Relevant bibliographies by topics / Fluid inclusion

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  1. Journal articles
  2. Dissertations / Theses
  3. Books
  4. Book chapters
  5. Conference papers
  6. Reports

Academic literature on the topic 'Fluid inclusion'

Author: Grafiati
Published: 4 June 2021
Last updated: 15 June 2025

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Journal articles on the topic "Fluid inclusion"

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Huang, Wenqing, Pei Ni, Jungui Zhou, et al. "Fluid Inclusion and Titanite U-Pb Age Constraints on the Yuanjiang Ruby Mineralization in the Ailao Shan-Red River Metamorphic Belt, Southwest China." Canadian Mineralogist 60, no. 1 (2022): 3–28. http://dx.doi.org/10.3749/canmin.2100009.

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ABSTRACT The Yuanjiang marble-hosted ruby deposit lies in the central segment of the Ailao Shan metamorphic massif of the Ailao Shan-Red River metamorphic belt. The mineralizing fluid and age were characterized by detailed petrography, Raman spectroscopy, microthermometry, and in situ titanite laser ablation-inductively coupled plasma-mass spectrometry dating. Some fluid inclusions in the corundum show an interesting morphology with a diaspore crystal fully separating the whole inclusion into two smaller inclusions. This morphological feature can be explained by morphological ripening and subsequent reactions between the trapped H2O and the host corundum during the cooling of the inclusion. Fluid inclusions in the ruby belong to the system CO2–H2S–COS–S8–H2S2–CH4–AlO(OH) with various daughter minerals, including diaspore, gibbsite, and native sulfur (S8). The observed seven-component fluid inclusion composition can be explained by two steps: (1) original fluid inclusion capture during deposit formation with compositions including CO2, H2S, COS, CH4, S8, and H2S2, and (2) post-entrapment fluid inclusion modification, such as diaspore and gibbsite. The presence of hydrous minerals in fluid inclusions strongly supports the idea that water was once present in the initial fluids. In the Yuanjiang deposit, petrographic evidence shows that titanite formed simultaneously with ruby, and U-Pb dating of titanite allows us to conclude that the ruby mineralization formed at 23.4 ± 0.3 Ma, in other words during the Himalayan orogeny.
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Zolensky, Michael E., Robert J. Bodnar, Hisayoshi Yurimoto, et al. "The search for and analysis of direct samples of early Solar System aqueous fluids." Philosophical Transactions of the Royal Society A: Mathematical, Physical and Engineering Sciences 375, no. 2094 (2017): 20150386. http://dx.doi.org/10.1098/rsta.2015.0386.

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We describe the current state of the search for direct, surviving samples of early, inner Solar System fluids—fluid inclusions in meteorites. Meteoritic aqueous fluid inclusions are not rare, but they are very tiny and their characterization is at the state of the art for most analytical techniques. Meteoritic fluid inclusions offer us a unique opportunity to study early Solar System brines in the laboratory. Inclusion-by-inclusion analyses of the trapped fluids in carefully selected samples will, in the immediate future, provide us detailed information on the evolution of fluids as they interacted with anhydrous solid materials. Thus, real data can replace calculated fluid compositions in thermochemical calculations of the evolution of water and aqueous reactions in comets, asteroids, moons and the terrestrial planets. This article is part of the themed issue ‘The origin, history and role of water in the evolution of the inner Solar System’.
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Van den Kerkhof, Alfons M., and Ulrich F. Hein. "Fluid inclusion petrography." Lithos 55, no. 1-4 (2001): 27–47. http://dx.doi.org/10.1016/s0024-4937(00)00037-2.

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Brown, Philip E. "Fluid inclusion research." Geochimica et Cosmochimica Acta 61, no. 10 (1997): 2149–50. http://dx.doi.org/10.1016/s0016-7037(97)83227-9.

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Brown, Philip E. "Fluid inclusion research." Geochimica et Cosmochimica Acta 61, no. 10 (1997): 2149. http://dx.doi.org/10.1016/s0016-7037(97)90192-7.

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Brown, Philip E. "Fluid inclusion research." Geochimica et Cosmochimica Acta 61, no. 10 (1997): 2149. http://dx.doi.org/10.1016/s0016-7037(97)90193-9.

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Brown, Philip E. "Fluid inclusion research." Geochimica et Cosmochimica Acta 61, no. 10 (1997): 2149. http://dx.doi.org/10.1016/s0016-7037(97)90194-0.

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FOSTER, R. P. "Fluid inclusion studies." Journal of the Geological Society 145, no. 1 (1988): 137–38. http://dx.doi.org/10.1144/gsjgs.145.1.0137.

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Moritz, Robert P. "Fluid inclusion research." Geochimica et Cosmochimica Acta 52, no. 6 (1988): 1743. http://dx.doi.org/10.1016/0016-7037(88)90247-5.

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Moritz, Robert P., and Serge R. Chevé. "Fluid-inclusion studies of high-grade metamorphic rocks of the Ashuanipi complex, eastern Superior Province: constraints on the retrograde P–T path and implications for gold metallogeny." Canadian Journal of Earth Sciences 29, no. 10 (1992): 2309–27. http://dx.doi.org/10.1139/e92-180.

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The high-grade metamorphic rocks of the Ashuanipi complex have been the subject of a microthermometric fluid-inclusion study. Four types of fluid inclusions were observed: CO2-rich fluids; low-temperature, high-salinity H2O fluids; CH4 ± N2-rich fluids; and high-temperature, low-salinity H2O fluids. The regionally distributed CO2-rich fluids are the earliest fluids, and their calculated isochores indicate a clockwise post-peak metamorphic P–T–t path for the Ashuanipi complex. The low-temperature, high-salinity aqueous fluid inclusions are also distributed regionally and can be interpreted as late brines, retrograde metamorphic fluids, or the wicked-off aqueous component of H2O–CO2 fluid inclusions. Both CH4 ± N2-rich fluids and the high-temperature, low-salinity aqueous fluid inclusions were found only locally in gold-bearing metamorphosed banded iron formations. Fluid-inclusion microthermometry, arsenopyrite thermometry, and metamorphic petrologic study at Lac Lilois, one of the principal gold showings, suggest that some gold deposition may have occurred during regional post-peak metamorphic exhumation and cooling at P–T conditions near the amphibolite–greenschist transition. However, it is possible that gold deposition began at higher near-peak metamorphic P–T conditions. Another major gold showing, Arsène, is characterized by CH4 ± N2-rich fluid inclusions, tentatively inferred to be either directly related to gold deposition or responsible for secondary gold enrichment. The association of CH4 ± N2-rich fluids with gold occurrences in the Ashuanipi complex is comparable to gold deposits of the Abitibi greenstone belt and of Wales, Finland, and Brazil.
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Dissertations / Theses on the topic "Fluid inclusion"

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Becker, Stephen Paul. "Fluid Inclusion Characteristics in Magmatic-Hydrothermal Ore Deposits." Diss., Virginia Tech, 2007. http://hdl.handle.net/10919/28318.

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Magmatic-hydrothermal ore deposits are formed in association with aqueous fluids that exsolve from hydrous silicate melts during ascent and crystallization. These fluids are invariably trapped as inclusions in vein-filling minerals associated with hydrothermal fluid flow, and their composition may be modeled based on the H₂O-NaCl system. Thus, if we know the pressure-volume-temperature-composition (PVTX) properties of H₂O-NaCl solutions, it is possible to interpret the PTX trapping conditions, which is important for understanding the processes leading to the generation of the hydrothermal system and ore mineralization. High salinity (> 26 wt. % NaCl) fluid inclusions contain liquid, vapor, and halite at room temperature, and are common in magmatic-hydrothermal ore deposits. These inclusions homogenize in one of three ways: A) halite disappearance (Tmhalite) followed by liquid-vapor homogenization (ThL-V), B) simultaneous ThL-V and Tmhalite, or C) ThL-V followed by Tmhalite. The PVTX properties of H₂O-NaCl solutions three phase (L+V+H) and liquid-vapor (L+V) phase boundaries are well constrained, allowing researchers to interpret the minimum trapping pressure of inclusion types A and B. However, data that describe the pressure at Tmhalite for inclusion type C are limited to a composition of 40 wt. % NaCl. To resolve this problem, the synthetic fluid inclusion technique was used to determine the relationship between homogenization temperature and minimum trapping pressure for inclusions that homogenize by mode C. These results allow researchers to interpret the minimum trapping pressure of these inclusions, and by extension the depth at which the inclusions formed. The temporal and spatial distribution of fluid inclusions formed in associated with porphyry copper mineralization has been predicted using a computer model. A simple geologic model of an epizonal intrusion was developed based on a Burnham-style model for porphyry systems and thermal models of the evolution of epizonal intrusions. The phase stability fields and fluid inclusion characteristics at any location and time were predicted based on PVTX properties of H₂O-NaCl solutions. These results provide vectors towards the center of a magmatic-hydrothermal system that allow explorationists to use fluid inclusion petrography to predict position with the overall porphyry environment when other indicators of position are absent.<br>Ph. D.
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Henderson, Iain Henry Campbell. "Fluid pressure variations in quartz veins, Pyrenees, France : fluid inclusion and cathodoluminescence studies." Thesis, University of Leeds, 1994. http://ethos.bl.uk/OrderDetails.do?uin=uk.bl.ethos.483635.

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Huff, Timothy A. "Fluid inclusion evidence for metamorphic fluid evolution in the Black Hills, South Dakota /." free to MU campus, to others for purchase, 2004. http://wwwlib.umi.com/cr/mo/fullcit?p1421144.

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Fall, Andras. "Application of fluid inclusions in geological thermometry." Diss., Virginia Tech, 2008. http://hdl.handle.net/10919/30265.

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Many geologic processes occur in association with hydrothermal fluids and some of these fluids are eventually trapped as fluid inclusions in minerals formed during the process. Fluid inclusions provide valuable information on the pressure, temperature and fluid composition (PTX) of the environment of formation, hence understanding PTX properties of the fluid inclusions is required. The most important step of a fluid inclusion study is the identification of Fluid Inclusion Assemblages (FIA) that represent the finest (shortest time duration) geologic event that can be constrained using fluid inclusions. Homogenization temperature data obtained from fluid inclusions is often used to reconstruct temperature history of a geologic event. The precision with which fluid inclusions constrain the temperatures of geologic events depends on the precision with which the temperature of a fluid inclusion assemblage can be determined. Synthetic fluid inclusions trapped in the one-fluid-phase field are formed at a known and relatively constant temperature. However, microthermometry of synthetic fluid inclusions often reveals Th variations of about ± 1- 4 degrees Centigrade, or one order of magnitude larger than the precision of the measurement for an individual inclusion. The same range in Th was observed in well-constrained natural FIAs where the inclusions are assumed to have been trapped at the same time. The observed small variations are the result of the effect of the fluid inclusion size on the bubble collapsing temperature. As inclusions are heated the vapor bubble is getting smaller until the pressure difference between the pressure of the vapor and the confining pressure reaches a critical value and the bubble collapses. It was observed that smaller inclusions reach critical bubble radius and critical pressure differences at lower temperatures than larger inclusions within the same FIA. Homogenization temperature (Th) variations depend on many factors that vary within different geological environments. In order to determine minimum and acceptable Th ranges fro FIAs formed in different environments we investigated several geologic environments including sedimentary, metamorphic, and magmatic hydrothermal environments. The observed minimum Th ranges range from 1-4 degrees Centigrade and acceptable Th range from 5-25 degrees Centigrade. The variations are mostly caused by the fluid inclusion size, natural temperature and pressure fluctuations during the formation of an FIA and reequilibration after trapping. Fluid inclusions containing H₂O-CO₂-NaCl are common in many geologic environments and knowing the salinity of these inclusions is important to interpret PVTX properties of the fluids. A technique that combines Raman spectroscopy and microthermometry of individual inclusions was developed to determine the salinity of these inclusions. In order to determine the salinity, the pressure and temperature within the inclusion must be known. The pressure within the inclusions is determined using the splitting in the Fermi diad of the Raman spectra of the CO₂ at the clathrate melting temperature. Applying the technique with to synthetic fluid inclusions with known salinity suggests that the technique is valid and useable to determine salinity of H₂O-CO₂-NaCl fluid inclusions with unknown salinity.<br>Ph. D.
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Stoffell, B. "Metal transport and deposition in hydrothermal fluids : insights from laser ablation microanalysis of individual fluid inclusion." Thesis, Imperial College London, 2007. http://ethos.bl.uk/OrderDetails.do?uin=uk.bl.ethos.504926.

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Schmatz, Joyce [Verfasser]. "Grain-boundary – fluid inclusion interaction in rocks and analogues / Joyce Schmatz." Aachen : Hochschulbibliothek der Rheinisch-Westfälischen Technischen Hochschule Aachen, 2011. http://d-nb.info/101649324X/34.

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Levasseur, Randy. "Fluid inclusion studies of rare element pegmatites, South Platte District, Colorado." Thesis, National Library of Canada = Bibliothèque nationale du Canada, 1997. http://www.collectionscanada.ca/obj/s4/f2/dsk2/ftp01/MQ30962.pdf.

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Westerman, Jonathan Mark. "Fluid inclusion planes in selected granitic rocks of the British Isles." Thesis, Kingston University, 1995. http://eprints.kingston.ac.uk/20590/.

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When hydrothermal fluids flow through microfractures in quartz, they effectively heal (anneal) them to produce Fluid Inclusion Planes (FIPs). These FIPs are viewed as a three dimensional plane or array of secondary fluid inclusions and may be used to relate brittle deformation associated with tectonic, thermal and hydraulic stresses to contemporaneous hydrothermal events. In this study, FIPs have been interpreted in granitic quartz from various geological settings. Analysis of the FIPs includes recording their orientation, the morphological characteristics of both the FIPs and the inclusions contained within them, together with the thermometric properties of the inclusions. Results show that FIPs may possess a preferential orientation over a wide area, similar to the trend of macrostructures observed in the field. However, local deviations in the stress field, related to the proximity of possible second order faults, may cause local deviations in the orientation of the FIPs. The presence of high FIP abundances has also been linked to the widespread, localised development of kaolinisation (possibly linked to tectonic stresses) and greisenisation (possibly linked to thermal and hydraulic stresses). These phenomena have been identified at several localities in the field areas. It is presumed that intense microfracture networks will allow the wide-spread movement of hydrothermal fluids allowing pervasive alteration. A classification scheme for FIPs has been devised, whereby FIPs may been classified as tensile, dilatant (mode 1) and dilatant shear (mode 2) fractures. This classification is based upon the orientation of the FIPs (to macro structures), their proposed origin and their morphology (both the FIP and the inclusions contained within them). Variation in inclusion morphology has been recorded within selected FIPs. Inclusions have been observed to occur parallel and perpendicular (rare) to the length of the FIP. The presence of a preferred shape orientation in the inclusions has been attributed to a combination of fracturing and subsequent healing process, with controlling parameters including the temperature and chemistry of the fluids (affecting crack lifetimes) together with the geometry of the fracture network.
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Christoula, Maria. "Fluid inclusion geochemistry of selected epigenetic, low temperature mineralization in the U.K." Thesis, Imperial College London, 2002. http://hdl.handle.net/10044/1/7326.

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Ting, Wupao. "A fluid and solid inclusion study of the Sukulu carbonatite complex, Uganda." Thesis, Kingston University, 1994. http://eprints.kingston.ac.uk/20577/.

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The thesis consists of 8 chapters. The first Chapter gives an introduction to carbonatites and outlines the general aims of this study. The general geology of Sukulu, the methodology used in this research, and previous work are presented in Chapter 2. Detailed descriptions and analytical results on the principal minerals are given in Chapter 3. Chapters 4 and 5 focus on aqueous and solid inclusions in apatite, and detailed descriptions, microthermometric results and interpretations are presented. Determination of oxygen and carbon stable isotope compositions and their interpretations are covered in Chapter 6. Chapter 7 describes geothermometric and geobarometric investigations and the calculation of oxygen fugacities during the deposition of apatite and carbonate. The final chapter discusses evolution of the fluids in the Sukulu carbonatite complex and presents a petrogenetic model. Aqueous inclusions in apatite from the Sukulu carbonatite consist essentially of three types: CO[sub]2-bearing, H[sub]2 0-rich and CH[sub]4-bearing. The CO[sub]2- and CH[sub]4-bearing inclusions, in general, are not present together in individual apatite crystals. It is considered that these compositionally discrete inclusions represent different fluids trapped during different stages of apatite crystallisation. The CO[sub]2-bearing fluid probably formed from an originally H[sub]2 0-rich fluid containing significant CO[sub]2 by immiscible separation under high pressure and temperature. This precursor H[sub]2 0-CO[sub]2 fluid was probably derived from a carbonatite melt, also by a possible process of liquid immiscibility. The CH[sub]4-bearing inclusions were probably formed by late stage hydrothermal processes under different P-T conditions. Many solid inclusions occur in apatite of the Sukulu carbonatite, of which the most abundant are carbonate. They can be classified into Mg-calcite. (primary) and calcite (secondary) inclusions based on their morphology, texture and chemical composition. Although such carbonate inclusions are ubiquitous in carbonatite apatite and have been described by many other workers, this study provides new insight into their genesis and petrogenetic significance. Carbon and oxygen stable isotopic composition from fluid inclusions, in both apatite and matrix carbonate, suggest that the CO[sub]2-bearing fluid was equilibrated with carbonate fluids at an early stage, but it evolved along a different path. The CO[sub]2-bearing fluids which has a stable isotopic composition close to upper-mantle values, evolved in a closed-system after being trapped by apatite, but the carbonate fluid evolved in an open-system and its isotopic composition was elevated by assimilation and contamination during ascent. The results also reveal that post-magmatic processes played an important role in the development of the Sukulu carbonatite. P-T-X isochores calculated for each type of fluid indicate that their evolution was probably from a CO[sub]2-bearing fluid, through a moderate to highly saline one, to a CH[sub]4-bearing one, and took place under temperatures and pressures varying from >1000°C and >7.4kb, through >560°C and >5kb, to about 500°C and <3 kb. This trend represents evolution of the carbonatite from a deep magmatic (carbonate melt) environment towards a shallow level hydrothermal system. This study confirms that both apatite and carbonate-can be precipitated over a wide range of temperatures and melt fluid compositions. The present findings indicate that the compositions of the fluids associated with the Sukulu carbonatite complex appear to have evolved chemically from a Mg-bearing calcite melt, through aqueous CO[sub]2-bearing and bicarbonate-rich melts (NaHC0[sub]3 daughters) to a final aqueous CH[sub]4-bearing fluid.
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Books on the topic "Fluid inclusion"

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L, Atwood J., Davies J. E. D, and MacNicol D. D, eds. Inclusion compounds. Oxford University Press, 1991.

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H, Rankin A., and Alderton D. H. M, eds. A practical guide to fluid inclusion studies. Blackie, 1985.

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Landis, Gary P. Anomalous low-density wolframite and fluid inclusion control of density, evidence from fluid inclusion content of water and carbon dioxide. Dept. of the Interior, U.S. Geological Survey, 1990.

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Landis, Gary P. Anomalous low-density wolframite and fluid inclusion control of density, evidence from fluid inclusion content of water and carbon dioxide. Dept. of the Interior, U.S. Geological Survey, 1990.

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Landis, Gary P. Anomalous low-density wolframite and fluid inclusion control of density, evidence from fluid inclusion content of water and carbon dioxide. Dept. of the Interior, U.S. Geological Survey, 1990.

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Landis, Gary P. Anomalous low-density wolframite and fluid inclusion control of density, evidence from fluid inclusion content of water and carbon dioxide. Dept. of the Interior, U.S. Geological Survey, 1990.

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G, Theodore Ted, Lowenstern Jacob B, and Geological Survey (U.S.), eds. Implications of fluid-inclusion motions in the Elder Creek porphyry copper system, Battle Mountain Mining District, Nevada. U.S. Dept. of the Interior, U.S. Geological Survey, 1996.

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G, Theodore Ted, Lowenstern Jacob B, and Geological Survey (U.S.), eds. Implications of fluid-inclusion motions in the Elder Creek porphyry copper system, Battle Mountain Mining District, Nevada. U.S. Dept. of the Interior, U.S. Geological Survey, 1996.

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Gostyayeva, Natalya. Implications of the fluid-inclusion motions in the Elder Creek porphyry copper system, Battle Mountain Mining District, Nevada. U.S. Dept. of the Interior, U.S. Geological Survey, 1996.

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Gostyayeva, Natalya. Implications of the fluid-inclusion motions in the Elder Creek porphyry copper system, Battle Mountain Mining District, Nevada. U.S. Dept. of the Interior, U.S. Geological Survey, 1996.

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Book chapters on the topic "Fluid inclusion"

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Dolson, John. "Using Fluid Inclusion Data in Exploration." In Understanding Oil and Gas Shows and Seals in the Search for Hydrocarbons. Springer International Publishing, 2016. http://dx.doi.org/10.1007/978-3-319-29710-1_7.

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Blamey, Nigel J. F., and Alan G. Ryder. "Hydrocarbon Fluid Inclusion Fluorescence: A Review." In Reviews in Fluorescence. Springer New York, 2009. http://dx.doi.org/10.1007/978-0-387-88722-7_13.

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Tazreiter, Claudia, Leanne Weber, Sharon Pickering, Marie Segrave, and Helen McKernan. "Processes of Reception and Inclusion in Australia." In Fluid Security in the Asia Pacific. Palgrave Macmillan UK, 2016. http://dx.doi.org/10.1057/978-1-137-46596-2_9.

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Mitchell, Thomas M., Jose M. Cembrano, Kazuna Fujita, et al. "Fluid Inclusion Evidence of Coseismic Fluid Flow Induced by Dynamic Rupture." In Fault Zone Dynamic Processes. John Wiley & Sons, Inc., 2017. http://dx.doi.org/10.1002/9781119156895.ch3.

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Hansteen, Thor H., and Andreas Klügel. "5. Fluid Inclusion Thermobarometry as a Tracer for Magmatic Processes." In Minerals, Inclusions And Volcanic Processes, edited by Keith D. Putirka and Frank J. Tepley III. De Gruyter, 2008. http://dx.doi.org/10.1515/9781501508486-006.

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Mekki, Mouna El, Claire Ramboz, Laurent Perdereau, Kirill Shmulovich, and Lionel Mercury. "Lifetime of Superheated Water in a Micrometric Synthetic Fluid Inclusion." In Metastable Systems under Pressure. Springer Netherlands, 2010. http://dx.doi.org/10.1007/978-90-481-3408-3_20.

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Quesnel, Benoît, Christophe Scheffer, and Georges Beaudoin. "The Light Stable Isotope (Hydrogen, Boron, Carbon, Nitrogen, Oxygen, Silicon, Sulfur) Composition of Orogenic Gold Deposits." In Isotopes in Economic Geology, Metallogenesis and Exploration. Springer International Publishing, 2023. http://dx.doi.org/10.1007/978-3-031-27897-6_10.

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AbstractOrogenic gold deposits formed in various terranes of most ages since the Paleoarchean and generally consist of quartz veins hosted in shear zones formed at the ductile brittle transition under greenschist to lower amphibolite metamorphic conditions. Vein mineralogy is dominated by quartz with various amounts of silicates, carbonates, phyllosilicates, borates, tungstates, sulfides, and oxides. The isotopic composition of these minerals and fluid inclusions has been investigated since the 1960s to constrain the characteristics of orogenic fluid systems involved in the formation of gold deposits worldwide. This review is based on 8580 stable isotope analyses, including δ18O, δD, δ13C, δ34S δ15N, δ11B, and δ30Si values, from 5478 samples from 558 orogenic gold deposits reported in the literature from 1960 to 2010. This contribution describes the variability of the light stable isotopic systems as function of the minerals, the age of the deposits, their regional setting, and their country rocks. The temperature of isotopic equilibrium of orogenic gold veins is estimated from mineral pairs for oxygen and sulfur isotopes. Based on these temperatures, and on fractionation between mineral and fluid components (H2O, CO2 and H2S), the isotopic composition of fluids is estimated to better constrain the main parameters shared by most of auriferous orogenic fluid systems. Orogenic gold deposits display similar isotopic features through time, suggesting that fluid conditions and sources leading to the formation of orogenic gold deposits did not change significantly from the Archean to the Cenozoic. No consistent secular variations of mineral isotope composition for oxygen (−8.1‰ ≤ δ18O ≤ 33‰, n = 4011), hydrogen (−187‰ ≤ δD ≤ −4‰, n = 246), carbon (−26.7‰ ≤ δ13C ≤ 12.3‰, n = 1179), boron (−21.6‰ ≤ δ11B ≤ 9‰, n = 119), and silicon (−0.5‰ ≤ δ30Si ≤ 0.8‰, n = 33) are documented. Only nitrogen (1.6‰ ≤ δ15N ≤ 23.7‰, n = 258) and sulfide sulfur from deposits hosted in sedimentary rocks (−27.2‰ ≤ δ34S ≤ 25‰, n = 717) display secular variations. For nitrogen, the change in composition is interpreted to record the variation of δ15N values of sediments devolatilized during metamorphism. For sulfur, secular variations reflect incorporation of local sedimentary sulfur of ultimate seawater origin. No significant variation of temperature of vein formation is documented for orogenic gold deposits of different ages. Quartz-silicate, quartz-carbonate and sulfide-sulfide mineral pairs display consistent temperatures of 360 ± 76 °C (1σ; n = 332), in agreement with the more common greenschist facies hostrocks and fluid inclusion microthermometry. Fluid sources for orogenic gold deposits are complex but the isotopic systems (hydrogen, boron, carbon, nitrogen, oxygen, sulfur) are most consistent with contributions from metamorphic fluids released by devolatilization of igneous, volcano-sedimentary and/or sedimentary rocks. The contribution of magmatic water exsolved from magma during crystallization is not a necessary component, even if permissible in specific cases. Isotopic data arrays can be interpreted as the result of fluid mixing between a high T (~550 °C)—high δ18O (~10‰)—low δD (~−60‰) deep-seated (metamorphic) fluid reservoir and a low T (~200 °C)—low δ18O (~2‰)—high δD (~0‰) upper crustal fluid reservoir in a number of orogenic gold deposits. The origin of the upper crustal fluid is most likely sea- or meteoric water filling the host rock porosity, with a long history of water–rock isotope exchange. Mixing of deep-seated and upper crustal fluids also explains the large variation of tourmaline δ11B values from orogenic gold veins. Regional spatial variations of oxygen and hydrogen isotope compositions of deep-seated fluid reservoirs are documented between orogenic gold districts. This is the case for the Val-d’Or (Abitibi), Coolgardie and Kalgoorlie (Yilgarn) where the oxygen isotope composition of the deep-seated fluid end-member is 4‰ lower compared to that from the Timmins, Larder Lake, and Kirkland Lake districts (Abitibi). However, both mixing trends converge towards a common, low δ18O upper crustal fluid end-member. Such variations cannot be related to fluid buffering at the site of deposition and suggest provinciality of the fluid source. The contribution of meteoric water is mainly recorded by fluid inclusions from Mesozoic and Cenozoic age deposits, but micas are not systematically in isotopic equilibrium with fluid inclusions trapped in quartz from the same vein. This suggests late involvement of meteoric water unrelated to deposit formation. Yet, a number of deposits with low δD mica may record infiltration of meteoric water in orogenic gold deposits. Isotope exchange between mineralizing fluid and country rocks is documented for oxygen, carbon, sulfur and silicon isotopes. Large variations (&gt; 10‰) of sulfide δ34S values at the deposit scale are likely related to evolving redox conditions of the mineralizing fluid during reaction with country rocks. Deposits hosted in sedimentary rocks show a shift to higher δ18O values as a result of fluid/rock oxygen exchange with the regional sedimentary country rocks.
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Huston, David L., Robert B. Trumbull, Georges Beaudoin, and Trevor Ireland. "Light Stable Isotopes (H, B, C, O and S) in Ore Studies—Methods, Theory, Applications and Uncertainties." In Isotopes in Economic Geology, Metallogenesis and Exploration. Springer International Publishing, 2023. http://dx.doi.org/10.1007/978-3-031-27897-6_8.

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AbstractVariations in the abundances of light stable isotopes, particularly those of hydrogen, boron, carbon, oxygen and sulfur, were essential in developing mineralization models. The data provide constraints on sources of hydrothermal fluids, carbon, boron and sulfur, track interaction of these fluids with the rocks at both the deposit and district scales, and establish processes of ore deposition. In providing such constraints, isotopic data have been integral in developing genetic models for porphyry-epithermal, volcanic-hosted massive sulfide, orogenic gold, sediment-hosted base metal and banded-iron formation-hosted iron ore systems, as discussed here and in other chapters in this book. After providing conventions, definitions and standards used to present stable isotope data, this chapter summarizes analytical methods, both bulk and in situ, discusses processes that fractionate stable isotopes, documents the isotopic characteristics of major fluid and rock reservoirs, and then shows how stable isotope data have been used to better understand ore-forming processes and to provide vectors to ore. Analytical procedures, initially developed in the 1940s for carbon–oxygen analysis of bulk samples of carbonate minerals, have developed so that, for most stable isotopic systems, spots as small as a few tens of μm are routinely analyzed. This precision provides the paragenetic and spatial resolution necessary to answer previously unresolvable genetic questions (and create new questions). Stable isotope fractionation reflects geological and geochemical processes important in ore formation, including: (1) phase changes such as boiling, (2) water–rock interaction, (3) cooling, (4) fluid mixing, (5) devolatilization, and (6) redox reactions, including SO2 disproportionation caused by the cooling of magmatic-hydrothermal fluids and photolytic dissociation in the atmosphere. These processes commonly produce gradients in isotopic data, both in time and in space. These gradients, commonly mappable in space, provide not only evidence of process but also exploration vectors. Stable isotope data can be used to estimate the conditions of alteration or mineralization when data for coexisting minerals are available. These estimates use experimentally- or theoretically-determined fractionation equations to estimate temperatures of mineral formation. If the temperature is known from isotopic or other data (e.g., fluid inclusion data or chemical geothermometers), the isotopic composition of the hydrothermal fluid components can be estimated. If fluid inclusion homogenization and compositional data exist, the pressure and depth of mineralization can be estimated. One of the most common uses of stable isotope data has been to determine, or more correctly delimit, fluid and sulfur sources. Estimates of the isotopic compositions of hydrothermal fluids, in most cases, do not define unequivocal sources, but, rather, eliminate sources. As an example, the field of magmatic fluids largely overlap that of metamorphic fluids in δ18O-δD space, but are significantly different to the fields of meteoric waters and seawater. As such, a meteoric or seawater origin for a fluid source may be resolvable, but a magmatic source cannot be resolved from a metamorphic source. Similarly, although δ34S ~ 0‰ is consistent with a magmatic-hydrothermal sulfur source, the signature can also be produced by leaching of an igneous source. Recent analytical and conceptual advances have enabled gathering of new types of isotopic data and application of these data to resolve new problems in mineral deposit genesis and geosciences in general. Recent developments such as rapid isotopic analysis of geological materials or clumped isotopes will continue to increase the utility of stable isotope data in mineral deposit genesis and metallogeny, and, importantly, for mineral exploration.
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Spitzenberger, Andy, Katrin Bauer, and Rüdiger Schwarze. "Reactive Cleaning and Active Filtration in Continuous Steel Casting." In Multifunctional Ceramic Filter Systems for Metal Melt Filtration. Springer International Publishing, 2024. http://dx.doi.org/10.1007/978-3-031-40930-1_17.

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AbstractBasic fluid dynamic processes of melt filtration have been investigated in order to increase the performance and efficiency of filtration systems in steelmaking, especially for continuous steel casting. Numerical simulations have been performed to investigate the interactions between filter structures and the mean melt flow, the development of endogenous non-metallic inclusion (NMI) populations in the flow, and inclusion removal from the melt. For this purpose, Euler–Lagrange models of the particle-laden flow have been developed. As a major finding, the reactive cleaning process of the melt has been proven to be a very efficient cleaning method. Here, inclusion removal is strongly improved by the lifting action of reactively generated gas bubbles at the NMI surfaces. Details of the reactive cleaning process and the combination of reactive cleaning and active filtration have been investigated, too. The prediction quality of the numerical models with regard to fluid flow and the efficiency of the employed filtration systems have been successfully examined by comparing numerical simulations with the results from experimental investigations in different water model experiments and the steel casting simulator.
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Li, Yanlong, Lifeng Zhang, and Ying Ren. "Fluid Flow, Alloy Dispersion and Inclusion Motion in Argonstirred Steel Ladles." In Celebrating the Megascale. John Wiley & Sons, Inc., 2014. http://dx.doi.org/10.1002/9781118889657.ch66.

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Conference papers on the topic "Fluid inclusion"

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Li, Hui, Junjia Fan, Xiaojiu Xu, Lijun Wang, and Meng Lei. "Fluid Inclusion Detection Based on Improved YOLOX." In 2023 4th International Conference on Computer, Big Data and Artificial Intelligence (ICCBD+AI). IEEE, 2023. http://dx.doi.org/10.1109/iccbd-ai62252.2023.00070.

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Kirschenmann, Jacob, Kenneth Hart, Timothy Homewood, Jessica Wilmot, and Matthew J. Severs. "FLUID INCLUSION INVESTIGATION OF SHAWANGUNK MINERAL DEPOSITS." In 59th Annual GSA Northeastern Section Meeting - 2024. Geological Society of America, 2024. http://dx.doi.org/10.1130/abs/2024ne-397628.

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Krieger, F. W., P. J. Eadington, and M. Lisk. "Fluid Inclusion Data for Rw in Reserves Estimation." In SPE Asia Pacific Oil and Gas Conference. Society of Petroleum Engineers, 1996. http://dx.doi.org/10.2118/36975-ms.

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Xu, Jinming, Bin Liu, and Qiang Xie. "Microscopic Heterogeneity of Fluid Inclusion Distributions in Rocks." In GeoCongress 2008. American Society of Civil Engineers, 2008. http://dx.doi.org/10.1061/40972(311)26.

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Stoller, Patrick, Jaro Ricka, Martin Frenz, and Yves Kruger. "Ultra-short pulse lasers in geological fluid inclusion analysis." In 2007 European Conference on Lasers and Electro-Optics and the International Quantum Electronics Conference. IEEE, 2007. http://dx.doi.org/10.1109/cleoe-iqec.2007.4386316.

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Towbin, William Henry, Evan M. Smith, Ulrika F. S. D'Haenens-Johansson, and Daniel C. Jones. "Macle Diamonds: Primary Fluid Inclusion Entrapment Along the Twinning Plane." In International Kimberlite Conference. University of Alberta, 2024. http://dx.doi.org/10.29173/ikc4165.

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Mamedov, Sergey. "APPLICATIONS OF RAMAN SPECTROSCOPY TO SOLID AND FLUID INCLUSION PHASE IDENTIFICATION." In GSA Connects 2023 Meeting in Pittsburgh, Pennsylvania. Geological Society of America, 2023. http://dx.doi.org/10.1130/abs/2023am-394796.

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Dubosq, Renelle, Anna Rogowitz, David Schneider, Kevin Schweinar, and Baptiste Gault. "Fluid inclusion induced hardening in pyrite: Results from atom probe tomography." In Goldschmidt2021. European Association of Geochemistry, 2021. http://dx.doi.org/10.7185/gold2021.3515.

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Lima, Annamaria, Robert J. Bodnar, and Benedetto De Vivo. "Fluid and Melt Inclusion Evidence for Immiscibility at Somma Vesuvius Volcano (Italy)." In Goldschmidt2020. Geochemical Society, 2020. http://dx.doi.org/10.46427/gold2020.1558.

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Wan, Zhenzhu, Peter Jenden, Andreas Schmidt Mumm, and Khaled Arouri. "STABLE CARBON ISOTOPIC VARIATION OF FLUID INCLUSION GASES FOR CHARGE HISTORY ANALYSIS." In GSA Annual Meeting in Indianapolis, Indiana, USA - 2018. Geological Society of America, 2018. http://dx.doi.org/10.1130/abs/2018am-319945.

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Reports on the topic "Fluid inclusion"

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Kingston, A. W., and O. H. Ardakani. Diagenetic fluid flow and hydrocarbon migration in the Montney Formation, British Columbia: fluid inclusion and stable isotope evidence. Natural Resources Canada/CMSS/Information Management, 2022. http://dx.doi.org/10.4095/330947.

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The Montney Formation in Alberta and British Columbia, Canada is an early Triassic siltstone currently in an active diagenetic environment at depths greater than 1,000 m, but with maximum burial depths potentially exceeding 5,000 m (Ness, 2001). It has undergone multiple phases of burial and uplift and there is strong evidence for multiple generations of hydrocarbon maturation/migration. Understanding the origin and history of diagenetic fluids within these systems helps to unravel the chemical changes that have occurred since deposition. Many cores taken near the deformation front display abundant calcite-filled fractures including vertical or sub-vertical, bedding plane parallel (beefs), and brecciated horizons with complex mixtures of vertical and horizontal components. We analyzed vertical and brecciated horizons to assess the timing and origin of fluid flow and its implications for diagenetic history of the Montney Fm. Aqueous and petroleum bearing fluid inclusions were observed in both vertical and brecciated zones; however, they did not occur in the same fluid inclusion assemblages. Petroleum inclusions occur as secondary fluid inclusions (e.g. in healed fractures and along cleavage planes) alongside primary aqueous inclusions indicating petroleum inclusions post-date aqueous inclusions and suggest multiple phases of fluid flow is recorded within these fractures. Raman spectroscopy of aqueous inclusions also display no evidence of petroleum compounds supporting the absence or low abundance of petroleum fluids during the formation of aqueous fluid inclusions. Pressure-corrected trapping temperatures (&amp;amp;gt;140°C) are likely associated with the period of maximum burial during the Laramide orogeny based on burial history modelling. Ice melt temperatures of aqueous fluid inclusions are consistent with 19% NaCl equiv. brine and eutectic temperatures (-51°C) indicate NaCl-CaCl2 composition. Combined use of aqueous and petroleum fluid inclusions in deeply buried sedimentary systems offers a promising tool for better understanding the diagenetic fluid history and helps constrain the pressure-temperature history important for characterizing economically important geologic formations.
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Kontak, D. J., S. Paradis, Z. Waller, and M. Fayek. Petrographic, fluid inclusion, and secondary ion mass spectrometry stable isotopic (O, S) study of Mississippi Valley-type mineralization in British Columbia and Alberta. Natural Resources Canada/CMSS/Information Management, 2022. http://dx.doi.org/10.4095/327994.

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A comprehensive study of Mississippi Valley-type base-metal deposits across the Canadian Cordillera was done to compare and contrast their features. Extensive dissolution of host rocks is followed by multiple generations of dolomite cements from early, low-temperature, fine-grained to coarser, higher temperature types that overlap with Zn-Pb sulfide minerals; late-stage calcite occludes residual porosity. Dolomite is generally chemically stoichiometric, but ore-stage types are often rich in Fe (&amp;amp;lt;1.3 weight per cent FeO) with small sphalerite inclusions. Sphalerite-hosted fluid inclusions record ranges for homogenization temperatures (77-214°C) and fluid salinity (1-28 weight per cent equiv. NaCl±CaCl2). These data suggest fluid mixing with no single fluid type related to all sulfide mineralization. In situ secondary ion mass spectrometry (SIMS) generated delta-18OVSMOW values for carbonate minerals (13-33 permille) reflect dolomite and calcite formation involving several fluids (seawater, basinal, meteoric) over a large temperature range at varying fluid-rock ratios. Sphalerite and pyrite SIMS delta-34SVCDT values vary (8-33 permille) but in single settings have small ranges (&amp;amp;lt;2-3 permille) that suggest sulfur was reduced via thermochemical sulfate reduction from homogeneous sulfur reservoirs. Collectively, the data implicate several fluids in the mineralizing process and suggest mixing of a sulfur-poor, metal-bearing fluid with a metal-poor, sulfide-bearing fluid.
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Dilley, Lorie M. Methodologies for Reservoir Characterization Using Fluid Inclusion Gas Chemistry. Office of Scientific and Technical Information (OSTI), 2015. http://dx.doi.org/10.2172/1177790.

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Dilley, Lorie M., David Norman, and Lara Owens. Identifying Fracture Types and Relative Ages Using Fluid Inclusion Stratigraphy. Office of Scientific and Technical Information (OSTI), 2008. http://dx.doi.org/10.2172/933170.

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Lorie M. Dilley. Chemical Signatures of and Precursors to Fractures Using Fluid Inclusion Stratigraphy. Office of Scientific and Technical Information (OSTI), 2011. http://dx.doi.org/10.2172/1010306.

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Chi, G. Fluid compositions and temperature-pressure conditions of intrusion-related gold systems in southwestern New Brunswick - a fluid-inclusion study. Natural Resources Canada/ESS/Scientific and Technical Publishing Services, 2002. http://dx.doi.org/10.4095/213694.

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Cattalani, S., and A. E. Williams-Jones. Geological and Fluid Inclusion Studies At the Saint-Robert Ag, W, Bi Deposit. Natural Resources Canada/ESS/Scientific and Technical Publishing Services, 1986. http://dx.doi.org/10.4095/120388.

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Aulstead, K. L., and R. Spencer. Fluid Inclusion Evidence On the Diagenesis of the Manetoe Facies, Yukon and Northwest Territories. Natural Resources Canada/ESS/Scientific and Technical Publishing Services, 1986. http://dx.doi.org/10.4095/130032.

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Stevens, K. Mineral zoning and fluid inclusion studies in the Candego / Madeleine Mines area, Gaspe, Quebec. Natural Resources Canada/ESS/Scientific and Technical Publishing Services, 1987. http://dx.doi.org/10.4095/130187.

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Chi, G., B. Dubé, and K. Williamson. Preliminary fluid-inclusion microthermometry study of fluid evolution and temperature-pressure conditions in the Goldcorp High-Grade zone, Red Lake mine, Ontario. Natural Resources Canada/ESS/Scientific and Technical Publishing Services, 2002. http://dx.doi.org/10.4095/213205.

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