Water-melt interaction in hydrous magmatic systems at high temperature and pressure
© Mysen; licensee Springer. 2014
Received: 3 December 2013
Accepted: 10 March 2014
Published: 22 April 2014
Experimental data on the structure and properties of melts and fluids relevant to water-melt interaction in hydrous magmatic systems in the Earth's interior have been reviewed. Complex relationships between water solubility in melts and their bulk composition [Al/Si-ratio, metal oxide/(Al + Si) and electron properties of metal cations] explain why water solubility in felsic magmas such as those of rhyolite and andesite composition is significantly greater than the water solubility in basalt melts. The silicate solubility in aqueous fluid is also significantly dependent on composition with metal oxide/(Al + Si) and electron properties of the metal cations, the dominant variables. Hydrogen bonding is not important in hydrous fluids and melts at temperatures above 500°C to 550°C and does not, therefore, play a role in hydrous magmatic systems. The properties of hydrous melts and aqueous solutions are governed by how the silicate speciation (Q n species, where n is the number of bridging oxygen in an individual species) varies with bulk composition, silicate composition, temperature, and pressure. The reactions that describe the interactions are similar in melts, fluids, and supercritical fluids. The degree of melt polymerization caused by dissolved water varies with melt composition and total water content. Silicate- and alkali-rich felsic magmatic melts are more sensitive to water content than more mafic magmas. Transport and configurational properties of hydrous magmatic melts can be modeled with the aid of the Q n speciation variations. Liquidus and melting phase relations of hydrous systems also can be described in such terms, as can minor and trace element partition coefficients. Stable isotope fractionation (e.g., D/H) can also be rationalized in this manner. Critical to these latter observations is the high silicate concentration in aqueous fluids. These components can enhance solubility of minor and trace elements by orders of magnitude and change the speciation of H and D complexes so that their fractionation factors change quite significantly. Data from pure silicate-H2O systems cannot be employed for these purposes.
KeywordsHydrous magma Aqueous fluid Melt structure Viscosity Isotope partitioning Partial melting Water solubility Silicate solubility Glass transition Solution mechanism
The principal mass and energy transport agents in the Earth are magmatic melts and water-rich fluids. Their transport properties are sensitive to their water and silicate content. Experimental characterization of solubility and solution mechanisms of water and silicate components is, therefore, central to our understanding of magmatic and metasomatic processes in the Earth’s interior.
Properties of magmatic melts are sensitive to their water content as first noted by Spallanzani (1798). Perhaps the most well-known among these effects is a several hundred degree centigrade temperature depression at high pressure of solidii and liquidii of silicate phase assemblages (including natural mineral assemblages) (e.g., Kushiro et al. 1968a, b; Grove et al. 2012). Liquidus phase relations (including partial melt compositions), transport, and volume properties of hydrous melts also vary in important ways with variations in water content (Kushiro 1972; Richet et al. 1996; Ochs and Lange 1999; Grove et al. 2003).
Aqueous solutions in the Earth's interior are efficient solvents of oxide components (Zhang and Frantz 2000; Manning 2004). Several mol% of silicate components dissolve under conditions corresponding to those of the deep continental crust and upper mantle. In the upper mantle, there can be complete miscibility between H2O and silicate (Bureau and Keppler 1999; Mibe et al. 2007). Major element solutes in aqueous fluids (silicate components) can also enhance the solubility of other components by up to orders of magnitude (Pascal and Anderson 1989; Antignano and Manning 2008; Mysen 2012a, b; Ayers and Watson 1993). Transport, volume, and mixing properties of silicate-rich aqueous fluids differ in important ways from those of pure H2O (Audetat and Keppler 2004; Hunt and Manning 2012; Hack and Thompson 2012; Foustoukos and Mysen 2013).
The property behavior of melts and fluids in hydrous silicate systems at the high temperatures and pressures can be traced to the relationships between fluid and melt structure and their properties. Most experimental and theoretical studies have focused on the behavior in chemically simpler systems in order to isolate the effects of individual intensive and extensive variables. With the information from chemically simpler systems, we can model melt and fluid behavior in systems relevant to natural processes. In this review, these relationships will be presented and their applications to natural systems will be discussed.
Water and properties of hydrous magma
Melting phase relations
Properties of hydrous silicate melts
Most other physical properties of silicate melts show analogous relations with water content and silicate composition. Examples include cation and water diffusion in melts (Watson 1994; Behrens and Nowak 1997), effects of water on glass transition temperature (Richet et al. 1996, 1997; Whittington et al. 2000), and electrical conductivity (e.g., Takata et al. 1981; Satherley and Smedley 1985). These effects exist because of the functional relationships that exist between these transport properties (Nernst 1888; Einstein 1905; Eyring 1935a, b).
Water solubility in magmatic melts
Given the complex relationships between melt composition and water solubility, it is not surprising that the solubility varies significantly in different magmatic systems. In general, water solubility in felsic magmas such as those of rhyolite and andesite composition is significantly greater than the solubility in basalt melts (Hamilton et al. 1964; Dixon and Stolper 1995; Behrens and Jantos 2001; Zhang 1999). This would be expected because of the higher alkali/alkaline earth and Si/Al ratios in rhyolite and andesite melt compared with melts of basaltic composition. These solubility relationships have been modeled with a variety of empirical models (e.g., Spera 1974; Burnham 1975; Dixon and Stolper 1995; Behrens and Jantos 2001). However, quantitative linkage between solubility behavior in chemically simple melts and more complex natural magma compositions await detailed structural characterization of the water solution mechanisms in simple and complex magmatic melts.
Silicate solubility in aqueous fluids
Melt and glass
Most of the experimental data on solubility and solution behavior of water in silicate melts at high temperature have been obtained by analysis of the glass formed by temperature quenching from a high-temperature/high-pressure hydrous melt. Temperature-dependent structure may change during such a cooling process and eventually gets frozen in at the temperature of the glass transition (Dingwell and Webb 1990). By definition, the glass transition temperature (actually a small temperature range), therefore, is that below which the material is not relaxed on the time scale of a measurement (glass), whereas above that temperature, the material is relaxed (liquid). In the temperature interval between a liquidus and glass transition temperature, the material is a supercooled liquid with the same property behavior as that of the melt above the melting temperature. These distinctions are important when a property measured on a glass is applied to the property behavior of its melt.
Principles of silicate melt structure
where XT and XO are the atomic proportions of tetrahedrally coordinated cations and oxygen, respectively.
where n is the number of bridging oxygen and mol fraction of individual Q n species. However, Q n species abundance obviously cannot be calculated from NBO/T values alone.
Solution mechanisms of silicate and water in fluids and melts in hydrous magmatic systems
Most structural data from hydrous silicate melts have been obtained from analysis of samples quenched from high temperature and pressure to ambient conditions prior to chemical and structural analysis. These data reflect, therefore, the melt structural environment near the glass transition temperature. Temperature-dependent structural features cannot be captured in such studies. That notwithstanding, many important principles have been derived from studies of quenched melt.
The behavior of an aqueous fluid in equilibrium with molten or crystalline silicates at high temperature and pressure may not be addressed by examination of quenched materials because most, perhaps all, of their properties (including the structure itself) cannot be determined by examination of the high-temperature/high-pressure fluid after quenching to ambient conditions. Fluid structure studies require, therefore, examination while the sample is at the temperature and pressure of interest. However, before addressing such experimental environments, structural data from quenched melts will be discussed.
Hydrous melts quenched from high temperature at high pressure
Water is dissolved in silicate melts in the form of water molecules, H2O0, and structurally bound hydroxyl groups, OH. The OH groups can form bonds with Si4+ and Al3+ as well as with other metal cations (Mysen and Virgo 1986; Xue and Kanzaki 2004; Cody et al. 2005). In either case, water dissolved in the form of OH groups in silicate melts affects their structure.
In chemically more complex systems, the OH-forming process also is more complex as will be discussed further below.
In this example, the network-modifying Na+ bonding with nonbridging oxygen in a Q3 species (with NBO/Si = 1) in an anhydrous melt reacts with H2O to form NaOH complexes in hydrous Na2O-SiO2 melts. This interaction causes the nonbridging oxygens bonded to Na+ in anhydrous Q3 to be transformed to bridging oxygens resulting in the formation of the more polymerized Q4 species. Silicon-29 MAS NMR data from melts quenched from 1,400°C along the Na2O-SiO2 join show that this is exactly the situation and that the abundance of NaOH complexes increases with increasing Na/Si (Cody et al. 2005). Similar conclusions have been reported for alkaline earth silicate glasses wherein Ca..OH and Mg..OH groups were formed in CaO-MgO-SiO2 melts (Xue and Kanzaki 2004).
From a compositional perspective, aluminosilicate melts are more akin to natural magmatic melts than metal oxide silicate melts. At pressures less than 5 to 6 GPa, Al3+ is in tetrahedral coordination where it is charge-balanced with alkalis or alkaline earths in a manner conceptually similar to that observed in crystalline aluminosilicates such as feldspars (see Lee et al. 2004; for high-pressure structural data). The aluminate groups (AlO2 -) in aluminosilicate melts can interact with dissolved water to form either Al-OH or metal-OH bonding (metal can be alkali metal or alkaline earth), or both, in addition to Si-OH bonding (Mysen and Virgo 1986; Schmidt et al. 2001). The extent to which aluminate interaction takes place is correlated with the Si/Al ratio of the melt (Mysen and Virgo 1986). The nature of the Al3+ charge balance probably also affects the solution mechanism because the Al-O bond strength depends on the electronic properties of the charge-balancing cation (Roy and Navrotsky 1984).
Additional complexity may exist because in melts with mixed M m+ cations and H+, the H+, because of its size for steric reasons, exhibits preference for forming OH groups in the silicate portion of the network by reacting with the nonbridging oxygen in Q n species with the largest number of nonbridging oxygens (Cody et al. 2005).
The decreasing ∂(NBO/T)/∂ with increasing water content, , reflects the decreasing rate of change of the abundance ratio, , as the total water content increases. This evolution, in turn, reflects the diminishing rate by which the Q n species changes with increasing concentration of water in the melt (Figure 16). These composition-dependent solution mechanisms of water in aluminosilicate melts also explain why the solubility of water in silicate melt at any temperature and pressure is significantly dependent on the bulk chemical composition of the melt itself.
Hydrous melts and aqueous fluids at high temperature and pressure
Experimental protocols have recently been implemented for examination of fluids and melts in hydrous silicate systems at deep crustal and mantle pressures and temperatures in situ while the sample is at the desired pressure and temperature conditions. Structural data obtained under such conditions are, therefore, increasingly available from all regions of silicate-H2O phase diagrams (Figure 4). In considering such data, commonly obtained in so-called hydrothermal diamond anvil cells (e.g., Bassett et al. 1994), the experiments usually are conducted in such a manner that pressure is a variable dependent on temperature. This means that increasing temperature normally is associated with increasing pressure. In the following discussion, this is the case unless otherwise indicated.
The system SiO2-H2O is too simple for modeling natural processes because neither Al2O3 nor alkali metals and alkaline earths are involved. The system Na2O-Al2O3-SiO2 is more realistic even though alkaline earths, in particular, have not yet been addressed. The Na2O-Al2O3-SiO2 system is also useful for characterization of the chemical interaction between nonbridging oxygen and important network-modifying cation (Na+) and protons (H+).
describes the equilibrium. Here, M denotes an alkali metal and where (M) and (H) indicate where alkali metals and protons form bonding with the relevant nonbridging oxygens, respectively. The tetrahedrally coordinated cations forming the Q n species can be either Al3+ or Si4+. The ∆H for this equilibrium (350 to 400 kJ/mol) is the same, within uncertainty for melt fluids and supercritical fluids (Mysen 2010a). With increasing Al/(Al + Si), equilibrium (11) likely shifts to the left (∆H decreases) because Al3+ will preferably occupy the most polymerized of available Q n species (Merzbacher and White 1991). In Equation 11, that species is Q3, but for other more polymerization melt compositions, Q4 species likely also would be involved. The principles outlined in equilibrium (11) may also be applied to alkaline earths, but quantitative information awaits further experiments. These are all considerations necessary for the application of the experimental data to hydrous magmatic systems. However, the necessary experimental data are at present insufficiently comprehensive for quantitative application.
Dissolved water and melt properties
The evolution of Q n species abundance of a melt with water content can be used to characterize how dissolved water governs phase relations and mixing properties of melts. For example, the rapid abundance increase of depolymerized species at the expense of polymerized species with water content of the melt enhances the stability of depolymerized relative to more polymerized liquidus phases. An example of this effect can be seen in the silica/pyroxene liquidus boundary of the Mg2SiO4-CaMgSi2O6-SiO2 system where the silica polymorph is more polymerized than pyroxene (their NBO/Si are 0 and 2, respectively) (Figure 2A). The magnitude of liquidus boundary shifts will reflect the size of the NBO/Si difference between the minerals coexisting along a liquidus boundary. The greater the NBO/Si difference, the greater is the effect of water on the shift of the boundary as illustrated, for example, by the different shifts of olivine/pyroxene and pyroxene/silica liquidus boundaries (Kushiro 1969). Effects such as these also explain why hydrous melts in equilibrium with peridotite mineral assemblages is more silica rich (quartz normative andesitic melts) than under anhydrous conditions (olivine normative tholeiitic melts) during melting and crystallization in the upper mantle.
where T g is glass transition temperature, T is the temperature of interest (T > T g), and C p conf(T g) is the configurational heat capacity at the glass transition temperature. This configurational heat capacity of hydrous magmatic melts is a systematic function of the water content of the melt (Richet et al. 1996; Bouhifd et al. 2006).
Water and fluid-melt equilibria
Stable isotope fractionation
The temperature and pressure effects in Figure 24 reflect the changes in silicate concentration and speciation in the coexisting aqueous fluid and silicate melts. Furthermore, different D/H values for different fluid densities again reflect the concentration and type of Q n species because the different density trajectories reflect pressure/temperature trajectories of the diamond cell experiments that followed different pressure paths (Mysen 2013). It follows from the different trajectories of D/H ratios in fluids and melts that the D/H partitioning between fluids and melts will also be dependent on temperature and pressure (Figure 25). Finally, in silicate mineral/aqueous fluid or silicate mineral/hydrous melt environments, temperature- and pressure-dependent partitioning will also take place because of the temperature/pressure dependence of the D/H fractionation with the fluid and melt phases.
Understanding the role of hydrous melts and silicate-rich fluids in transport processes depends sensitively on how chemical composition, temperature, and pressure govern the physicochemical properties of these materials (viscosity, diffusion, thermodynamics of mixing, element partitioning between phases, phase relations, etc.; see, for example, Mysen and Richet 2005, for review of experimental and theoretical information of structure-property relations of silicate glasses and melts). Attainment of this objective requires well-determined solubilities in and partitioning between melts, fluids, and crystalline phases, detailed understanding of the oxide solution mechanisms in melts and fluids, and determination of how fluid and melt structure governs those properties.
Structural information cannot be obtained directly on chemically complex natural systems because the resolving power of spectroscopic methods employed for such purposes diminishes rapidly with increasing chemical complexity. However, structural data from simpler binary and ternary systems can be used to describe the more complex systems. This objective requires, however, detailed characterization of silicate speciation in fluids and melts as a function of Al/Si ratio, the type of charge balance for tetrahedrally coordinated cations, and the type and proportion of network-modifying metals (alkali metals and alkaline earths). Currently, a combination of structural information and empirical relationships can be applied to describe liquidus phase relations and fluid/mineral/melt element and stable isotope partitioning. Transport properties can be understood and sometimes quantified in terms of configurational properties of individual Q n species. However, the experimental database used for these purposes dominantly is from alkali silicate and alkali aluminosilicate systems. This permits application to felsic magmatic systems. However, the lack of much information in alkaline earth aluminosilicate system makes quantitative application to hydrous basaltic less quantitative.
Many of the ideas and conclusions discussed in this review were developed during the preparation of invited lectures at Tohoku University, Japan in 2013. Portions of the reviewed research were supported by grants from the National Science Foundation (US) (EAR-0707861, EAR1250449, EAR12151931 and EAR-1212754).
- Adam G, Gibbs JH: On the temperature dependence of cooperative relaxation properties in glass-forming liquids. J Chem Phys 1965, 43: 139–146. 10.1063/1.1696442Google Scholar
- Antignano A, Manning CE: Rutile solubility in H 2 O, H 2 O -SiO 2 , and H 2 O-NaAlSi 3 O 8 fluids at 0.7–2.0 GPa and 700–1000 degrees C; implications for mobility of nominally insoluble elements. Chem Geol 2008, 255: 283–293. 10.1016/j.chemgeo.2008.07.001Google Scholar
- Audetat A, Keppler H: Viscosity of fluids in subduction zones. Science 2004, 303: 513–516. 10.1126/science.1092282Google Scholar
- Audetat A, Keppler H: Solubility of rutile in subduction zone fluids, as determined by experiments in the hydrothermal diamond anvil cell. Earth Planet Sci Lett 2005, 232: 393–402. 10.1016/j.epsl.2005.01.028Google Scholar
- Ayers JC, Watson EB: Apatite/fluid partitioning of rare-earth elements and strontium; experimental results at 1.0 GPa and 1000 degrees C and application to models of fluid-rock interaction. Chem Geol 1993, 110: 299–314. 10.1016/0009-2541(93)90259-LGoogle Scholar
- Bassett WA, Shen AH, Bucknum M, Chou IM: A new diamond cell for hydrothermal studies to 2.5 GPa and from -190˚C to 1200˚C. Rev Sci Instrum 1994, 64: 2340–2345.Google Scholar
- Behrens H, Jantos N: The effect of anhydrous composition on water solubility in granitic melts. Amer Miner 2001, 86: 14–20.Google Scholar
- Behrens H, Nowak M: The mechanisms of water diffusion in polymerized silicate melts. Contrib Miner Petrol 1997, 126: 377–385. 10.1007/s004100050257Google Scholar
- Behrens H, Meyer M, Holtz F, Nowak M: The effect of alkali ionic radius, temperature, and pressure on the solubility of water in MAlSi 3 O 8 melts (M=Li, Na, K, Rb). Chem Geol 2001, 174: 275–289. 10.1016/S0009-2541(00)00320-XGoogle Scholar
- Bernini D, Audetat A, Dolejs A, Keppler H: Zircon solubility in aqueous fluids at high temperatures and pressures. Geochim Cosmochim Acta 2013, 119: 178–187.Google Scholar
- Boettcher AL: The system SiO 2 -H 2 O-CO 2 : Melting solubility mechanisms of carbon and liquid structure to high pressures. Amer Miner 1984, 69: 823–834.Google Scholar
- Bottinga Y, Richet P: Silicate melts: The "anomalous" pressure dependence of the viscosity. Geochim Cosmochim Acta 1995, 59: 2725–2732. 10.1016/0016-7037(95)00168-YGoogle Scholar
- Bouhifd MA, Whittington A, Roux J, Richet P: Effect of water on the heat capacity of polymerized aluminosilicate glasses and melts. Geochem Cosmochim Acta 2006, 70: 711–722. 10.1016/j.gca.2005.09.012Google Scholar
- Boyd FR, England JL, Davis BCT: Effect of pressure on the melting and polymorphism of enstatite, MgSiO 3 . J Geophys Res 1964, 69: 2101–2109. 10.1029/JZ069i010p02101Google Scholar
- Buckermann W-A, Muller-Warmuth W, Frischat GH: A further 29 Si MAS NMR study on binary alkali silicate glasses. Glasstechnische Bericht 1992, 65: 18–21.Google Scholar
- Bureau H, Keppler H: Complete miscibility between silicate melts and hydrous fluids in the upper mantle; experimental evidence and geochemical implications. Earth Planet Sci Lett 1999, 165: 187–196. 10.1016/S0012-821X(98)00266-0Google Scholar
- Burnham CW: Thermodynamics of melting in experimental silicate-volatile systems. Geochim Cosmochim Acta 1975, 39: 1077–1084.Google Scholar
- Cody GD, Mysen BO, Lee SK: Structure vs. composition: A solid state 1 H and 29 Si NMR study of quenched glasses along the Na 2 O-SiO 2 -H 2 O join. Geochim Cosmochim Acta 2005, 69: 2373–2384. 10.1016/j.gca.2004.11.012Google Scholar
- Dingwell DB, Webb SL: Relaxation in silicate melts. Eur J Mineral 1990, 2: 427–449.Google Scholar
- Dixon JE, Stolper EM: An experimental study of water and carbon dioxide solubilities in mid-ocean ridge basaltic liquids; Part II, Applications to degassing. J Petrol 1995, 36: 1633–1646.Google Scholar
- Einstein A: Über die von der molekular-kinetischen Theorie der Wärme geforderte Bewegung von in ruhenden Flüssigkeiten suspendierten Teilchen. Ann Phys 1905, 17: 549–560.Google Scholar
- Eyring H: The activated complex in chemical reactions. J Chem Phys 1935, 3: 107–115. 10.1063/1.1749604Google Scholar
- Eyring H: The activated complex and the absolute rate of chemical reactions. Chem Rev 1935, 17: 65–77. 10.1021/cr60056a006Google Scholar
- Farnan I, Kohn SC, Dupree R: A study of the structural role of water in hydrous silica using cross-polarisation magic angle NMR. Geochim Cosmochim Acta 1987, 51: 2869–2874. 10.1016/0016-7037(87)90165-7Google Scholar
- Foustoukos DI, Mysen BO: D/H isotopic fractionation in the H 2 -H 2 O system at supercritical water conditions: Composition and hydrogen bonding effects. Geochim Cosmochim Acta 2012, 86: 88–102.Google Scholar
- Foustoukos DI, Mysen BO: H/D methane isotopologues dissolved in magmatic fluids: Stable hydrogen isotope fractionations in the Earth’s interior. Amer Miner 2013, 98: 946–954. 10.2138/am.2013.4419Google Scholar
- Grove TL, Elkins-Stanton LT, Parman SW, Chatterjee N, Muntner O, Gaetani GA: Fractional crystallization and mantle-melting controls on calc-alkaline differentiation trends. Contrib Miner Petrol 2003, 145: 515–543. 10.1007/s00410-003-0448-zGoogle Scholar
- Grove TL, Till CB, Krawczynski MJ: The roleof H 2 O in subduction zone magmatism. Ann Rev Earth Planet Sci 2012, 40: 413–439. 10.1146/annurev-earth-042711-105310Google Scholar
- Hack A, Thompson AB: Density and viscosity of hydrous magmas and related fluids and their role in subduction zone processes. J Petrol 2012, 52: 1333–1362.Google Scholar
- Hamilton DL, Burnham CW, Osborn EF: The solubility of water and the effects of oxygen fugacity and water content on crystallization of mafic magmas. J Petrol 1964, 5: 21–39. 10.1093/petrology/5.1.21Google Scholar
- Hess K-U, Dingwell DB: Viscosities of hydrous leucogranitic melts: A non-Ahrrenian model. Amer Miner 1996, 81: 1297–1300.Google Scholar
- Holloway JR, Jakobsson S: Volatile solubilities in magmas: Transport of volatiles from mantles to planet surfaces. J Geophys Res 1986, 91: 505–508. 10.1029/JB091iB04p0D505Google Scholar
- Holtz F, Behrens H, Dingwell DB, Johannes W: H 2 O solubility in haplogranitic melts: Compositional, pressure, and temperature dependence. Amer Miner 1995, 80: 94–108.Google Scholar
- Hunt JD, Manning CE: A thermodynamic model for the system SiO 2 -H 2 O near the upper critical end point based on quartz solubility experiments at 500–1100 degrees C and 5–20 kbar. Geochim Cosmochim Acta 2012, 86: 196–213.Google Scholar
- Jackson I: Melting of the silica isotypes SiO 2 , BeF 2 and GeO 2 at elevated pressures. Phys Earth Planet Int 1976, 13: 218–231. 10.1016/0031-9201(76)90096-0Google Scholar
- Jaeger WL, Drake MJ: Metal-silicate partitioning of Co, Ga, and W; dependence on silicate melt composition. Geochim Cosmochim Acta 2000,64(22):3887–3895. 10.1016/S0016-7037(00)00489-0Google Scholar
- Kawamoto T, Ochiai S, Kagi H: Changes in the structure of water deduced from the pressure dependence of the Raman OH frequency. J Chem Phys 2004, 120: 5867–5870. 10.1063/1.1689639Google Scholar
- Kennedy GC, Wasserburg GJ, Heard HC, Newton RC: The upper three-phase region in the system SiO 2 -H 2 O. Amer J Sci 1962, 260: 501–521. 10.2475/ajs.260.7.501Google Scholar
- Kohn SC, Schofield PF: The importance of melt composition in controlling trace-element behaviour: An exprimental study of Mn and Zn partitioning between forsterite and silicate melt. Chem Geol 1994, 117: 73–87. 10.1016/0009-2541(94)90122-8Google Scholar
- Kurkjian CR, Russell LE: Solubility of water in molten alkali silicates. J Soc Glass Techn 1958, 42: 130T-144T.Google Scholar
- Kushiro I: The system forsterite-diopside-silica with and without water at high pressures. Amer J Sci 1969, 267-A: 269–294.Google Scholar
- Kushiro I: Effect of water on the composition of magmas formed at high pressures. J Petrol 1972, 13: 311–334. 10.1093/petrology/13.2.311Google Scholar
- Kushiro I: Partial melting of mantle wedge and evolution of island arc crust. J Geophys Res 1990, 95: 15929–15939. 10.1029/JB095iB10p15929Google Scholar
- Kushiro I, Mysen BO: A possible effect of melt structure on the Mg-Fe 2+ partitioning between olivine and melt. Geochim Cosmochim Acta 2002, 66: 2267–2273. 10.1016/S0016-7037(01)00835-3Google Scholar
- Kushiro I, Yoder HS, Nishikawa M: Effect of water on the melting of enstatite. Geol Soc Amer Bull 1968, 79: 1685–1692. 10.1130/0016-7606(1968)79[1685:EOWOTM]2.0.CO;2Google Scholar
- Kushiro I, Syono Y, Akimoto SI: Melting of a peridotite nodule at high pressures and high water pressures. J Geophys Res 1968, 73: 6023–6029. 10.1029/JB073i018p06023Google Scholar
- Lee SK, Stebbins JF: The degree of aluminum avoidance in aluminum silicate glasses. Amer Miner 1999, 84: 937–945.Google Scholar
- Lee SK, Cody GD, Fei Y, Mysen BO: Nature of polymerization and properties of silicate melts at high pressure. Geochem Cosmochim Acta 2004, 68: 4189–4200. 10.1016/j.gca.2004.04.002Google Scholar
- Luth WC, Jahns RH, Tuttle OF: The granite system at pressures of 4 to 10 kilobars. J Geophys Res 1964, 69: 759–773. 10.1029/JZ069i004p00759Google Scholar
- Maekawa H, Maekawa T, Kawamura K, Yokokawa T: The structural groups of alkali silicate glasses determined from 29 Si MAS-NMR. J Non-Cryst Solids 1991,127(1):53–64. 10.1016/0022-3093(91)90400-ZGoogle Scholar
- Manning CE: The solubility of quartz in H2O in the lower crust and upper mantle. Geochim Cosmochim Acta 1994, 58: 4831–4840. 10.1016/0016-7037(94)90214-3Google Scholar
- Manning CE: The chemistry of subduction-zone fluids. Earth Planet Sci Lett 2004, 223: 1–16. 10.1016/j.epsl.2004.04.030Google Scholar
- McMillan PF: Water solubility and speciation models. In Volatiles in magmas. Edited by: Carroll MR, Holloway JR. Washington DC: Mineralogical Society of America; 1994:131–156.Google Scholar
- McMillan PF, Holloway JR: Water solubility in aluminosilicate melts. Contr Miner Petrol 1987, 97: 320–332. 10.1007/BF00371996Google Scholar
- Merzbacher CI, White WB: The structure of alkaline earth aluminosilicate glasses as determined by vibrational spectroscopy. J Non-Cryst Solids 1991, 130: 18–34. 10.1016/0022-3093(91)90152-VGoogle Scholar
- Mibe K, Kanzaki M, Kawamoto T, Matsukage KN, Fei Y, Ono S: Second critical endpoint in the peridotite-H2O system. J Geophys Res 2007., 112: doi: 10.1029/2005JB004125 doi: 10.1029/2005JB004125Google Scholar
- Moulson AJ, Roberts JP: Water in silica glass. Trans Faraday Soc 1961, 57: 1208–1216.Google Scholar
- Mysen BO: Water in peralkaline aluminosilicate melts to 2 GPa and 1400°C. Gechim Cosmochim Acta 2002, 66: 2915–2928. 10.1016/S0016-7037(02)00877-3Google Scholar
- Mysen BO: The solution behavior of H2O in peralkaline aluminosilicate melts at high pressure with implications for properties of hydrous melts. Geochim. Cosmochim. Acta, 71, 1820–1834. Geochim Cosmochim Acta 2007, 71: 1820–1834. 10.1016/j.gca.2007.01.007Google Scholar
- Mysen BO: Solution mechanisms of silicate in aqueous fluid and H 2 O in coexisting silicate melts determined in-situ at high pressure and high temperature. Geochim Cosmochim Acta 2009, 73: 5748–5763. 10.1016/j.gca.2009.06.023Google Scholar
- Mysen BO: Structure of H 2 O-saturated peralkaline aluminosilicate melt and coexisting aluminosilicate-saturated aqueous fluid determined in-situ to 800˚C and ~800 MPa. Geochim Cosmochim Acta 2010, 74: 4123–4139. 10.1016/j.gca.2010.04.024Google Scholar
- Mysen BO: Speciation and mixing behavor of silica-saturated aqueous fluid at high temperature and pressure. Amer Miner 2010, 95: 1807–1816. 10.2138/am.2010.3539Google Scholar
- Mysen BO: An experimental study of phosphorous and aluminosilicate speciation in and partitioning between aqueous fluids and silicate melts determined in-situ at high temperature and pressure. Amer Miner 2011, 96: 1636–1649. 10.2138/am.2011.3728Google Scholar
- Mysen BO: High-pressure/-temperature titanium solution mechanisms in silicate-saturated aqueous fluids and hydrous silicate melts. Amer Miner 2012, 97: 1241–1251. 10.2138/am.2012.4084Google Scholar
- Mysen BO: Silicate-COH melt and fluid structure, their physicochemical properties, and partitioning of nominally refractory oxides between melts and fluids. Lithos 2012, 148: 228–246.Google Scholar
- Mysen BO: Hydrogen isotope fractionation between coexisting hydrous melt and coexisting silicate-saturated aqueous fluid: An experimental study in-situ at high pressure and temperature. Amer Miner 2013, 98: 376–386. 10.2138/am.2013.4247Google Scholar
- Mysen BO, Virgo D: Trace element partitioning and melt structure; an experimental study at 1 atm pressure. Geochim Cosmochim Acta 1980,44(12):1917–1930. 10.1016/0016-7037(80)90191-XGoogle Scholar
- Mysen BO, Virgo D: Volatiles in silicate melts at high pressure and temperature. 1. Interaction between OH groups and Si 4+ , Al 3+ , Ca 2+ , Na + and H + . Chem Geol 1986, 57: 303–331. 10.1016/0009-2541(86)90056-2Google Scholar
- Mysen BO, Wheeler K: Solubility Behavior of Water in Haploandesitic Melts at high Pressure and high Temperature. Amer Miner 2000, 85: 1128–1142.Google Scholar
- Mysen BO, Cody GD: Solubility and solution mechanism of H 2 O in alkali silicate melts and glasses at high pressure and temperature. Geochem Cosmochim Acta 2004, 68: 5113–5126. 10.1016/j.gca.2004.07.021Google Scholar
- Mysen BO, Richet P Developments in geochemistry. In Silicate glasses and melts: properties and structure. New York: Elsevier; 2005.Google Scholar
- Mysen BO, Mibe K, Chou I-M, Bassett WA: Structure and equilibria among silicate species in aqueous fluids in the upper mantle: Experimental SiO 2 -H 2 O and MgO-SiO 2 -H 2 O data recorded in-situ to 900˚C and 5.4 GPa. J Geophys Res 2013., 118: doi:10.1002/2013JB010537 doi:10.1002/2013JB010537Google Scholar
- Nernst W: Zur Kinetik der in lösung befindtlicher Körper. Erste Abhandlung, Theorie der Diffusion. Z Phys Chem 1888, 2: 613–637.Google Scholar
- Newton RC, Manning CE: Solubility of enstatite+forsterite in H 2 O in deep crust/upper mantle conditions: 4 to 15 kbar and 700 to 900˚C. Geochim Cosmochim Acta 2002, 66: 4165–4176. 10.1016/S0016-7037(02)00998-5Google Scholar
- Newton RC, Manning CE: Solubility of corundum in the system Al 2 O 3 –SiO 2 –H 2 O–NaCl at 800 °C and 10 kbar. Chem Geol 2008, 249: 250–261. 10.1016/j.chemgeo.2008.01.002Google Scholar
- Nowak M, Behrens H: The speciation of water in haplogranitic glasses and melts by in-situ, near-infrared spectroscopy. Geochim Cosmochim Acta 1995, 59: 3445–3450. 10.1016/0016-7037(95)00237-TGoogle Scholar
- Ochs FA, Lange RA: The density of hydrous magmatic liquids. Science 1999, 283: 1314–1317. 10.1126/science.283.5406.1314Google Scholar
- Ohtani E, Taulelle F, Angell CA: Al 3+ coordination changes in liquid silicates under pressure. Nature 1985, 314: 78–81. 10.1038/314078a0Google Scholar
- Pascal ML, Anderson GM: Speciation of Al, Si, and K in supercritical solutions: Experimental study and interpretation. Geochim Cosmochim Acta 1989, 53: 1843–1856. 10.1016/0016-7037(89)90305-0Google Scholar
- Poli S, Schmidt MW: Petrology of subducted slabs. Ann Rev Earth Planet Sci 2002, 30: 207–235. 10.1146/annurev.earth.30.091201.140550Google Scholar
- Richet P: Viscosity and configurational entropy of silicate melts. Geochim Cosmochim Acta 1984, 48: 471–483. 10.1016/0016-7037(84)90275-8Google Scholar
- Richet P, Neuville DR: Thermodynamics of silicate melts: configurational properties. In Thermodynamic data: systematics and estimation. Advances in physical geochemistry, vol 10. Edited by: Saxena SK. New York: Springer; 1992:132–161.Google Scholar
- Richet P, Lejeune A-M, Holtz F, Roux J: Water and the viscosity of andesite melts. Chem Geol 1996, 128: 185–197. 10.1016/0009-2541(95)00172-7Google Scholar
- Richet P, Neuville DR, Holtz F: Viscosity of water-bearing melts. Terra Nova Abstr Supple 1997.,9(480):
- Roy BN, Navrotsky A: Thermochemistry of charge-coupled substitutions in silicate glasses:-The systems M n n+ AlO 2 - SiO 2 (M=Li, Na, K, Rb, Cs, Mg, Ca, Sr, Ba, Pb). J Amer Ceram Soc 1984, 67: 606–610. 10.1111/j.1151-2916.1984.tb19603.xGoogle Scholar
- Satherley K, Smedley SI: The electrical conductivity of some hydrous and anhydrous molten silicates-as a function of temperature and pressure. Geochim Cosmochim Acta 1985, 49: 769–777. 10.1016/0016-7037(85)90171-1Google Scholar
- Schmidt BC, Riemer T, Kohn SC, Holtz F, Dupree R: Structural implications of water dissolution in haplogranitic glasses from NMR spectroscopy: Influence of total water content and mixed alkali effect. Geochim Cosmochim Acta 2001, 65: 2949–2964. 10.1016/S0016-7037(01)00623-8Google Scholar
- Spallanzani L: Viaggi alle Due Sicilie e in alcune parti dell' Appennino, transl. as Travels in the Two Sicilies and Some Parts of the Appenines, J. Robinson, London. Comini, Pavia: Stamperia di B; 1798.Google Scholar
- Spera FJ: A thermodynamic basis for predicting water solubilties in silicatemelts and implications for the low velocity zone. Contr Mineral Petrol 1974, 45: 175–186. 10.1007/BF00383436Google Scholar
- Stebbins JF: Identification of multiple structural species in silicate glasses by 29 Si NMR. Nature 1987, 330: 465–467. 10.1038/330465a0Google Scholar
- Stern CR, Huang W-L, Wyllie PJ: Basalt-andesite-rhyolite-H 2 O: Crystallization intervals with excess H 2 O and H 2 O-undersaturated liquidus surfaces to 35 kilobars, with implications for magma genesis. Earth Planet Sci Lett 1975, 28: 189–196. 10.1016/0012-821X(75)90226-5Google Scholar
- Stolper E: The speciation of water in silicate melts. Geochim Cosmochim Acta 1982, 46: 2609–2620. 10.1016/0016-7037(82)90381-7Google Scholar
- Takata M, Acocella J, Tomozawa M, Watson EB: Effect of water content on the electrical conductivity of Na 2 O•3SiO 2 glass. J Amer Ceram Soc 1981, 64: 719–724. 10.1111/j.1151-2916.1981.tb15894.xGoogle Scholar
- Toplis MJ, Corgne A: An experimental study of element partitioning between magnetite, clinopyroxene and iron-bearing silicate liquids with particular emphasis on vanadium. Contrib Mineral Petrol 2002, 144: 22–37. 10.1007/s00410-002-0382-5Google Scholar
- Tuttle OF, Bowen NL: Origin of granite in light of experimental studies in the system NaAlSi 3 O 8 -KAlSi 3 O 8 -SiO 2 -H 2 O. Geol Soc Amer Mem 1958, 74: 1–153.Google Scholar
- Virgo D, Mysen BO, Kushiro I: Anionic constitution of 1-atmosphere silicate melts: implications of the structure of igneous melts. Science 1980, 208: 1371–1373. 10.1126/science.208.4450.1371Google Scholar
- Walrafen GE, Yang WH, Chu YC: Raman OD-stretching overtone spectra from liquid D 2 O between 22 and 152 decrees C. C. J Phys Chem 1996, 100: 1381–1391. 10.1021/jp952134iGoogle Scholar
- Wang YB, Cody SX, Cody GD, Mysen BO: 2H and 1H NMR study on hydrogen isotope effects in silicate glasses. San Francisco, CA: Paper presented at the 2011 AGU Fall Meeting; 2011.Google Scholar
- Wasserburg GJ: The effects of H 2 O in silicate systems. J Geol 1957, 65: 15–23. 10.1086/626402Google Scholar
- Watson EB: Diffusion in volatile-bearing magmas. In Volatiles in magmas: reviews in mineralogy. 30th edition. Edited by: Carroll MR, Holloway JR. Washington, DC: Mineralogical Society of America; 1994:371–411.Google Scholar
- Whittington APR, Holtz F: Water and the viscosity of depolymerized silicate melts. Geochim Cosmochim Acta 2000, 64: 3725–3736. 10.1016/S0016-7037(00)00448-8Google Scholar
- Xue Y, Kanzaki M: Dissolution mechanisms of water in depolymerized silicate melts: Constraints from 1 H and 29 Si NMR spectroscopy and ab initio calculations. Geochim Cosmochim Acta 2004, 68: 5027–5057. 10.1016/j.gca.2004.08.016Google Scholar
- Zhang Y-G, Frantz JD: Enstatite-forsterite-water equilibria at elevated temperatures and pressures. Amer Miner 2000, 85: 918–925.Google Scholar
- Zhang Y: H 2 O in rhyolitic glasses and melts: measurements, speciation, solubility, and diffusion. Rev Geophys Space Phys 1999, 37: 493–516. 10.1029/1999RG900012Google Scholar
- Zotov N, Keppler H: The influence of water on the structure of hydrous sodium tetrasilicate glasses. Amer Miner 1998, 83: 823–834.Google Scholar
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