests only a post–Triassic age formineralization. Lead isotope model ages suggest, atleast, a pre-Eocene age for mineralization, which isolder than granitoid emplacement in the Oligocene-Miocene and volcanic activity in the Miocene.These data and comments indicate that thePb-Zn-Cu veins in the investigated area were formedby deep circulated meteoric water. The metals andsulfur were leached from the surrounding pre-Eoceneunits and deposited along the fault zones.262

P66European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 264Hydrothermal fluids in the base-metal vein mineralization in the NízkeTatry Mts. (Western Carpathians, Slovakia)Luptáková, Jarmila*, Biron, Adrian*, Hurai, Vratislav*, Chovan, Martin** and Prochaska, Walter****Geological Institute, Slovak Academy of Sciences, Dúbravská cesta 9, 840 05 Bratislava, Slovakia**Comenius University, Faculty of Natural Sciences, Department of Mineralogy and Petrology, 842 15Bratislava, Slovakia***Department of Geosciences, University of Leoben, A-8700 Leoben, AustriaThe Jasenie-Soviansko deposit represents thelargest accumulation of Pb-Zn ore in the Nízke TatryMountains. Hydrothermal veins are hosted in mediumto-highgrade metamorphic rocks (Rb/Sr: 400-380Ma), and clustered in a stockwork with approximatelyENE strike and 60-70° dip to SE. Circulating fluidsaffected surrounding gneisses and caused stronghydrothermal illitization and/or chloritization. Reactionsequence of 2M 1illite to 1M dillite-smectite indicatesdecreasing fluid temperatures (from ~300 to

P67European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 266Basinal brines as witnesses of fluid flow changes in a compressionalto-extensionaltectonic regime: the case of El Tule stratabound F-Srdeposit, NE MéxicoTritlla, Jordi*, Levresse, Gilles*, Lamadrid, Héctor*, Bourdet, Julien** and Corona-Esquivel, Rodolfo****Prog. de Geofluidos, Centro de Geociencias, Campus Juriquilla, UNAM, 76230 Querétaro, México.**UMR 7566 G2R-CREGU, Univ. H. Poincaré, B.P. 239, Vandoeuvre-lès-Nancy, 54506, France.***Museo de Geología-Instituto de Geología, UNAM, 06400, México D.F., México.In North-East Mexico, several low-temperature,epigenetic, stratabound Pb-Zn-F-Ba ore depositsoutcrop forming a newly defined MVT province (Tritllaet al., 2007). These deposits present a closeassociation with organic matter (liquid hydrocarbons,bitumen, gas), display a very simple mineralogy(hypogene: barite, celestine, fluorite, sphalerite,galena) and present low formation temperatures (90-105 ºC) and variable salinities.An unusual mixed celestine-fluorite ore depositis located at El Tule, north of Muzquiz (Coahuila). Itis made up by a single stratabound body whosedisposition is controlled by sub-horizontal stratificationjoints with clear evidence of layer-parallel slip.Celestine contains abundant aqueous, twophasefluid inclusions with evidence of post-trappingchanges. Th’s are between 80 and 120 °C with veryvariable salinities between 5 and 11 wt% eq. of NaCl(Lamadrid, unpublished personal data). Ramananalyses indicate no traces of other gases than watervapor. The Th vs salinity plot suggests a mixing offluids as the main mechanism for celestineprecipitation, despite the heavy dispersion of data.Fluorite contains brine-bearing and oil-bearingprimary fluid inclusions. Brine-bearing fluid inclusionsare bi-phase (L+V) to poly-phase (L+V+S trapped). Thare between 120 and 150 °C and salinities between11.7 and 16 wt% eq. of NaCl respectively (Lamadrid,unpublished personal data). In a Th vs salinity plot,the data array suggests that fluorite precipitatedmainly by cooling after mixing of two, contrastedfluids. Raman analyses indicate the presence ofvariable amounts of CH 4, H 2S and CO 2within the gasphase. Hydrocarbon-bearing fluid inclusions are darkbrown in color (heavy oils) and poly-phase (L+V+B),owing to the presence of variable amounts of solidbitumen. Both fluid inclusion types in fluorite showclear evidence of coeval trapping. FTIR analyses andCLSM volumetric reconstructions of the hydrocarbonbearingfluids indicate the presence of heavy oils. Allthese data have been used to model the PVTconditions for fluorite precipitation using the PITsoftware (Thiery et al., 2000).Celestine precipitated within openedsedimentary joints during and after the Laramidedeformation, partially substituting the enclosinglimestone, filling up fenestral porosity after anhidritedissolution. Fluorite precipitated after a dramaticchange of the fluid composition, which probablyterminated celestine formation. The residual Ca 2+ -enriched brine, which remaind after celestineprecipitation, mixed with an external emulsion ofbrine and hydrocarbons. This resulted in partialdegradation of the organic matter by means of TSRreactions and the generation of CH 4, H 2S and CO 2,which is found in the gas phase of the brine-bearingfluid inclusions.The mineralogical change from celestine tofluorite precipitation probably reflects a change in thefluid regime and composition from a compressiveregime (Laramide orogeny) to the subsequent postlaramideextension.REFERENCESTritlla, J.; Levresse, G.; Corona-Esquivel, R.; Banks,D.; Lamadrid, H. and Bourdet, J. (2007) Geol. Soc.Am. Sp. Pap. 422, in press.Thiery, R., Pironon J., Walgenwitz F, Montel F,(2000) Jour. Geochem. Exp. 69-70, 701-704.266

P68European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 268A preliminary fluid inclusion study of the Belo Brdo Pb-Zn (Ag) deposit,northern KosovoVeselinovic-Williams, Milica 1 , Treloar, Peter J. 1 , Rankin, Andrew H. 1 and Strmic-Palinkas, Sabina 2 .1. Centre for Earth and Environmental Science Research, Faculty of Science, Kingston University, PenrhynRoad, Kingston upon Thames, Surrey, KT1 2EE, UK2. Geology Department, Faculty of Science, Zagreb University, CroatiaThe Belo Brdo Pb-Zn (Ag) deposit is locatedwithin the NNW-SSE-trending Vardar Zone of theDinaride-Hellenide Belt. Cretaceous carbonate rockshost three main ore bodies of hydrothermal repla cement-type.An additional hydrothermal vein deposit islocated within Tertiary andesites. The present studywas initiated with the aim of improving understandingof the conditions of formation of the Pb-Zn (Ag)deposits in the Vardar Zone.Preliminary fluid inclusion studies for the BeloBrdo deposit were conducted on several quartzsamples, which were selected from 17 doublypolished wafer sections covering a depth range of195 m of the main ore body. A very large number ofinclusions of presumed primary origin were con centratedalong growth zones of the euhedral quartzcrystals (Fig. 1A) syngenetic with sulphides. Due totheir small size, they were generally not suitable formicrothermometric studies. Isolated probable primaryinclusions (Fig. 1B), which vary in size from less than2 µm to up to 5 µm, contain only two phases at roomtemperature – a low-salinity H 2O liquid phase and avapour bubble with no daughter minerals, typical ofepithermal environments (Bodnar et al., 1985). Homogenisationinto the liquid phase occurred between138 °C and 210 °C. Cooling was hampered by thesmall size of inclusions, so the incipient melting of icewas difficult to observe. Where possible, final meltingtemperatures were recorded at ~ -4.4 °C indicatingsalinities of ~ 7 eq. wt. % NaCl .Fluid inclusions from the late-stage quartz crystalsfrom open cavities contained two types of inclusions.Type I are large, irregularly shaped, inclusions(Fig.1C), which contain a small bubble and dominantliquid phase. Homogenisation temperatures are inthe range of 201 °C and 240 °C and final ice meltingtemperatures are observed at –6.8 °C (10.2 eq. wt. %NaCl). In some inclusions, it was very difficult to distinguishbetween the ice and a clathrate. Type II(Fig.1D) includes large, aqueous fluid inclusions witha small bubble, exhibiting homogenisation at 165 °Cto 177 °C. The temperatures of last ice melting of ~–3.5 °C and –3.0 °C point to salinity of 5.7 and 4.9 eq.wt. % NaCl, respectively.Preliminary fluid inclusion data suggest that atleast two types of fluids are associated with the mineralisationat the Belo Brdo deposit.ACFig. 1. Transmitted light photomicrographs of fluidinclusions from the Belo Brdo deposit.A: dark bands of primary inclusions along growthzones in euhedral quartz; scale 100 µm.B: Individual primary inclusions; scale 2 µm.C: Irregular “pseudo-secondary inclusion”; scale20 µm.D: Large aqueous fluid inclusions; scale 50 µm.REFERENCESBodnar, R. J., Reynolds, T. J. and. Kuehn, C. A.1985. Fluid Inclusion Systematics in EpithermalSystems. In: Berger, B. R. and Bethke, P. M. (eds),Geology and Geochemistry of Epithermal Systems.Reviews in Economic Geology, Vol 2, 73-97.BD268

P69European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 270Fluid geochemistry in the Ivigtut cryolite deposit, South GreenlandKoehler, Jasmin*and Markl, Gregor**Institut für Geowissenschaften, Universität Tübingen, Wilhelmstr. 56, 72074 Tübingen GermanyThe mid-Proterozoic Ivigtut intrusion inSouthern Greenland is world-famous for its cryolitedeposit [Na 3AlF 6] which is now mined out. Thedeposit is situated within an A-type granite stockwhere F-rich fluids led to metasomatism, greisenisationand formation of cryolite, rare fluorides, sulfides andsiderite (Goodenough et al., 2000). A detailed fluidinclusion study was carried out in order to constrainthe exact mechansims and the role of the fluid whichled to the evolution of this unique deposit.Fluid inclusions were analysed in quartz,cryolite, fluorite and siderite and are mostly ofsecondary origin. Microthermometry of fluid inclusionsshows that three types of inclusions can be dis tinguished:(1) pure CO 2, (2) aqueous carbonic and (3)saline aqueous inclusions. Melting temperatures areabout -56.6 °C for type 1 inclusions, range between-23 to -15 °C for type 2 and from -15 to -10 °C for type3 inclusions. Most inclusions homogenise between110 and 150 °C into the liquid. Fluid petrography andmeasured temperatures suggest fluid immiscibilitydue to different degrees of fill and strongly varyingproportions of CO 2and H 2O in type 2 inclusions.Stable isotope compositions of CO 2and H 2Owere measured from crushed inclusions. δ 13 C valuesare about -5 ‰ PDB which is typical of mantle-derivedmagmas (Pineau & Javoy, 1983). δ 18 O (CO 2)ranges between 21 and 42 ‰ VSMOW while δ 18 O(H 2O) varies from -1 to -20 ‰ VSMOW. Thesesvalues suggest low-temperature isotope exchangeas proposed by Richet et al. (1977). δD (H 2O) rangesfrom -19 to -123 ‰ VSMOW. The isotopic compositionof inclusion water closely follows the meteoric waterline and is comparable to other fluids from Gardarcomplexes (see accompanying abstracts by Graserand Schoenenberger) and Canadian Shield brines(Bottomley et al., 1994; Fig.1).Ion chromatography revealed the fluid’spredomincance in Na, Cl and F. Cl/Br ratios rangebetween 56 and 110, suggest intensive fluid interactionwith the host granite and support the fluid’s nonmarinederivation.Fig. 1. Cl-Br systematics of fluid inclusions fromIvigtut compared to other Gardar complexes(Ilímaussaq, Motzfeldt, see abstracts) and CanadianShield Brines (Frape et al., 1984; Bottomley et al.,1994).Our results show that the Ivigtut fluid has thetypical characteristics of a hydrothermal, Na-dominatedbrine. Isotopic data suggest that the CO 2component is mantle-derived whereas the dominantH 2O part is of meteoric origin and intensively interactedwith the host granite.REFERENCESBottomley, D.J., Gregoire, D.C., Raven, K.G. (1994)Geochimica et Cosmochimica Acta 58: 1483-1498.Goodenough, K.M., Upton, B.G.J., Ellam, R.M.(2000) Lithos 51: 205-221.Frape, S.K., Fritz, P., McNutt, R.H. (1984)Geochimica et Cosmochimica Acta 48: 1617-1627.Pineau, F., Javoy, M. (1983) Earth and PlanetaryScience Letters 62: 239-257.Richet, P., Bottinga, Y., Javoy, A. (1977) AnnualReviews Earth Planetary Science 5: 65-110270

P70European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 272The significance of clathrates in fluid inclusions in the Broadlands-Ohaaki geothermal system, New Zealand.Simmons, Stuart F.*, Simpson, Mark P.* and Reynolds, T. James*** School of Geography, Geology and Environmental Science, University of Auckland, Private Bag 92019,Auckland Mail Centre, Auckland 1142, New Zealand** FLUID INC., 1401 Wewatta St. #PH3, Denver, CO 80202, USAGeothermal systems have long provedimportant in calibrating the utility of fluid inclusions forinterpreting P-T-X conditions in ancient hydrothermalenvironments. Here we report results of a detailedstudy of fluid inclusions, which form CO 2clathratesupon freezing, in a single quartz crystal from the upflowzone of the Broadlands-Ohaaki geothermalsystem (well Br-15, 1252 m depth). Although theclathrates form in a large number of primary andpseudo-secondary inclusions, we believe the highCO 2inclusion fluid concentrations are all artefacts oftwo-phase trapping.For background, the deep hydrothermal fluidsin the modern geothermal system only contain up to3.3 wt percent CO 2and 0.1 wt percent Cl. Earlier fluidinclusion investigations show that most Th-Tm datareflect boiling and mixing in the upper 2 km of thesystem, matching modern fluid conditions.The quartz crystal studied contains twogenerations of coexisting liquid-rich and vapor-richfluid inclusions. The earliest generation occupies thecore of the quartz crystal, with a dense concentrationof two-phase inclusions having smooth outlines andequant shapes. Many of these are liquid-rich with ~65percent liquid and ~35 percent vapor. Their liquidvaporratios appear nearly uniform, with Th data from288 to >365 °C, Tm data from -0.1 to -2.2 °C, andTclath data from 5.3 to 11.5 °C. Only a few fluidinclusions with Th data of ~300 °C and Tm data from-1.4 to -1.6 °C appear realistic in terms of the likelyconditions of early quartz precipitation from a modestlyover-pressured fluid. The second generation of fluidinclusions occurs in a late overgrowth with Th data of~300 °C and Tm data of -0.2 to -0.8 °C, reflectingvalues that closely match the modern P-T-X conditionsat 1258 m depth in the well.Localized, heterogeneous two-phase trappingof co-existing gas and liquid best explains theexistence of the anomalous concentrations of CO 2producing the clathrates in early fluid inclusions, asthese are the only such fluid inclusions known atBroadlands-Ohaaki. This interpretation is supportedby calculations which model two-phase trapping ofliquid and gas (steam + CO 2), resulting from a smallamount of boiling starting at 310 and 305 °C of aparent fluid initially containing 3.3 wt % CO 2.The results imply that “gassy” geothermalsolutions may be prone to producing fluid inclusionswith anomalously high CO 2concentrations and thatextra care may be required to resolve if they arepossibly artefacts of two-phase trapping. Note thatthe simultaneous entrapment of liquid and vapour didnot produce fluid inclusions with widely varing liquidto vapor ratios as normally expected.The results also imply that pressures exceedinghydrodynamic gradients can develop at least locallyduring the life of a geothermal system. Fluctuatingpressure conditions may simply reflect the verticalextent of boiling conditions. If true, then the CO 2composition of the deep liquid could have remainednearly constant throughout the period represented byboth the early and late stage fluid inclusions.REFERENCESSimmons S. F. et al., (2007) Economic Geology.102: in press.272

P71European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 274Mineral precipitations and fluid chemistry variations during LIBSablationFabre, Cécile, Boiron, Marie-Christine and Dubessy, JeanDépartement Sciences de la Terre, UMR G2R CNRS, 54506 Vandoeuvre Les Nancy, FranceLaser Induced Breakdown Spectroscopy(LIBS) is based on the use of a pulsed laser focusedonto the sample surface to drill down to the fluidinclusion (FI). After FI opening, the elemental compositionof the liquid phase can be obtained accordingto its chlorinity (Na, Ca, Mg, K, Li, Ba, Sr …).Precipitation of minerals is rarely observed during theablation process, however, this study presents astriking example of halite precipitation from alpinefluid inclusions.Samples from alpine crystals have beenextensively studied over several years, with typicalcompositions displaying moderate salinities and lowCO 2-CH 4contents. The selected quartz samplecontains a homogeneous FI population with a salinityof 11 equiv. wt% NaCl (T mice= –7.4 °C). For some FI,the first laser shots allow the chemical composition ofthe initial fluid to be obtained, but subsequently,minute crystals suddenly precipitate all around the FIcrater on the quartz surface (Fig. 1).The chemical composition of the fluid thatremains on the bottom of the inclusion dramaticallychanges, with a drop in the Na content and anincrease in the Ca-signal (Fig. 2). SEM observationhas identified halite crystals on the inclusion borderbut no Ca-bearing crystals have yet been identifiedon the bottom of the fluid inclusions. However,different LIBS analyses of these minute crystalsindicate the presence of calcium (in very low amounts).The table reports the reconstructed fluid compositionsbefore and after the precipitations.Fig. 2. Optical emission intensities of major elementsduring ablation process (arrow correspondsto halite precipitation)mmole/l Na Ca K LiBefore 1560 32 93 63After 770 384 230 12The enhancement of the Ca signal probablyarises from Ca precipitation on the FI. A pressuredrop during the opening of the FI, linked to the presenceof minor CO 2in the vapour phase, may modifythe calcite/fluid equilibrium. Numerical modelling ofthe fluid/mineral equilibrium will be carried out to testthe hypothetical fractionation process.Fig. 1. Halite crystals observed using SEM aroundthe ablated fluid inclusion274

P72European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 276An online GC-irMS crushing technique for stable isotope analysis oftrace gases in aqueous-dominated fluid inclusions: An example fromthe Noranda VMS District, Quebec, CanadaPotter, Joanna*, Zubowski, Stephen M.**, Spooner, Edward T.C.***, Bray, Colin J.***, Longstaffe, Frederick J.*and Gibson, Harold L.***Department of Earth Sciences, The University of Western Ontario, London, Ontario N6A 5B7, Canada**Department of Earth Sciences, Laurentian University, Sudbury, Ontario P3E 2C6, Canada*** Department of Geology, University of Toronto, 22 Russell Street, Toronto, Ontario M5S 3B1, CanadaA continuous-flow crushing technique has beendeveloped for extraction of fluid inclusion volatiles forcompound-specific carbon- and hydrogen-isotopeanalysis by gas chromatography isotope-ratio massspectrometry.Fluid inclusion volatiles are extractedby crushing samples in a high helium flow at ~120 °C,based on the method of Bray and Spooner (1992).The gases released are captured in a molecularsieve trap immersed in liquid nitrogen, enabling captureof non-condensable and condensable phases.The high helium flow through the molecular sievetrap is then switched to a low flow (1-2 ml/min). Thetrapped gases are released and transferred to a0.32 mm x 25 m Poraplot Q column. Eluting gasesare passed through a combustion reactor for carbonisotopedetermination or a pyrolysis reactor forhydrogen-isotope determination by isotope-ratiomass-spectrometry (see Potter and Longstaffe, 2007for details).The McDougall I and II faults in the NorandaDistrict, Quebec represent localised hydrothermalalteration and mineralisation, interpreted to be afeeder system for Archean VMS deposits. Twocompositional types of fluid inclusions have beenidentified: (1) primary, pseudo-secondary andsecondary two-phase aqueous H 2O-NaCl±KCl/CaCl 2inclusions in hydrothermal, comb-textured quartz,and (2) secondary aqueous-CO 2inclusions in quartzassociated with chalcopyrite. Trace amounts of lighthydrocarbons (

P73European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 278A new approach for measuring salinities of aqueous fluid inclusionsthat contain compressed gasesAudétat, Andreas**Bayerisches Geoinstitut, Universität Bayreuth, 95440 Bayreuth, GermanyMicrothermometric determination of the salinityof aqueous fluid inclusions that contain compressedgases (e.g., CO 2, CH 4, N 2, H 2S) is hampered by theformation of clathrates, which severely complicatephase relations at low temperatures. In many casesaccurate salinity determination is impossible,particularly if mixed gases are present. Even in therelatively simple system H 2O-NaCl-CO 2, fluid salinitiescannot properly be constrained if the last melting ofclathrates occurs in the absence of liquid CO 2.A potential way to get around this problem is torelease compressed gases within the fluid inclusionsby opening them mechanically, and subsequentlydetermine fluid salinities on the basis of ice meltingtemperatures or other phase transitions in gas-freemodel systems. A piercing stage containing a tungstencarbide needle was developed that allows individualfluid inclusions that reside close to the sample surface(

P74European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 280An updated understanding of acoustic emission decrepitationBurlinson, KingsleyBurlinson Geochemical Services Pty. Ltd., Darwin, NT, Australia. kgb@synix.com.auThe premature demise of acoustic emissiondecrepitation as a fluid inclusion study technique wasmainly because of an inability to relate the temperatureof onset of massive decrepitation with the formationtemperature. But much of this problem was in factdue to a lack of understanding of the importance andbehaviour of CO 2in fluid inclusions. From the gaslaw, it is clear that CO 2-rich fluid inclusions will develophigh internal pressures at low temperatures,resulting in decrepitation well below their formationtemperatures. Although this behaviour is a hindrancein determining formation temperatures it meansdecrepitation data can easily be used to detect CO 2-rich inclusion populations, which is very useful inmineral exploration for Au deposits because of thecommonly documented association between Au andCO 2-rich fluids (Fig 1).Other gases such as CH 4behave just like CO 2and so they contribute to this low temperaturedecrepitation effect. Plots of the equation of state forvarious gases show that they all result in highinclusion pressures and low temperature decrepitation.Statements by some authors that CH 4does notcause fluid inclusion decrepitation are incorrect andcontradict the gas law.Schmidt-Mumm (1991) asserted that soundsmeasured in decrepitation experiments were dominatedby cyrstallographic and grain boundary effects.This is incorrect as the instruments used measure apressure pulse in the air column between the sampleand sensor. Changes in crystal structure or grainboundary movements simply cannot generate largeenough pressure pulses to be detected. Only therupture of fluid inclusions with subsequent release ofhigh pressure gases or a steam explosion fromsuperheated water can generate the pressures necessaryfor detection. And because secondary inclusionsleak gradually or open at low temperatures, they failto generate sufficient pressure to be detected. Consequently,acoustic decrepitation side-steps the entireproblem of secondary inclusions and their potentialmis-identification in microthermometric studies.A comparison of fluid inclusion abundancecounts in thin-section with decrepitation of the samesamples shows that only some 0.5% of inclusionslarger than 8 µm across decrepitate and are detectedduring analysis. Despite this, replicate analyses ofaliquots of the same sample give consistent andreliably reproducible results.Acoustic decrepitation has been incorrectlymaligned and although it is not a high precisionmethod, it gives consistently reproducible fluidinclusion population temperatures and an indicationof CO 2+ CH 4gas contents. As it is fast and cheap itis ideal for use in exploration or for preliminaryscanning in conjunction with conventional micro thermometricstudies.Fig. 1. Quartz from Ballarat decrepitates at lowtemperatures between 180 and 300 °C as itcontains abundant CO 2-rich inclusions, while quartzfrom Dongping lacks CO 2-rich inclusions and doesnot decrepitate until 370 °C, its approximate T .fREFERENCESSchmidt-Mumm A. (1991) Phys Chem Minerals.17:545-553.280

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 282Author IndexAAbart, R. 234Ahmadi, M. 222Allan, M.M. 186Amacher, P. 170Andreeva, I.A. 224Audétat, A. 142, 278Azbej, T. 220BBabansky, A.D. 210Badanina, E.V.C. 196Bakker, R.J. 24, 58, 178, 238Baksheev, I.A. 254Bali, E. 78, 142, 214, 230Banks, D. 48, 72, 90, 94, 96, 98, 100Barakat, A. 244Bass, J.D. 56Baumgartner, L. 114Baumgartner, M. 58, 178Becker, S.P. 134Bell, A.S. 144Bento dos Santos, T.M. 168Berkesi, M. 80Béziat, D. 248Biron, A. 264Blamey, N.J.F. 42, 206Bleuet, P. 60, 180Bobos, I. 200Bodnar, R.J. 36, 84, 102, 108, 134, 136, 212Bohrson, W. 102Boiron, M.C. 48, 90, 94, 124, 244, 274Bonelli, R. 228Boni, M. 130Borsato, A. 126Boschi, C. 176Boulvais, P. 90, 94Bourdet, J. 266Bouybaouenne, M.L. 166Boyce, A. 72Bozkaya, G. 262Bray, C.J. 276Brown, K.L. 110Brugger, J. 62, 180Brune, J. 190Burlinson, K. 280CCanals, À. 150Cannatelli, C. 212, 102Castelain, T. 28Cathelineau, M. 90, 94, 124, 244Cauzid, J. 60, 180Chistyakova, N.I. 226Chovan, M. 92, 264Cline, J.S. 116Compagnoni, R. 122Conliffe, J. 38Constantin, S. 128Coquinot, Y. 28, 58, 174, 178Corona-Esquivel, R. 266Courtieu, C. 188Cuney, M. 94DDallai, L. 126, 176Dégi, J. 234, 242De Capitani, C. 52De Vivo, B. 102, 212Diamond, L.W. 30, 46Dias Neto, C. 168Dini, A. 176Dória, A. 168, 246Dowman, E. 198Driesner, T. 70, 140Duan, Z. 22Dubessy, J. 20, 90, 274Dublyansky, Y. 126Dubois, M. 28, 138, 174, 248Dutkiewicz, A. 44, 152EEsposito, R. 212Ezhov, A.A. 158FFabre, C. 90, 274Fall, A. 136Fallick, A.E. 72, 112Fedele, L. 84, 102, 212Feely, M. 38, 42Ferrando, S. 122Figueiredo e Silva, R.C. 98282

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 283Fintor, K. 154Fonarev, V.I. 236Fonseca, P.E. 168Forti, P. 128Fourcade, S. 124Franz, L. 52Frenz, M. 64, 130, 184Frezzotti, M.-L. 122, 228Fricker, M. 190Frisia, S. 126GGarofalo, P.S. 128George, S.C. 44, 152Gianelli, G. 176Gibson, H.L. 276Gilg, H.A. 36, 130Girnis, A. 208Goffé, B. 28Gokce, A. 262Goldstein, R.H. 40Gordienko, V.V. 196Goryainov, S. 76Gouy, S. 28Grandia, F. 150Graser, G. 106Grassineau, N.V. 262Grishina, S. 76Guedes, A. 168, 246Guillaume, D. 188Guillong, M. 66, 82, 186Günther, D. 128, 190Guzmics, T. 78, 214, 230HHagemann, S.G. 96, 98, 100Halter, W. 78, 86Hanley, J.J. 66, 186Harbidge, P. 250Harlov, D. 120Harris, C.R. 68Hart, C.J. 66Havancsák, I. 214, 220Hayashi, K. 146Hazemann, J.-L. 62, 180Heijboer, T. 170Hein, U.F. 164Heinrich, C.A. 34, 66, 68, 70, 82, 114, 140, 186Hennings, S. 164Hermann, J. 148Herms, P. 238Hidas, K. 80, 230, 232Hrstka, T. 252Hurai, V. 92, 240, 264IInvernizzi, C. 50JJames-Smith, J. 62, 180Janák, M. 240Jaques, L. 200Jarmolowicz-Szulc, K. 156Jeffries, T. 192Jessell, M. 48Jiménez Sandoval, S. 160Johannsson, L. 120John, T. 238KKetcham, R.A. 182Kleine, T. 68Kodera, P. 112Kodolányi, J. 78, 234Koehler, J. 106, 270Koller, F. 220Konc, Z. 232Kostova, B. 70Kotelnikov, A.R. 32Kotelnikova, Z.A. 32Kóthay, K. 216Kouzmanov, K. 114Kovács, I. 78, 230Kovalenker, V. 218Kovalenko, V.I. 224Krause, P. 190Krüger, Y. 64, 130, 184Kyle, J.R. 182LLamadrid, H. 266Lauritzen, S.-E. 128Lawrence, D.M. 250Levresse, G. 160, 266Lexa, J. 112Lexa, O. 92Lima, A. 102, 212Liu, W. 62, 180283

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 284Lledo, H.L. 116Lobato, L.M. 98Longstaffe, F.J. 276Lopez de Luchi, M. 204Lüders, V. 36, 60Luptáková, J. 264MMao, S. 22Marignac, C. 244Markl, G. 104, 106, 260, 270Marosi, G. 242Marshall, D. 88Martinez-Criado, G. 180Masalehdani, M. 174Mavrogenes, J. 148Meier, D. 186Melnikov, F.P. 158Mercadier, J. 94Monnin, C. 28Moritz, R. 258Mossman, D.J. 152Mullis, J. 52, 170, 172Munhá, J.M.U. 168Mutchler, S. 84NNaranjo-Vesga, J.F. 42Naumov, V.B. 210, 218Naze, N. 174Nédli, Z. 220Neumayr, P. 100Norman, D.I. 206Noronha, F.M. 168, 200Ntafl os, T. 216OOlga, V. 236Olivetti, V. 166Ortiz Suarez, A. 204Owens, P. 42PPainsi, M. 30Perfetti, E. 20Pernot, N. 138Perucchi, A. 122Petersen, K.J. 100Pettke, T. 26, 36, 68, 118Philippot, P. 62, 180Pierron, O. 124Piqué, À. 150Polozov, A. 76Potdevin, J.-L. 174Potter, J. 106, 276Prochaska, W. 92, 264Prokofi ev, V.Y. 158, 254Proux, O. 62, 180Pudilová, M. 252Putlitz, B. 114RRamos, J.F. 246Ramos-Rosique, A. 160Rankin, A.H. 198, 250, 268Reynolds, T.J. 136, 272Ribeiro, M.A. 246Rice, C. 72Richard, A. 94Richard, L. 124Ricka, J. 64, 184Rickers, K. 60, 180Ridley, J.S.C. 44, 152Rolandi, G. 212Romer, R.L. 36Rossetti, F. 166Ruggieri, G. 176Rusinov, V. 218Ryder, A.G. 42SSalvi, S. 188, 248Sanchez-Valle, C. 56Scambelluri, M. 118Schenk, V. 238Schmidt, C. 54Schoenenberger, J. 104Schubert, F. 154, 162Schulmann, K. 92Sekine, K. 146Selby, D. 38Selda, B. 256Selector, S. L. 158Severs, M. 212Sezerer Kuru, G. 256Sharygin, V.V. 216, 232Siebenaller, L. 48Simmons, S.F. 110, 272284

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 285Simon, A.C. 26, 144Simpson, M.P. 272Skora, S. 114Sokolov, S.V. 202, 226Solovova, I.P. 208Sosa, G. 204Spandler, C. 148Spera, F. 102Spooner, E.T.C. 66, 276Spötl, C. 126Staude, S. 260Steele, G. 72Stoller, P. 64, 130, 184Strmic-Palinkas, S. 268Stünitz, H. 46Šulcová, B. 252Syritso, L.F. 196Szabó, B. 162Szabó, C. 74, 78, 80, 214, 216, 220, 230, 232TTarantola, A. 46, 172Tassinari, C.C.G. 168Tecce, F. 122, 166Testemale, D. 62, 180Thiéry, R. 20Thomas, R. 196Thorne, W. 96Titov, A. 76Tolstikh, M.L. 210Török, K. 216, 234, 242Tóth, T.M. 154, 162Treloar, P.J. 250, 268Tritlla, J. 160, 266Trubkin, N.V. 158VVanderhaeghe, O. 48Van den Kerkhof, A.M. 120, 164, 204Van Roermund, H.L.M. 118Vapnik, Y. 236Vennemann, T. 52, 114, 170Veselinovic-Williams, M. 268Volk, H. 44, 152Vollbrecht, A. 164Vry, V. 192WWagner, T. 260Wall, F. 198Walshe, J. 100Wilkinson, J. 192, 194Williams, P. 62XXue, G. 88YYardley, B.W.D. 100, 186ZZacharias, J. 194, 252Zajacz, Z. 78, 86, 230Zoheir, B. 258Zubowski, S.M. 276285

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 286Conference ParticipantsMr. Ahmadi Mojtaba Department of Geology Tehran University PO Box 14155-6455 Tehran IRAN ahmadi29@yahoo.comDr. Andreeva Irina Institute of Geology of OreDeposits, Petrography,Mineralogy, andGeochemistryMrs. Aubet Natalie Department of Earth &Atmospheric SciencesAcademy of Sciences Staromonetny per.,35University of Alberta 1-26 Earth SciencesBuildingDr. Audétat Andreas Bayerisches Geoinstitut Universität Bayreuth Universitätsstrasse30Prof. Babansky Andrey Institute of Geology of OreDeposits, Petrography,Mineralogy, andGeochemistryDr. Badanina Elena Department ofGeochemistryAcademy of Sciences Staromonetny per.,35State University ofSt. Petersburg119017 Moscow RUSSIANFEDERATIONT6G 2E3 Edmonton,Albertaandreeva@igem.ruCANADA aubet@ualberta.ca95447 Bayreuth GERMANY andreas.audetat@uni-bayreuth.de119017 Moscow RUSSIANFEDERATIONUniversity emb. 7/9 199034 St. Petersburg RUSSIANFEDERATIONbaban@igem.ruelena_badanina@mail.ruDr. Bakker Ronald J. Mineralogy & Petrology University of Leoben Peter-Tunner-Str. 5 8700 Leoben AUSTRIA bakker@unileoben.ac.atDr. Bali Enikö Bayerisches Geoinstitut University of Bayreuth Universitatstrasse 95447 Bayreuth GERMANY Eniko.Bali@uni-bayreuth.deDr. Banks David Earth and Environment University of Leeds Woodhouse Lane LS2 9JT Leeds USA D.Banks@see.leeds.ac.ukMrs. Baumgartner Miriam Applied Geosciences andGeophysicsMr. Bell Aaron Geosciences University of NevadaLas VegasDr. Bento dosSantosUniversity of Leoben Peter-Tunner-Str. 5 A-8700 Leoben AUSTRIA miriam.baumgartner@mu-leoben.at4505 MarylandParkwayTelmo Centro de Geologia Universidade de Lisboa Ed. C6, Piso 2,6.2.70, CampoProf. Berkesi Marta Lithosphere FluidResearch Lab, Petrologyand GeochemistryEötvös LorándUniversityDr. Blamey Nigel Department of Chemistry National University ofIrelandDr. Bodnar Robert Geosciences Virginia Tech StateUniversityDr. Boiron Marie-ChristinePázmány Péter stny1/C89154-40101749-016Las Vegas UNITED STATES bella19@unlv.nevada.eduLisbon PORTUGAL tmsantos@fc.ul.pt1117 Budapest HUNGARY marta.berkesi@gmail.comUniversity Avenue Galway IRELAND Nigel.Blamey@nuigalway.ie4044 Derring Hall 24061 Blacksburg,VirginiaG2R-CREGU Nancy University BP 239 54506 Vandoeuvreles NancycedexUNITED STATES rjb@vt.eduFRANCE marie-christine.boiron@g2r.uhpnancy.frMrs. Bozkaya Gülcan Geological Engineering Cumhuriyet University Kayseri Street 58140 Sivas TURKEY gulcan.bozkaya@gmail.comDr. Brennan Sean Eastern Energy ResourcesTeamU.S. Geological Survey MS 956, 12201Sunrise Valley DMr. Burlinson Kingsley KJUH Burlinson GeochemicalServices p/lProf. Canals Angels Cristal.lografia, Mineralogiai Dipòsits MineralsUniversitat deBarcelona20192 Reston UNITED STATES sbrennan@usgs.govPO 37134 821 Winnellie AUSTRALIA kgb@synix.com.auC. Martí i Franquès s/n08028 Barcelona SPAIN angelscanals@ub.edu286

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 287Mrs. Cannatelli Claudia Geosciences Virginia Tech StateUniversityMr. Castelain Teddy School of Earth &Environment4044 Derring Hall 24061 Blacksburg,VirginiaUniversity of Leeds Woodhouse Lane LS236RPDr. Cathelineau Michel G2R-CREGU Nancy University BP 239 54506 Vandoeuvreles NancycedexLeeds UNITEDKINGDOMUNITED STATES claudiac@vt.edut.castelain@see.leeds.ac.ukFRANCE michel.cathelineau@g2r.uhp-nancy.frDr. Cauzid Jean ID 22 Experiment Division ESRF 6 Rue Jules Horowitz 38043 Grenoble FRANCE jean.cauzid@esrf.frDr. Cline Jean Geoscience University of NevadaLas VegasMr. Conliffe James Department of Earth andOcean SciencesMr. de Gier Fred EPT-SCF Shell InternationalExploration andProductionMrs. Dégi Júlia Petrology andGeochemistryDr. Di Martino Corrado Department of Earth andGeo-EnvironmentalSciencesProf. Diamond Larryn W. Institute of GeologicalSciences4505 MarylandParkway, Box 45489154-4010Las Vegas UNITED STATES jean.cline@unlv.eduNUI, Galway University Road Galway IRELAND j.conliffe1@nuigalway.ieEötvös LorándUniversityDr. Doria Armanda Dep. of Geology Faculty of SciencesPorto UniversityDr. Driesner Thomas Isotope Geochemistry andMineral ResourcesProf. Duan Zhenhao Institute of Geology andGeophysicsKessler Park 1 2288 GS Rijswijk NETHERLANDS fred.degier@shell.comPázmány Péter stny1/CUniversity of Bologna Piazza di Porta sanDonato, 11117 Budapest HUNGARY degi@freemail.hu40126 Bologna ITALY corrado.dimartino@unibo.itUniversity of Bern Baltzerstrasse 1,3 3012 Bern SWITZERLAND diamond@geo.unibe.chRua do CampoAlegre 6874169-007Porto PORTUGAL adoria@fc.up.ptETH Zürich Clausiusstrasse 25 8092 Zürich SWITZERLAND thomas.driesner@erdw.ethz.chChinese Academy ofSciencesDr. Dubessy Jean G2R-CREGU Nancy University BP 239 54506 Vandoeuvreles NancycedexDr. Dublyansky Yuri Institut für Geologie undPalontologieLeopold-Franzens-Universität InnsbruckProf. Dubois Michel UMR/CNRS PBDS University of Lille UFR Sciences de laTerreMr. Esposito Rosario Geosciences Virginia Tech StateUniversity19 Beitucheng Road 100029 Beijing CHINA duanzhenhao@gmail.comFRANCE jean.dubessy@g2r.uhp-nancy.frInnrain 52 6020 Innsbruck AUSTRIA Juri.Dublyanski@uibk.ac.at705 Appalachian dr#659655 Villeneuved’AscqDr. Fabre Cécile G2R-CREGU Nancy University BP 239 54506 Vandoeuvreles NancycedexMr. Fall András Geosciences Virginia Tech StateUniversity4044 Derring Hall 24061 Blacksburg,VirginiaFRANCE Michel.Dubois@univ-lille1.fr24060 Blacksburg UNITED STATES rosario@vt.eduFRANCE cecile.fabre@g2r.uhp-nancy.frUNITED STATES afall@vt.edu287

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 288Dr. Fedele Luca Geosciences Virginia Tech StateUniversityMrs. Felker -KóthayKlára Department of Petrologyand GeochemistryMr. Fintor Krisztián Department of MineralogyGeochemistry andPetrologyProf. Fonarev Viacheslav Laboratory ofMetamorphismProf. Frezzotti Maria Luce Dipartimento Scienze dellaTerraEötvös LorándUniversity4044 Derring Hall 24061 Blacksburg,VirginiaPázmány Péter stny1/CUNITED STATES lfedele@vt.edu1117 Budapest HUNGARY klara.kothay@t-online.huUniversity of Szeged Egyetem u. 2-6 6722 Szeged HUNGARY fintor@geo.u-szeged.huInstitute ofExperimentalMineralogy RASAcademy of sciences 142432 ChernogolovkaRUSSIANFEDERATIONfonarev@iem.ac.ruUniversità di Siena Via Laterina 8 53100 Siena ITALY frezzottiml@unisi.itMr. Fricker Mattias D-CHAB ETH Zürich Wolgang-Pauli-Str. 10 8093 Zürich SWITZERLAND fricker@inorg.chem.ethz.chDr. Garofalo Paolo Dipartimento Scienze dellaTerra e Geologico-AmbientaliDr. Gilg H. Albert Lehrstuhl fürIngenieurgeologieUniversit di Bologna Piazza Porta S.Donato, 1Technische UniversitätMünchen40126 Bologna ITALY paolo.garofalo@unibo.itArcisstr. 21 80333 München GERMANY agilg@tum.deProf. Goldstein Robert Geology University of Kansas 1475 Jayhawk Blvd 66045 Lawrence, KS USA gold@ku.eduMrs. Graser Gesa Institut fürGeowissenschaften, ABMineralogie undGeodynamikDr. Grishin Yury Institute of Geology,Mineralogy andPetrographyDr. Grishina Svetlana Institute of Geology,Mineralogy andPetrographyEberhard-KarlsUniversität TübingenSiberian Branch ofRussian Academy ofSciencesSiberian Branch ofRussian Academy ofSciencesDr. Guedes Alexandra Geology University of Porto R. Campo Alegre,687Dr. Guillaume Damien LMTG OMP 14 Avenue EdouardBelinWilhelmstrasse 56 72074 Tübingen GERMANY gesa.graser@uni-tuebingen.deKoptyuga avn. 630090 Novosibirsk RUSSIANFEDERATIONKoptyuga avn. 630090 Novosibirsk RUSSIANFEDERATION4169-007grishina@uiggm.nsc.rugrishina@uiggm.nsc.ruPorto PORTUGAL aguedes@fc.up.pt31400 Toulouse FRANCE damien.guillaume@lmtg.obs-mip.frDr. Guillong Marcel D-ERDW, IGMR ETH Zürich Clausiusstr. 25 8092 Zürich SWITZERLAND guillong@erdw.ethz.chMr. Guzmics Tibor Lithosphere FluidResearch Lab, Institute ofGeography and EarthSciencesProf. Hagemann Steffen Centre for ExplorationTargetingEötvös LorándUniversityUniversity of WesternAustraliaProf. Hanchar John Dept. of Earth Sciences Memorial University ofNewfoundlandPázmány Péter stny1/CH-1117 Budapest HUNGARY tibor.guzmics@gmail.com2/77 Broadway 6009 Nedlands-WA AUSTRALIA shageman@cyllene.uwa.edu.auAlexander Murray Bu A1B 3X5 St. John’s CANADA johnh@esd.mun.ca288

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 289Dr. Hanley Jacob Isotope Geochemistry andMineral ResourcesETH Zürich Clausiusstrasse 25 8092 Zürich SWITZERLAND hanley@erdw.ethz.chMrs. Harris Caroline IGMR ETH Zürich Clausiusstrasse 25 8092 Zürich SWITZERLAND harris@erdw.ethz.chMrs. Havancsák Izabella Department of Petrologyand GeochemistryDr. Heijboer Tjerk Institut de Géochimie etMinéralogieProf. Heinrich ChristophA.Department of EarthSciencesMrs. Hennings Sibylle Structural Geology &GeodynamicsDr. Herms Petra Institut fürGeowissenschaftenMr. Hidas Károly Lithosphere FluidResearch Lab, Institute ofGeography and EarthSciencesEötvös LorándUniversityPázmány Péter stny1/CH-1117 Budapest HUNGARY havancsaki@gmail.comUniversité de Lausanne Antropole 1015 Lausanne SWITZERLAND tjerk.heijboer@unil.chETH Zürich Clausiusstr. 25 8092 Zürich SWITZERLAND heinrich@erdw.ethz.chGeoscience Centre,University of GöttingenEbellstr. 22 30625 Hannover GERMANY shennings@gmx.netUniversity of Kiel Olshausenstr. 40 24098 Kiel GERMANY ph@min.uni-kiel.deEötvös LorándUniversityPázmány Péter stny1/CDr. Hu Fang Fang D-CHAB ETH Zürich Wolfgang-Pauli-Str.10Dr. Hurai Vratislav Geological Institute Slovak Academy ofSciencesDubravska cesta 9,P.O. Box 10Dr. Invernizzi Chiara Dept.Scienze delle Terra University of Camerino via Gentile III daVaranoDr. Jarmolowicz-SzulcKatarzyna Center of Excellence Polish GeologicalInstituteProf. Mullis Josef Mineralogisch-Petgrographisches InstitutMr. Kainrath Peter Aufschuss- undAnalysentechnikMrs. Köhler Jasmin Institut fürGeowissenschaften, ABMineralogie undGeodynamikDr. Kodera Peter Geology of MineralDepositsMr. Kodolányi János Institute of GeologicalSciencesMr. Konc Zoltan Lithosphere FluidResearch Lab, Institute ofGeography and EarthSciencesH1117 Budapest HUNGARY karoly.hidas@gmail.com8093 Zürich SWITZERLAND ffhu11@yahoo.com.cn840 05 Bratislava SLOVAKIA vratislav.hurai@savba.sk62032 Camerino(MC)ITALY chiara.invernizzi@unicam.it4 Rakowiecka 00-975 Warsaw POLAND katarzyna.jarmolowicz-szulc@pgi.gov.plUniversität Basel Bernoullistrasse 30 4056 Basel SWITZERLAND josef.mullis@unibas.chS-Prep GmbH Im Amann 7 88662 Überlingen GERMANY kainrath@s-prep.comEberhard-KarlsUniversität TübingenWilhelmstrasse 56 72074 Tübingen GERMANY jasmin.koehler@uni-tuebingen.deComenius University Mlynska Dolina 842 15 Bratislava SLOVAKIA kodera@fns.uniba.skUniversity of Bern Baltzerstrasse 1,3 3012 Bern SWITZERLAND janos@geo.unibe.chEötvös LorándUniversityPázmány Péter stny1/CH1117 Budapest HUNGARY zoltan.konc@gmail.com289

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 290Prof. Kotelnikova Zoya Institute of Geology of OreDeposits, Petrography,Mineralogy, andGeochemistryDr. Kouzmanov Kalin Department of Mineralogy,Section des Sciences de laTerreAcademy of Sciences Staromonetny per.,35University of Geneva Rue des Maraîchers,13Dr. Krause Petra Tyne + Wear CETAC Technologies 242, BamburghAvenueDr. Krüger Yves LFA-Labor fürFluideinschluss-AnalytikProf. Kyle J. Richard Dept. of GeologicalSciencesMr. Lawrence David M. Geography and EarthScienceDr. Lledo Haroldo Geoscience University of Nevada,Las VegasUniv. of Texas at Austin 1 University Station,C1100119017 Moscow RUSSIANFEDERATIONgirnis@igem.ru1205 Geneva SWITZERLAND kalin.kouzmanov@terre.unige.chNE333HXSouth Shields UNITEDKINGDOMpkrause@cetac.comCäcilienrain 3 3007 Bern SWITZERLAND lfa@fluidinclusion.chKingston University Penrhyn Road KT12EE Kingston-Upon-Thames4505 MarylandParkway78712 Austin, Texas UNITED STATES rkyle@mail.utexas.edu89154-4010UNITEDKINGDOMk0638949@kingston.ac.ukLas Vegas UNITED STATES Haroldo.Lledo@UNLV.eduDr. Lüders Volker GFZ Potsdam Telegrafenberg 14473 Potsdam GERMANY volue@gfz-potsdam.deDr. Luptáková Jarmila Geological Institute Slovak Academy ofSciencesDr. Macleod Gordon Geochemistry S-130 ExxonMobil UpstreamResearchSeverna 5 974 01 BanskaBystricaSLOVAKIA luptakova@savbb.sk3319 Mercer Street 77027 Houston UNITED STATES gordon.macleod@exxonmobil.comMrs. Malsy Anna Gübelin Gem Lab Ltd. Maihofstrasse 102 6006 Luzern SWITZERLAND a.malsy@gubelingemlab.chProf. Marshall Dan Earth Sciences Simon FraserUniversityMr. Marton Istvan Department of Mineralogy University of Geneva Rue des Maraîchers,13Dr. Moritz Robert Section des Sciences de laTerreMr. Mutchler Scott Geosciences Virginia Tech StateUniversityDr. Naumov Vladimir Vernadsky Institute ofGeochemistry andAnalytical ChemistryUniversité de Genève Rue des Maraîchers,13Prof. Noronha Fernando Departamento de Geologia Universidade do Porto Rua do CampoAlegre,Mrs. Painsi Monika Institute of GeologicalSciencesDr. Petersen KlausJuergenCET/SEGS University of WesternAustralia8888 University Dr V5A 1S6 Burnaby CANADA marshall@sfu.ca4044 Derring Hall 24061 Blacksburg,Virginia1205 Geneva SWITZERLAND istvan.marton@terre.unige.ch1205 Genève SWITZERLAND robert.moritz@terre.unige.chAcademy of Sciences Kosygina, 19 119991 Moscow RUSSIANFEDERATION4169-007UNITED STATES srm@vt.edunaumov@geokhi.ruPorto PORTUGAL fmnoronh@fc.up.ptUniversity of Bern Baltzerstrasse 1,3 3012 Bern SWITZERLAND Monika.Painsi@geo.unibe.ch35 Stirling Highway 6009 Crawley AUSTRALIA kjpeters@cyllene.uwa.edu.au290

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 291Prof. Pettke Thomas Institute of GeologicalSciencesDr. Potter Joanna Department of EarthSciencesProf. Prokofiev Vsevolod Russian Academy ofSciencesMr. Ramos-RosiqueUniversity of Bern Baltzerstrasse 1,3 3012 Bern SWITZERLAND pettke@geo.unibe.chUniversity of WesternOntarioN6A 5B7 London,OntarioIGEM RAS Staromonetny, 35 119017 Moscow RUSSIANFEDERATIONCANADA jpotter6@uwo.cavpr@igem.ruAldo CGEO UNAM Campus Juriquilla 76000 Queretaro MEXICO aldoramro@gmail.comProf. Rankin Andrew Earth Sciences andGeographyKingston University Penrhyn Road KT1 2EE KingstonUpon ThamesMr. Richard Antonin G2R-CREGU Nancy University BP 239 54506 Vandoeuvreles NancycedexUNITEDKINGDOMa.rankin@kingston.ac.ukFRANCE antonin.richard@g2r.uhp-nancy.frDr. Rickers Karen HASYLAB DESY Notkestrasse 85 22603 Hamburg GERMANY karen.rickers@desy.deDr. Ridley John Department ofGeosciencesDr. Ruggieri Giovanni Institute of Geosciencesand Earth ResourcesMr. Rykkje JohannesMohrProf. Salvador Morales-RuanoProf. Sanchez-Valle Carmen Institute for Mineralogy andPetrologyProf. Scambelluri Marco Dipartimento per lo Studiodel Territorio e delle sueRisorseDr. Schmidt Christian Department 4: Chemie derErdeMr. SchoenenbergerColorado StateUniversityCO80523Fort Collins UNITED STATES jridley@warnercnr.colostate.eduCNR Via La Pira 4 50121 Florence ITALY ruggieri@igg.cnr.itLaboratory & Analysis Norsk Hydro, O&E Sandsliveien 90 5020 Bergen NORWAY johannes.m.rykkje@hydro.comMineralogy & Petrology University of Granada AvenidaFuentenueva, s/nJohannes Institut fürGeowissenschaften, ABMineralogie undGeodynamik18002 Granada SPAIN smorales@ugr.esETH Zürich Clausiusstrasse 25 8092 Zürich SWITZERLAND carmen.sanchez@erdw.ethz.chUniversita’ di Genova Corso Europa 26 16132 Genova ITALY marco.scambelluri@dipteris.unige.itGeo ForschungsZentrum PotsdamDr. Sekine Kotaro Institute of Fluid Science Tohoku University 2-1-1, Katahira,Aoba-kuMrs. Sezerer Kuru Gülay General Directorate ofMineral Research andExplorationTelegrafenberg 14473 Potsdam GERMANY hokie@gfz-potsdam.deMr. Siebenaller Luc G2R-CREGU Nancy University BP 239 54506 Vandoeuvreles NancycedexUniversität Tübingen Wilhelmstr. 56 72074 Tübingen GERMANY johannes.schoenenberger@unituebingen.de980-8577Sendai JAPAN ksekine@ifs.tohoku.ac.jpEskisehirroad street 6520 Ankara TURKEY sezererkuru@yahoo.comFRANCE luc.siebenaller@g2r.uhp-nacy.fr291

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 292Mrs. Silva Rosalina Departamento de Geologia UFMG Av. Antnio Carlos 6627 Pampulha-BeloHorizonteProf. Simmons Stuart School of Geography,Geology, andEnvironmental ScienceDr. Simon Adam Geoscience University of NevadaLas VegasMrs. Small Penelope School of Earth Scienceand GeographyDr. Sokolov Stanislav Federal Agency of MineralResourcesProf. Solovova Irina Institute of Ore Deposits,Petrography, Mineralogyand GeochemistryUniversity of Auckland Private Bag 92019,Auckland Ma4505 MarylandParkwayAll-Russia Institute ofMineral Resources(VIMS)Russian Academy ofSciencesStaromonetnyi per.31BRAZIL rosalinecris@yahoo.com.br1149 Auckland NEW ZEALAND sf.simmons@auckland.ac.nz89154 Las Vegas UNITED STATES adam.simon@unlv.eduUNITEDKINGDOM119017 Moscow RUSSIANFEDERATIONStaromonetny, 35 119017 Moscow RUSSIANFEDERATIONpenelope.small@gmail.comvims-sokol@mail.rugirnis@igem.ruDr. Sosa Graciela Geology University of Göttingen Lehnshof 5 37079 Göttingen GERMANY gsosa@t-online.deDr. Spandler Carl Institute of GeologicalSciencesProf. Spooner Ed Geology University of Toronto 22 Russell St. M5S3B1Mr. Staude Sebastian Institut fürGeowissenschaften, ABPetrologie undGeodynamikUniversity of Bern Baltzerstrasse 1,3 3012 Bern SWITZERLAND spandler@geo.unibe.chKingston University Penrhyn Road KT1 2EE Kingstonupon-ThamesEberhard-Karls-Universität TübingenTORONTO CANADA etcs@geology.utoronto.caWilhelmstrasse 56 72074 Tübingen GERMANY sebastian.staude@uni-tuebingen.deDr. Stoller Patrick Institute of Applied Physics University of Bern Sidlerstrasse 5 3012 Bern SWITZERLAND patrick.stoller@iap.unibe.chProf. Szabó Csaba Lithosphere FluidResearch Lab, Petrologyand GeochemistryDr. Szabó Barbara Department of Mineralogy,Geochemistry andPetrologyDr. Tarantola Alexandre Institute of GeologicalSciencesDr. Tecce Francesca Istituto GeologiaAmbientale eGeoingegneriaEötvös LorándUniversityDr. Török Kálmán Geophysical Institute Eötvös LorándUniversityPázmány Péter stny1/C1117 Budapest HUNGARY cszabo@elte.huUniversity of Szeged Egyetem utca 2-6. 6701 Szeged HUNGARY szabob@geo.u-szeged.huUniversity of Bern Baltzerstrasse 1,3 3012 Bern SWITZERLAND alexandre.tarantola@geo.unibe.chCNR p.le A.Moro 5 185 Roma ITALY francesca.tecce@igag.cnr.itKolumbusz ucta 17-23Dr. Tritlla Jordi Centro de Geociencias UNAM Carr. Qro-SLP km15,51145 Budapest HUNGARY torokklm@elgi.hu76230 Queretaro MEXICO jordit@geociencias.unam.mx292

European Current Research on Fluid Inclusions (ECROFI-XIX)University of Bern, Switzerland, 17–20 July, 2007. Abstract Volume, p. 293Dr. Van denKerkhofMrs. Veselinovic-WilliamsAlfons Applied Geology University of Göttingen Goldschmidtstrasse 3 37077 Göttingen GERMANY akerkho@gwdg.deMilica Earth Sciences andGeographyMrs. Vry Victoria Earth Science andEngineeringKingston University Penrhyn Road KT1 2EE Kingston uponThamesImperial CollegeLondon16 Hillworth Road SW22DYMr. Williams Curtis Geological Sciences Indiana University 1001 east TenthStreetUNITEDKINGDOMLondon UNITEDKINGDOMm.v.williams@kingston.ac.ukv.vry06@imperial.ac.uk47405 Bloomington USA cuwillia@indiana.eduMr. Woodard Jeremy Department of Geology University of Turku YO-Kyl 26A2 20540 Turku FINLAND jdwood@utu.fiDr. Zacharias Jiri Institute of Geochemistry,Mineralogy and MineralResourcesMr. Zajacz Zoltán Institute of IsotopeGeochemistry and MineralResourcesDr. Ziemann Martin A. Institut fürGeowissenschaftenCharles University inPragueAlbertov 6 12843 Prague CZECHREPUBLICzachar@natur.cuni.czETH Zürich Clausiusstrasse 25 8092 Zürich SWITZERLAND zajacz@erdw.ethz.chUniversität Potsdam Karl-Liebknecht-Str.24 / H2714476 Potsdam-GolmGERMANY ziemann@geo.uni-potsdam.de293

ECROFI-XIX CONFERENCE SCHEDULETuesday 17 July Wednesday 18 July Thursday 19 July Friday 20 July08:15 Opening of Conference08:3008:45 ORAL:09:00 Theoretical Studies09:1509:3009:45 ORAL:Experimental I:10:00Synthetic10:15 Fluid Inclusions10:3010:45Refreshments11:0011:1511:3011:4512:0012:1512:30ORAL:Magmatic-HydrothermalOre Deposits IORAL:Experimental II:DiamondAnvil CellORAL:Analytical Methods I:Non-destructiveRefreshmentsORAL:Magmatic-HydrothermalOre Deposits IIORAL:Analytical Methods II:Laser Ablation ICPMSORAL:Mineral depositsRefreshmentsORAL:“Non-Magmatic”Ore DepositsORAL:EpithermalOre DepositsRefreshmentsDay 4Poster Session12:45 Lunch13:00 Lunch Lunch Lunch13:1513:3013:4514:00ORAL:14:15MagmatismORAL:14:30Diagenesis IDay 214:45 Poster Session ORAL:15:00Tribute to Ed Roedder15:1515:30ORAL:Refreshments15:45Tectonics16:00Banquet events16:1516:30Refreshments ORAL:16:45Mantle17:0017:1517:30Day117:45 Poster Session18:0018:15Petrography WorkshopORAL:Deep fluidsRefreshmentsORAL:Diagenesis IIPlenary Discussion18:30 Closure of18:45Conference