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Spor Mountain
Origin of the fluorine- and beryllium-rich rhyolites of the Spor Mountain Formation, Western Utah
Uranium-bearing opals: Products of U-mobilization, diffusion, and transformation processes
Non-pegmatitic Deposits of Beryllium: Mineralogy, Geology, Phase Equilibria and Origin
Partitioning of F and Cl between magmatic hydrothermal fluids and highly evolved granitic magmas
The distribution of F and Cl between aqueous fluids and melts of haplogranite and topaz rhyolite composition was determined experimentally at 0.5 to 5 kbar and 775° to 1,000°C. The distribution coefficients, D i , for F and Cl were calculated as the parts per million by weight (ppmw) of i in the fluid/parts per million by weight (ppmw) of i in the melt. D Cl ranges from 0.8 to 85; however, under typical geologic conditions, Cl partitions more strongly into an aqueous fluid relative to F-bearing granitic melts. Cl partitions increasingly in favor of the fluid as F in the fluid and magma decrease and as the X H 2 O fl (molar H 2 O/H 2 O + CO 2 in fluid), temperature, pressure, and Cl in the fluid and melt increase. Cl partitions in favor of haplogranite melts that contain >7 wt % F and ⩽1,200 ppm Cl at 1,000°C and 2 kbar. D F ranges from 0.2 to >1.0; however, F typically is concentrated in granitic melts relative to aqueous fluids. F concentrates more strongly into topaz rhyolite melt as pressure, F in the fluid, and melt, temperature, and the X H 2 O fl decrease. However, F partitions in favor of aqueous fluids relative to topaz rhyolite melts at 800°C and 2 kbar, if the melt contains ⩾7 wt % F. Computations indicate that extreme enrichments in F (>4 wt %) and Cl (>5,000 ppm) may occur in magmas and in associated magmatic hydrothermal fluids during the end stages of crystallization of topaz rhyolite magmas and magmas associated with Climax-type molybdenum deposits if the initial H 2 O, CaO, and ferromagnesian contents in the magma are low, and if the pressure at which water saturation occurs is high.
Partitioning of lithophile trace elements between H 2 O and H 2 O + CO 2 fluids and topaz rhyolite melt
Several types of mineralization appear to be related to the emplacement of fluorine-rich silicic lava flows and domes. An important example is the beryllium deposit at Spor Mountain, west-central Utah, where bertrandite, fluorite, amorphous silica, and Mn-Fe oxides replace dolomite fragments in tuffaceous surge deposits just beneath a topaz-bearing rhyolitic lava flow. The Be-mineralized zone is also highly enriched in F, Sn, W, Nb (and presumably Ta), Zn, Pb, and several other metals (but not in Mo). The uniform lateral character of the mineralization, the restriction of Be mineralization to the upper-most few meters of tuff, and the lack of mineralization in fluorite-bearing breccia pipes (tuffaceous vent breccias, in some cases) in underlying dolomite suggest (Bikun, 1980) that the beryllium mineralization resulted from the devitrification of the overlying lavas (a “steam iron” model). Mass-balance calculations based on comparisons of the chemical compositions of glassy and devitrified rhyolite are consistent with this unconventional interpretation. A second important example is provided by “Mexican-type” fumarolic tin deposits, characterized by cassiterite in carapace breccias of rhyolitic domes. Low-temperature dissolution and reworking of early fumarolic cassiterite may produce the colloform “wood tin” common in this deposit type. Deposits of this type occur in Nevada and New Mexico, as well as in many areas of northern Mexico. Fluorine-rich intrusive domes (better known as plutons) may also host metal mineralization, generally of the porphyry type. Examples include the well-known Climax-type porphyry molybdenum deposits of Colorado, New Mexico, and Utah, and the porphyry tungsten deposit at Mount Pleasant, New Brunswick, Canada. These subvolcanic deposits, in common with those associated with extrusive silicic lava flows and domes, are believed to have been derived by the crystallization-devolatization of highly fractionated magma.