Volatile Interactions in Magmas

Holloway, John

doi:10.1007/978-1-4612-5871-1_13

Cited by 68 publications

(35 citation statements)

References 33 publications

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“…Calculated annite activities, and estimated water fugacities using each of the annite activity models are presented in Table 3, along with the calculated water fugacities for experimental samples, calculated using a Modified Redlich Kwong (MRK) equation of state (EOS) (Holloway, 1981). …”

Section: Discussionmentioning

confidence: 99%

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Estimation of pre-eruptive magmatic water fugacity in the Phlegrean Fields, Naples, Italy

Fabbrizio¹,

Scaillet²,

Carroll³

2009

ejm

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We estimated the water fugacity (f H 2 O) in the trachytic magma of Phlegrean Fields using the biotite-magnetite-sanidine equilibrium. We confirm that the partly ionic model is the most appropriate to estimate annite activity (a annite ) for the experimental biotite. Crystallization experiments were carried out on a representative sample of trachytic Breccia Museo eruption, Naples, Italy. Experiments were performed in the temperature and pressure range of 725-870 °C and 50-200 MPa, and redox conditions ranging from NNO (nickel-nickel oxide) + 1 (±0.2) to FMQ (fayalite + magnetite + quartz). Most experiments were done under conditions of H 2 O saturation (P water = P total ). Few experiments were done using a mixed H 2 O-CO 2 fluid phase. The pre-eruptive fH 2 O of the Phlegrean Fields magma is estimated at 735 bars, which compares well with available melt inclusion constraints. Our results confirm that this geohygrometer can be used in any magmatic systems bearing the worked assemblage.

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Section: Discussionmentioning

confidence: 99%

“…Natural biotite data are taken from Armienti et al (1983), Melluso et al (1995), Orsi et al(1995) and Civetta et al (1997). (Holloway, 1981). Squares, estimated water fugacity using the annite activity model of Wones & Eugster (1965).…”

Section: Discussionmentioning

confidence: 99%

Estimation of pre-eruptive magmatic water fugacity in the Phlegrean Fields, Naples, Italy

Fabbrizio¹,

Scaillet²,

Carroll³

2009

ejm

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“…6c, including those for CO-C0 2 -saturated basaltic melts (Pawley et al, 1992), correspond reasonably well to the 1: 1 line. Most importantly, the Henrian model for the activity of carbonate in the melt is valid even for melts coexisting with C0 2 -rich vapor, where a significant enhancement of C0 2 concentration relative to the I : I line was expected based on studies of C0 2 concentrations in melts saturated with C0 2 -H 2 0 vapors at significantly higher pressure (Eggler, 1973;Holloway & Lewis, 1974;Karlik & Eggler, 1975;Mysen et al, 1975Mysen et al, , 1976Brey & Green, 1976;Mysen, 1976;Eggler & Rosenhauer, 1978;Holloway, 1981 ). The difference between our results and previous studies that reported non-Henrian behavior of C0 2 (i.e.…”

Section: J1 C2mentioning

confidence: 99%

An Experimental Study of Water and Carbon Dioxide Solubilities in Mid-Ocean Ridge Basaltic Liquids. Part I: Calibration and Solubility Models

Dixon

Stolper

Holloway

1995

Journal of Petrology

138

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INTRODUCTIONSu baerial magmas solidify at a pressure of -1 bar, but the pressure on submarine magmas ranges from near I bar to several hundred bars, depending on the water depth at which they erupt. Even over this small pressure range, the vesicularity and vesicle-gas composition of submarine magmas of constant bulk composition can change dramatically, reflecting the large differences in volume between gaseous a nd melt species, the large compressibility of the gas phase at these low pressures, and the increasing (but different) solubilities of all gaseous species with pressure in this pressure range. Thus, the well-known negative corr elation between eruption depth a nd vesicularity of subm arine magmas reflects the degassing of magmas at progressively lower pressures under conditions where the exsolving vapor is unable to escape fully from the m agma (e.g. Moore, 1965, (!) Oxford University Press 1995 1970Moore & Schilling, 1973). Likewise, the different solubilities of the major (e.g. C02, H20, S) and minor (e.g. rare gases) volatile species are expected (though not yet observed) to lead to a strong dependence of the composition of the vapor in the vesicles on depth (e.g. Moore, 1965Moore, , 1970Jambon et al., 1985;Gerlach, 1986; ]ambon et al., 1986; Zhang & Zindler, 1989; Bottinga & Javoy, 1990b). Similarly, it is thought that differing solubilities of oxidized and reduced gaseous species can result in systematic changes in the oxidation state of iron and sulfur in erupting magmas as a function of the degree and depth of degassing (e.g. Sa to, 1978;Mathez, 1984; Carmichael & G hiorso, 1986;Christie et al., 1986;Wallace & Carmichael, 1992;Nilsson & Peach, 1993). In view of the importance of the exsolution of a vapor phase from submarine magmas in . understanding their vesicle contents, their eruptive style, aspects of their chemistry, and ultimately the chemistry of the atmosphere and ocean (e.g. Javoy et al., 1982;Des Marais, 1985; Marty & ]ambon, 1987;Gerlach, 1989; Zhang & Zindler, 1989, it is surprising how little is known about the behavior of volatile components in these systems in the pressure range over which these magmas are erupted. For example, only recently has the solubility of carbon dioxide, the major component of vesicle gases in mid-ocean ridge basalt (MORB) (Killingley & Muenow, 1975;Moore et al., 1977;Delaney et al., 1978;]ambon & Zimmermann, 1987), been measured in MORB melt by experiment (Stolper & Holloway, 1988;Shilobreyeva & Kadik, 1989; Mattey, 1991; Pan et al., 1991 ;Pawley et al., 1992;Trull et al. , 1992) . Water is even more abundant than carbon dioxide in most MORB glasses, but we know of no measurements of the solubility of water in MORB liquids at eruptive conditions, although water solubilities have been measured at higher pressures ( 1-10 kbar) in other basaltic compositions (Khitarov et al., 1959;Hamilton et al., 1964;Kadik et al., 1971 ). Kadik et al. (1972} reported mixed C0 2 and H 2 0 solubilities in basaltic melts at 1-3 kbar, but their experiments did not extend to...

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“…Carbon dioxide (CO 2 ) is the second most abundant magmatic volatile (e.g. Gerlach and Graeber, 1985;Symonds et al, 1994;Jambon, 1994) being even dominant in some volcanic systems (Roedder, 1965;Wyllie and Huang, 1976;Holloway, 1981;Giggenbach, 1997;Andersen and Neumann, 2001). Some of these systems may reflect a high CO 2 abundance in their source regions, as witnessed by unusual magma compositions (such as nephelinite, melilitite and kamafugite) which have been suggested to result from high CO 2 activity during mantle melting (e.g.…”

Section: Introductionmentioning

confidence: 99%

Carbon dioxide in silica-undersaturated melt. Part I: The effect of mixed alkalis (K and Na) on CO2 solubility and speciation

Morizet

Paris

Gaillard

et al. 2014

Geochimica et Cosmochimica Acta

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Volatile Interactions in Magmas

Cited by 68 publications

References 33 publications

Estimation of pre-eruptive magmatic water fugacity in the Phlegrean Fields, Naples, Italy

Estimation of pre-eruptive magmatic water fugacity in the Phlegrean Fields, Naples, Italy

An Experimental Study of Water and Carbon Dioxide Solubilities in Mid-Ocean Ridge Basaltic Liquids. Part I: Calibration and Solubility Models

Carbon dioxide in silica-undersaturated melt. Part I: The effect of mixed alkalis (K and Na) on CO2 solubility and speciation

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