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Hydrothermal Phlogopite and Anhydrite from the SH2 Well, Sabatini Yolcanic District, Latium, Italy: Fluid Inclusionsand Mineral Chemistry H,Q.Nvnve

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Hydrothermal Phlogopite and Anhydrite from the SH2 Well, Sabatini Yolcanic District, Latium, Italy: Fluid Inclusionsand Mineral Chemistry H,Q.Nvnve American Mineralogist, Volume 73, pages 775-797, 1988 Hydrothermal phlogopite and anhydrite from the SH2 well, Sabatini Yolcanic district, Latium, Italy: Fluid inclusionsand mineral chemistry H,q.nvnvE. Brr,xrN U.S. Geological Survey, 959 National Center, Reston, Virginia 22092,U.5.4. Grusnppn Clv.lRnrrr,c, Centro di Studio per la Geologia dell'Italia Centrale del C.N.R., % Dipartimento di Scienzedella Terra, Universitd degli Studi di Roma "La Sapienza,"00185, Roma, Italy BnNronrro Dn Vrvo Dipartimento di Geofisica e Vulcanologia, Largo S. Marcellino 10, 80138 Napoli, Italy Fn-c,NcnscA.Tpccn Centro di Studio per la Geologia dell'Italia Centrale del C.N.R., % Dipartimento di Scienzedella Terra, Universitd degli Studi di Roma "La Sapienza,"00185, Roma, Italy AssrRAcr The SH2 well(2498.7 m) was drilled vertically in 1982-1983by an AGIP-ENEL Joint Venture as an exploratory hole to assessthe geothermal potential of the area north of Bracciano Lake, Latium, Italy, located in the Sabatini volcanic district. Drill-cutting sam- ples from a thermometamorphic-metasomaticzone (1 140-2498.7 m) contain hydrother- mal anhydrite + phlogopite (+ calcite + pyrite) and other authigenic volatile-rich phases. Microthermometry of primary and secondarytwo-phase [vapor (V) + liquid (L)] and multiphase (V + L * crystals)liquid-rich inclusions in anhydrite yields pressure-corrected temperatures of homogenization (trapping temperatures)that range from 144 to 304'C and that are generally coincident with measuredin-hole temperatures.The fluids have a variable salinity from 0.5 to 14.0 wto/oNaCl equivalent and also contain Ca2+ at least. Rare liquid COr-bearing aqueousinclusions have been verified by laser Raman spectros- copy. Also, rare liquid hydrocarbons(?)have beenobserved. Clathrates have been observed upon freezing, and crushing studies reveal noncondensablegas at P > I atm in some inclusions. Euhedral to subhedral phlogopite crystals (-0.5 to -2 mm) commonly are zoned and contain solid inclusions ofanhydrite and apatite and two-phase (V * L) and multiphase (V + L + crystals)fluid inclusions. Microthermometry of primary two-phase inclusions yields pressure-correctedtemperatures of homogenization (trapping tempera- tures) that range from 178 to 298 oC and are also generallycoincident with in-hole mea- sured temperatures. Freezing studies show a variable fluid salinity (0.2-7.8 wto/oNaCl equiv.); the fluid contains Ca2+at least. If we assumethat the current hydrologic regime existed during anhydrite and phlogopite formation, the pressureof formation ranged from - 148to -220bars for phlogopite(1600--2500 m) and - 120to -220bars for anhydrite (1300--2500 m). Hence, the phlogopite and other authigenic phaseshave crystallized from a low P-2, volatile-rich, generallydilute, geothermal solution. Detailed microprobe analysesof fluid inclusion-bearing phlogopites indicate that they are nearly end member, Fer/(Fe, + Mg) : 0.02 to 0.1 and the t4tAlper I I oxygen equiv- alentsvaries from 1.0 to 1.35.F, BaO, and TiO, rangefrom 2.4 to 5.0 wt0/0,0 to 3.5 wt0/0, and 0.1 to 0.89 wt0/0,respectively, and an Fe2+-Favoidance is observed. Various cation substitutional schemesappear to be operative and are assessed.The dark zones are Fe- rich, but may have more or lessF, BaO, or TiO, than the light zones.xRF-KEvEx analysis of eight anhydrite samplesyield averagevalues (ppm) of Sr: 5500, Ba : 1900, Rb : 250' Ce: 140,and La: 100. The variation of fluid-inclusion salinities, the phlogopite zoning, and the chemical vari- ation of the anhydrite and phlogopite suggestthat different fluids and/or episodic condi- tions were operative in this geothermal system. 0003404x/88/0708-0775$02.00 775 776 BELKIN ET AL.: HYDROTHERMAL PHLOGOPITE AND ANHYDRITE basis of the various minerals recorded throughout the SH2 well, Cavarretta and Tecce (1987) have suggested that the ascendinghydrothermal solutions were rich in SO, + CO, plus other volatiles (B, HD and that perhaps a shallow Ca-rich fluid was present. They also have de- bated the hypothesisthat the brine was, in part, the result of remobilization of sedimentary (Triassic) sulfates in a low-pressureenvironment. They have concludedthat the hydrothermal solution and heat source was a magma of possible trachytic (or less differentiated) composition with a high volatile content that intruded in a subvolcanic en- BRACCIANOLAKE vironment in the northern Bracciano Lake area. The study of fluid inclusions in hydrothermal minerals may allow an evaluation of the fluid composition, tem- XA perature,and hydrology at the time of trapping, thus pro- CB viding information on the evolution of the geothermal systems(e.g., Browne et al., 1976; Taguchi and Hoyashi, {c 1983;Belkin et al., 1986).We have studiedthe fluid in- r Skm r /o clusions and mineral chemistry of the authigenic assem- blageof anhydrite and phlogopite. Anhydrite is becoming Fig. l. Location ofthe SH2 well and the generalfeatures of increasinglyrecognized important physicochemical the Sabatini volcanic district. A : scoria cones;B : explosive as an craters;C : caldera rims; D : fault. indicator in geothermal and mineralized hydrothermal systems(e.g., Cavarrettaetal., 1982;Queen and Motyka, 1984;Hattori et al., 1985).Authigenic phlogopite in geo- INrnolucrroN thermal or hydrothermal systems is rare; furthermore, The Sabatini volcanic district, located in northern La- fluid-inclusion studies of phlogopite are unknown to the tium, Italy, (Fig. l) has recently received considerable authors. Therefore, we have also undertaken extensive attention by the AGIP-ENEL Joint Venture (National Oil microprobe analysesof the phlogopite mineral chemistry and Electricity Boards, respectively; ENEL as operator) as a function of sample depth and crystal zoning. Phlog- for geothermalenergy exploration. The initial targetarea opite reflects the relative fugacities of HF, HCl, 02, H2, was the Cesano-Baccanocaldera that has the highest geo- and water during crystallization and hence monitors in- thermal gradient(l0G-150'C/km; Calamai et al., 1975) tensive variablesduring hydrothermal processes.The de- ofthe region.From 1975to date, l4 deepwells have been tailed characterization of the SH2 authigenic phlogopite drilled. Four ofthem produced a hot supersaturatedchlo- is especiallyimportant becausewe can define its environ- ride-sulfate brine (200 oC, reservoir conditions) charac- ment of formation in terms of pressure,temperature, and terized by unusually high values of total dissolved salts fluid composition. The trace-elementchemistry of the au- (up to 400 g/L, postflash; flashing steam estimated to be thigenic anhydrite was also determined in an attempt to 20-25o/oof total floq Calamaiet al., 1975).The difficul- provide additional information on the nature of the co- ties inherent with the use ofhot brines for electricity pro- existing solutions. duction have prompted the searchfor lower-salinity geo- thermal fluids outside the Cesano-Baccanocaldera. Gnor,ocrc sETTTNG The SH2 deep well (2498.7 m) wris drilled vertically in The Sabatini volcanic district is part ofthe perpotassic 1982-1983as an exploratoryhole to assessthe geother- Roman comagmatic province of Washington (1906) that mal potential of the area north of Bracciano Lake (Fig. borders the easternTyrrhenian Sea and is aligned along l). The bottom temperature was 290 oC,but no exploit- a NW-SE tectonic trend. Although the origin of the vol- able fluids were found (Calamai et al., 1985). Neverthe- canic activity is debated,the most current interpretation less,the pervasive hydrothermal alteration describedby defines the tectonic style as postcollisional and the asso- Cavarretta and Tecce (1987) is convincing evidencethat ciated magmatism as subduction related rather than re- an extensive hydrothermal system must have existed in sulting from intraplate rifting (e.g., Di Girolamo, 1978; the recent past. Extensive vein and pore-spacefillings by Rogerset al., 1985). hydrothermal minerals have effectively sealed the sys- The largest volcano-tectonic structure in the area, an tem. The lower 1630 m of the SH2 well is characterized almost square depression,is located near the Bracciano by the hydrothermal assemblageanhydrite + calcite + village and is now a lake (BraccianoLake). The Sacrofano pyrite plus, at various levels, the addition of K-feldspar, center, a stratovolcanic structure, is the main eruptive garnet, vesuvianite, apatite, phlogopite, spinel, pyroxene, center(De Rita et al., 1983).Numerous other minor cen- wollastonite, and the occurrenceof uncommon, volatile- ters (-20) give the areaa"crater-field" morphology.Their rich minerals such as wilkeite, cuspidine, harkerite, can- activity was mainly explosive, producing huge volumes crinite, and reyerite (Cavarrettaand Tecce, I 987). On the of pyroclastics;lava flows, very subordinate in volume, BELKIN ET AL.: HYDROTHERMAL PHLOGOPITE AND ANHYDRITE 777 are most abundant in the northern part of the Bracciano Lake area. The lake perimeter is characterizedby several recentminor eruptive centers,such as Trevignano, Vigna di Valle, Polline, and Acquerello. The oldest dated products of the Sabatini complex are the 0.6 Ma Morlupo center pyroclastics, whereas the youngestdated product is the 0.083 Ma Baccano pyro- A clastic flow. However, as defined by stratigraphy,the lat- est products were erupted from the Martignano, Le Case, and Stracciacappecenters (Di Filippo et al., 1984). The composition of products erupted within the Sa- o batini volcanic district is considered to be transitional o (to o between
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