Minerals fluid interactions

Inoue, A., Utada, M. and Shimizu, M. (1999) Mineral-fluid interactions in the Sumikawa geothermal system, northeast Japan. Resource Geology Special Issue, 20, 79-98. 

Frezzotti ML, de Vivo B, Clocchiatti R (1991) Melt-mineral-fluid interactions in ultramafic nodules from alkaline lavas of Mount Etna (Sicily, Italy) melt and fluid inclusion evidence. J Volcanol Geotherm Res 47 209-219... 

Elucidation of the kinetics and mechanisms of mineral-fluid interactions requires high-resolution X-ray scattering measurements on rapid time scales. Time series analyses are desired for addressing the evolution of structure and composition at the interface, on time scales as small as milliseconds or less. The high brilliance of the third-generation synchrotron sources affords new opportunities for such time-resolved studies, because we can observe in real time the processes of adsorption/desorption and complex formation at mineral-fluid interfaces. For example, experiments using a pressure-jump relaxation techniques yield rates of adsorption and desorption of protons and hydroxide at the surface of metal oxides in the range of milliseconds to seconds (reviewed by Casey and... 

Gamo (1995) revealed based on the chemical and isotopic compositions of hydrothermal fluids from midocean ridges that the precipitation of minerals and interaction... 

A critical issue is the extent to which the isotope composition of a metamorphic rock is modified by a fluid phase. Volatilization reactions leave an isotope signature greatly different from that produced when fluid-rock interaction accompanies mineral-fluid reaction. Changes of 5-10%c are a strong indication that fluid-rock interaction rather than volatilization reactions occurred during the metamorphic event. Coupled 0-C depletions are seen in many metamorphic systems involving carbonate rocks. Figure 3.50 summarizes results from 28 studies of marble mostly... 

Fedele, L., Tarzia, M., Belkin, H. E., De Vivo, B., Lima, A., and Lowenstern, J. B. (2006). Magmatic-hydrothermal fluid interaction and mineralization in alkali-syenite nodules from the Breccia Museo pyroclastic deposit, Naples, Italy. In Volcanism in the Campania Plain Vesuvius, Campi Flegrei and Ignimbrites (B. De Vivo, ed.). Developments in Volcanology, 9, pp. 125-161. Elsevier, Amsterdam, The Netherlands. 

The rest of the chapter is organized as follows. In Section 6.07.2 we discuss the chemical composition of hydrothermal fluids, why they are important, what factors control their compositions, and how these compositions vary, both in space, from one location to another, and in time. Next (Section 6.07.3) we identify that the fluxes established thus far represent gross fluxes into and out of the ocean crust associated with high-temperature venting. We then examine the other source and sink terms associated with hydrothermal circulation, including alteration of the oceanic crust, formation of hydrothermal mineral deposits, interactions/uptake within hydrothermal plumes and settling into deep-sea sediments. Each of these fates for hydrothermal material is then considered in more detail. Section 6.07.4 provides a detailed discussion of near-vent deposits, including the formation of polymetallic sulfides and... 

Bj0rlykke K. and Lynch F.L. (1997) Mineral/water interaction, fluid flow, and Frio sandstone diagenesis evidence from the rocks—Discussion and Reply. Am. Assoc. Petrol. Geologists Bull. 81, 1534-1537. 

Hydrocarbons are sometimes trapped in inclusions within igneous intrusions [16,115,117,135] or crystalline basement [139,140], or are associated with ore deposits [110]. For example, hydrocarbons trapped in ore veins from the Aberfoyle tin-tungsten deposit in Tasmania, Australia, include biomarkers that suggest that the mineralizing fluid evolved through interaction with sedimentary country rocks [110]. Sphalerite- and... 

Thus, the high and variable content of boron in mineralized granites, such as the Cornubian batholith, provide evidence of granite host rock-fluid interaction that can thus be detected in samples that lack discrete mineralization. 

In Hadrian s Wall, mineral/cement fluid reactions in the dolerite produced a zone of increased porosity (caused by dissolution) and a deeper, parallel zone in which macroporosity was unchanged due to replacement by reaction products. The combined effect is to increase the surface area of solid material (dolerite or reaction product). This could increase the extent of any subsequent matrix/fluid interaction. 

In the early days, IP was directed mostly on ore mineral exploration. Later, pore space properties and connected effects became more interesting. Today, frequency-dependent complex resistivity measurements are generally directed on problems of pore space characterization and description of fluid-mineral interactions. Measurements are sensitive to physico-chemical mineral-water-interaction at the grain surfaces. In comparison to conventional geoelectrics, a complex electrical measurement can also provide - besides conductivity -information on the electrical capacity and the relaxation process in the frequency range below some kHz (Bomer, 2006). 

Microbial cells transported with the stream of fluid above the surface interact with conditioning films. Immediately after attachment, microorganisms initiate production of slimy adhesive substances, predominantly exopolysaccharides (EPS) that assist the formation of microcolonies and microbial films. EPS create bridges for microbial cells to the substratum and permit negatively charged bacteria to adhere to both negatively and positively charged surfaces. EPS may also control interfacial chemistry at the mineral/biofilm interface. 

Origin of ore fluids is constrained by (1) chemical compositions of ore fluids estimated by thermochemical calculations (section 1.3.2) and by fluid inclusion analyses, (2) isotopic compositions of ore fluids estimated by the analyses of minerals and fluid inclusions (section 1.3.3), (3) seawater-rock interaction experiments, (4) computer calculations on the seawater-rock interaction, and (5) comparison of chemical features of Kuroko ore fluids with those of present-day hydrothermal solutions venting from seafloor (section 2.3). 

Giggenbach (1984) calculated the effect of temperature on the chemical composition of fluids buffered by alteration minerals. The causes for the hydrothermal alteration considered below are mainly based on the works by Shikazono (1978a) and Giggenbach (1984). The effect of the extent of water-rock interaction is not taken into account. 

Gangue minerals and salinity give constraints on the pH range. The thermochemical stability field of adularia, sericite and kaolinite depends on temperature, ionic strength, pH and potassium ion concentration of the aqueous phase. The potassium ion concentration is estimated from the empirical relation of Na+/K+ obtained from analyses of geothermal waters (White, 1965 Ellis, 1969 Fournier and Truesdell, 1973), experimental data on rock-water interactions (e.g., Mottl and Holland, 1978) and assuming that salinity of inclusion fluids is equal to ffZNa+ -h m + in which m is molal concentration. From these data potassium ion concentration was assumed to be 0.1 and 0.2 mol/kg H2O for 200°C and 250°C. 

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