Rhenium solubility and speciation in aqueous fluids at high temperature and pressure
Progress in Earth and Planetary Science volume 10, Article number: 58 (2023)
In order to characterize rhenium transport via infiltration of fluids in the Earth's interior, the solubility and solution mechanisms of ReO2 in aqueous fluids were determined to 900 °C and about 1710 MPa by using an externally–heated hydrothermal diamond anvil cell. In order to shed light on how Re solubility and solution mechanisms in aqueous fluids can be affected by interaction of Re with other solutes, compositions ranged from the comparatively simple ReO2–H2O system to compositionally more complex Na2O–ReO2–SiO2–H2O fluids. Fluids in the ReO2–SiO2–H2O, SiO2–H2O, Na2O–SiO2–H2O, and Na2O–ReO2–H2O systems also were examined. The presence of Na2O enhances the ReO2 solubility so that in Na2O–ReO2–H2O fluids, for example, Re solubility is increased by a factor of 10–15 compared with the Re solubility in Na2O-free ReO2–H2O fluids. The SiO2 component in ReO2–SiO2–H2O causes reduction of ReO2 solubility compared with ReO2–H2O fluids. The ReO2 solubility in the Na-bearing Na2O–ReO2–SiO2–H2O fluids is greater than that in fluids in both the ReO2–H2O and ReO2–SiO2–H2O systems. Rhenium is dissolved in aqueous fluid as ReO4-complexes with Re in fourfold coordination with oxygen. Some, or all, of the oxygen in these complexes is replaced by OH-groups depending on whether Na2O also is present. It is proposed that during dehydration of hydrated subduction zone mineral assemblages in the upper mantle, the alkali/alkaline earth ratio of the source of the released aqueous fluid affects the extent to which Re (and other HFSE) can be transported into an overlying peridotite mantle wedge. The infiltration of such fluids will, in turn, affect the Re content (and Re/Os ratio) of magma formed by partial melting of this peridotite wedge.
The rhenium distribution in the Earth's interior is heterogeneous perhaps because of Re transport by infiltrating aqueous fluids (D'Souza and Canil 2018). For example, significant Re enrichments in the mantle wedge overlying subducting plates near continental margins have been reported (Becker 2000; Sun et al. 2003; Tassara et al. 2018; Crossley et al. 2020). This enrichment could be the result of Re transfer from dehydrating slab materials to the overlying peridotite wedge during slab descent into the mantle. During partial melting of a peridotite wedge altered by the infiltrating fluids, its Re signature can be imparted on the partial melt. This signature could depend on temperature, pressure, redox conditions, bulk composition of the slab source of the fluid, and the fluid composition itself because those variables may affect the solubility of Re in the infiltrating fluid.
The solubility of an element in fluid can vary significantly depending on whether or not other solutes are present. For example, for a simple system such as Al2O3–H2O, the alumina solubility under deep crustal and upper mantle conditions is on the order of tens of ppm (Becker et al. 1983; Ragnarsdóttir and Walther 1985; Tropper and Manning 2007). However, in the presence of, in particular, alkali metals such as Na+ and K+, the Al2O3 solubility increases by several orders of magnitude (Anderson and Burnham 1983; Pascal and Anderson 1989; Diakonov et al. 1996; Wohlers et al. 2011). Similar solubility behavior has been reported for nominally insoluble minor and trace elements such as Ti4+ and Zr4+. In pure H2O at deep crustal and upper mantle temperature and pressure conditions, the TiO2 and ZrO2 solubility is on the order of a few to a few tens of ppm (Audétat and Keppler 2005; Antignano and Manning 2008; Mysen 2012, 2015; Bernini et al. 2013; Louvel et al. 2013). However, with other solutes such as alkali metals, and perhaps SiO2, under similar temperature and pressure conditions, both TiO2 and ZrO2 solubility increases by several orders of magnitude (Antignano and Manning 2008; Hayden and Manning 2011; Wilke et al. 2012, 2013; Mysen 2012, 2015, 2022). Rhenium may exhibit similar solution behavior, but relevant experimental data appear not to be available.
In order to characterize the influence of fluid transport on major, minor, and trace element concentrations in the Earth's interior, it is necessary to establish how their solubility in fluid and fractionation between fluid and condensed phases (magmatic liquid and mineral assemblages) depend on fluid composition, temperature, pressure, and, for some elements, redox conditions (see, for example, Pokrovski et al. 2013; Stefánsson et al. 2013, for reviews). It is also necessary to establish how interaction between other solutes affects solution mechanisms and solubility of elements of interest in the fluid (Diakonov et al. 1996; Azaroual et al. 1996; Wohlers et al. 2011; Manning 2018).
Whether, or the extent to which, interaction between rhenium and other solutes in fluids may take place, is not well known. However, in light of such effects on the solubility of other metals including geochemically similar elements (Bali et al. 2011, 2012; Ulrich and Mavrogenes 2008; Klein-BenDavid et al. 2011; Watenphul et al. 2014) and because of the importance of characterization of rhenium distribution in the Earth’s interior (e.g., Tassara et al. 2018; Crossley et al. 2020), examination of possible effects of Re complexing with other solutes on Re solubility and Re solution mechanisms in high-temperature/-pressure H2O-rich fluids relevant to upper mantle conditions is the principal objective of the present report.
2 Experimental methods
Examination of fluid-bearing samples comprised of ReO2 and other oxides was conducted experimentally while the samples were at the desired temperatures and pressures. Experiments were carried out in this way because structure and solubility of oxide components in aqueous fluids at high temperature and pressure cannot be determined with precision by examination of the fluids after their quenching back to ambient temperature and pressure.
Characterization while at high temperature and pressure was accomplished by using externally heated, hydrothermal diamonds cells (HDAC) based on the design by Bassett et al. (1994). The optical access through the diamond windows in these diamond anvil cells allows for petrographic and spectroscopic examination of the sample while at the temperature and pressure of interest. In the present study, samples were characterized with optical examination and Raman spectroscopy.
Four different Re-containing mixtures (ReO2–H2O, ReO2–SiO2–H2O, Na2O–ReO2–H2O, and Na2O–ReO2–SiO2–H2O) were used as starting materials to assess effects of interactions among dissolved components such as Na2O and SiO2 on rhenium speciation and solubility in aqueous fluids. In addition, two starting compositions without ReO2, but with SiO2 (SiO2–H2O and Na2O–SiO2–H2O), were employed to aid in the identification of spectroscopic features from Si–O bonding in species in (Si + Re)-bearing fluids.
The starting materials were comprised of double-distilled H2O, H2O with 1 molar NaOH, and spectroscopically pure crystalline ReO2 and SiO2. The Na- and Si-components were chosen as additional solutes because they have been demonstrated to cause pronounced solubility changes of components that are nearly insoluble in H2O alone (Pascal and Anderson 1989; Hayden and Manning 2011; Wilke et al. 2012; Louvel et al. 2013).
The samples in the HDAC were contained in 125 µm thick Re gaskets with a central 500 µm-diameter sample containment hole between the two opposing diamonds with 1 mm culets. Sample temperatures were monitored with two K-type thermocouples touching both the upper and lower diamonds of the HDAC. Temperature variations within the cell, assessed with NaCl melting, which melts at 801.5 °C at ambient pressure, were 2–3 °C.
Pressure in the hydrothermal diamond anvil cell was generated by increasing the temperature, which causes increased pressure from the H2O-rich fluid of the sample. This pressure is governed by the PVT properties of H2O (Wagner and Pruss 2002), or, more precisely, from the oxide-saturated aqueous fluids. However, because the sample volume varies with temperature and pressure, pressure calculations from PVT properties yield unreliable result. Moreover, the PVT properties of oxide-saturated fluids also are affected by such solutes (Mysen 2010; Wilke et al. 2013). Therefore, actual pressure was determined from the one-phonon Raman shift of synthetic 13C diamond. This Raman shift depends on pressure and temperature (e.g., Schiferl et al. 1997).
Pressure determination from the one-phonon Raman shift of the 13C diamond, placed within the fluid, was accomplished by using the pressure-/temperature-calibrated Raman shift (Mysen and Yamashita 2010). Carbon-13 diamond was used for this purpose to avoid interference of the Raman signal from the natural diamond anvils in the diamond anvil cell. The frequency difference between the one-phonon Raman shifts from natural diamond of the diamond anvils, which are nearly 100% carbon-12, and the synthetic carbon-13 diamond is about 80 cm−1 (Hanfland et al. 1985). The carbon-13 diamonds were synthesized with a CVD method where 13CH4 gas was the source of carbon from which to grow diamonds (Liang et al. 2013).
Raman spectra were recorded with a JASCO™ microRaman spectrometer equipped with confocal optics, a single monochromator, a holographic notch filter and holographic gratings. The confocal optics reduce the focal depth of the laser beam used to excite the sample, which, in turn, diminishes the potential for interference with a sample signal from adjacent materials. Raman excitation was achieved by using the 490 nm line of a Coherent MX-Series solid state laser with ~ 40 mW laser power at the sample.
For pressure determination with the one-phonon shift of the 13C diamond spectrum, 2400 grooves/mm grating density was employed to maximize accuracy of the spectrometer. This accuracy (± 1 cm−1) was improved further by using emission lines from a Neon lamp as internal standard. A ± 0.1 cm−1 frequency uncertainty is attained with this design. This uncertainty translates to a ± 40 MPa precision of pressure measurements. The overall pressure uncertainty in the HDAC experiments, which also incorporates the uncertainty in the pressure/temperature calibration of the one-phonon Raman shift of the carbon-13 diamond from Mysen and Yamashita (2010), is ± 110 MPa.
Each of the starting compositions was subjected to nearly the same temperature sequence. However, even though the temperatures were similar, the pressure–temperature trajectories of these individual experimental series differed because the proportion of fluid and solids (crystalline ReO2 and SiO2) differed in each experiment so that the fluid volume and, therefore, the pressure exerted by this fluid, was different. It is not feasible to load the same proportions of fluid and solids in the sample hole of the Re gaskets because of the small sample volume in the diamond cell sample containment design (volume ~ 15·10–3 mm3).
In each experimental temperature/pressure measurement series, the fluid + oxide sample was first brought to the highest planned temperature with its corresponding pressure and left there for about an hour prior to recording spectra while the sample remained at this temperature and pressure. Following measurements at a pressure/temperature condition, the next lowest temperature/pressure condition was reached with a 1 °C/s cooling rate. The 60-min dwell time at each temperature and pressure before spectroscopic measurements was considered sufficient to reach equilibrium with the present experimental configuration given that similar experimental duration has been shown sufficient to establish isotopic equilibrium between fluid and condensed phases at similar temperatures (Mysen 2015). Spectra of carbon-13 diamond were recorded at each temperature to determine the pressure.
3 Results and discussion
Crystalline ReO2 and SiO2 powders, together and individually, coexisting with aqueous fluid were present in the experiment (e. g., Fig. 1). The experiments were carried out in the 550–900 °C and about 150–1710 MPa temperature and pressure ranges, respectively (Fig. 2). The temperature–pressure relationships in Fig. 2 must be kept in mind, therefore, when reference is made to temperature of an experiment in this report.
3.1 Raman spectroscopy and solution mechanisms in fluid
Raman spectra were recorded in the 300–1200 cm−1 range (low-frequency range) where Raman signals from vibrations of Re–O and Si–O bonds can be detected. Raman signals in this frequency range were used, therefore, to examine structural features of oxide components dissolved in the aqueous fluid.
Spectra recorded in the 3000–4000 cm−1 range (high-frequency range) comprise signals assigned to stretch vibrations from OH-groups. These OH-groups can be a part of molecular H2O or as OH-groups that form bonding with metal cations dissolved in aqueous fluid.
3.1.1 Low-frequency range (300–1200 cm−1)
The Raman spectra of ReO2–H2O fluids in the 300–1200 cm−1 frequency range characteristically are comprised of three bands near 320 cm−1, 920 cm−1 and 960 cm−1, respectively (Fig. 3A). The same three bands were observed in spectra of Na2O–ReO2–H2O fluid. In addition, in this latter system, a fourth band was observed near 1040 cm−1 (Fig. 3B).
The 320, 920, 960 cm−1 bands in the spectrum of ReO2–H2O fluid occur at frequencies similar to those from Re–O vibrations in isolated ReO4 groups such as existing in crystalline ReO2 in which Re4+ is in fourfold coordination with oxygen and also from calculated spectra of isolated ReO4 groups (Busey and Keller 1964; Weinstock et al. 1973). It seems reasonably to conclude, therefore, that in fluids in the ReO2–H2O system, dissolved Re4+ also occupies fourfold coordination with oxygen perhaps forming isolated rhenate groups (ReO4).
The rhenium solution mechanism in aqueous fluid in the simple ReO2–H2O system, may be described, therefore, with the expression:
with the Re(OH)4 structure schematically illustrated in Fig. 4A.
The Raman band near 1040 cm−1 in the spectra of Na2O–ReO2–H2O fluid might reflect Re–O bonding in structural entities more polymerized than isolated ReO4 groups (i.e., containing Re–O–Re bridges). This suggestion is based on analogy with the Si–O vibrations of bridging oxygen in silicate melts and in silicate-saturated aqueous fluid at sufficiently high temperature and pressure to stability polymerized silica complexes (Virgo et al. 1980; Zotov and Keppler 2002; Mysen 2010). In such silicate complexes, Si–O symmetric stretch vibrations also result in a broad Raman band near 1040–1060 cm−1 (Furukawa et al. 1981; Lasaga 1982).
Although details of the structure of polymerized rhenate groups is not clear from the experimental data, by using relationships between SiO2 concentration and silicate polymerization in aqueous fluid and silicate melts as a guide (Mysen et al. 1982a, 2013), a pyrorhenate complex (Re2O7) seems most likely structural complex containing bridging oxygen. The solution mechanism of ReO2 in Na2O–ReO2–H2O fluids may then be described as follows:
In Eq. (2), the value of n defines distribution of H+ and Na+ bonded to nonbridging oxygen in the ReO4 and Re2O7 groups such as in Eq. (2) and illustrated schematically in Fig. 4B. From this information, the OH/Na abundance ratio in the orthorhenate groups (Na4−nReO4−2n(OH)2n) will always by greater than in the pyrorhenate group (Na6−2nRe2O7−2n(OH)2n) because the oxygen bridge between the two ReO4 groups in the pyrorhenate complex is not bonded to either H+ or Na+ (e.g., Fig. 4B). We also note that the relationships in Eq. (2) and Fig. 4B do not consider possible complexes in the fluids that include Na–OH bonding. In analogy with the structural interpretation of 1H and 29Si MAS NMR spectra of hydrous Na-silicate melts in which isolated NaOH groups were found to be common (Cody et al. 2005), NaOH-type complexes probably also exist in the Re-bearing fluids.
In the spectra of ReO2–H2O fluid, there is an approximately fourfold increase in integrated area of each of the three low-frequency bands with increasing temperature and pressure (from 600 °C/ ~ 600 MPa to 900 °C/ ~ 1700 MPa; see insert in Fig. 3A). If the Raman cross sections for these vibrations do not change with concentration and no other structural changes take place in the neighborhood of the Re–O bonds of interest, this observed intensity increase would correspond to a fourfold Re concentration increase in the fluids in this temperature and pressure range. Such a conclusion has been reported for sulfur species in aqueous fluids, for example (Schmidt and Seward 2017).
However, in the spectra of Na2O–ReO2–H2O fluids, the intensity of the three highest-frequency bands (920, 960, and 1040 cm−1) all decrease with increasing temperature and pressure, whereas the lower-frequency 320 cm−1 band intensity appears to pass through a maximum at intermediate temperature and pressure (insert in Fig. 3B). Additional structural complexity likely exists here as evidenced by the 1040 cm−1 band. As discussed above, this band probably reflects the presence of Re–O–Re bridges in the Re-complexes in these fluids. Under such circumstances, the intensity relations are not simply a function of the intensity of the Raman bands assigned to Re–O vibrations in other Re-bearing structural complexes in the fluid.
Raman spectra of fluid in systems that include both ReO2 and SiO2 (ReO2–SiO2–H2O and Na2O–ReO2–SiO2–H2O) are compared with the low-frequency spectra of ReO2-free equivalent systems (SiO2–H2O and Na2O–SiO2–H2O) in Fig. 5. The spectra of ReO2–SiO2–H2O fluids (Fig. 5A) include the same bands as those in fluid spectra from ReO2–H2O (320, 920, and 960 cm−1 bands; see also Fig. 3A). These three Raman bands are assigned to the same Re–O vibrations with Re in fourfold coordination with oxygen in the fluid (Re–O vibrations in ReO4 groups).
The spectra of ReO2–SiO2–H2O fluid recorded at the highest temperatures and pressures examined contain two or three additional bands near 470, 650, and 780 cm−1 (Figs. 3A and 5A). These bands were not observed in the ReO2–H2O fluid spectra. The 650 and 780 cm−1 bands also are evident in the spectra of SiO2–H2O fluid (Fig. 5B). In the spectra of SiO2–H2O fluids, there is also a weak band near 900 cm−1. In spectra of both Re-bearing (Fig. 5A, C) and Re-free (Fig. 5B, D) fluids with SiO2, the integrated Raman intensities of the latter bands grow with increasing temperature and pressure (Fig. 6). Their intensities in the spectra of Re-free SiO2–H2O fluid exceed those in the spectra of ReO2–SiO2–H2O fluid (Fig. 6).
The 650, 780, and 900 cm−1 Raman bands in the spectra of SiO2–H2O and ReO2–SiO2–H2O fluid are assigned to Si–O vibrations in silicate-bearing fluid species. In other structural studies of silicate speciation in SiO2–H2O fluids at high temperature and pressure, the 780 cm−1 band has been assigned to Si–O stretch vibrations in isolated SiO4 tetrahedra with H+ attached to oxygen in the corners of those tetrahedra (Zotov and Keppler 2000; Mysen 2010, 2009). In the SiO2–H2O fluids, there are two additional bands, near 650 and 900 cm−1, respectively, as well as another band near 1040 cm−1 (Fig. 5D). The 650 cm−1 is assigned to Si–O–Si bending vibrations in polymerized silicate structures (Zotov and Keppler 2002), and the 1040 cm−1 band to Si–O stretch vibrations of bridging oxygen bonds (Furukawa et al. 1981; Lasaga 1982; Mysen et al. 1982a). The existence of those two bands do not define the number of oxygen bridges in this silicate structure, and merely the existence of bridging oxygens, which exist in all polymerized silicate structures. However, the 900 cm−1 band most likely should be assigned to Si–O stretching of a nonbridging Si–O bond in pyrosilicate (Si2O7) structure in silicate melts and silicate-saturated aqueous fluids (Lasaga 1982; Seifert et al. 1982; Mysen 2009). This assignment also is consistent with the assignments of the 650 and 1040 cm−1 bands.
The simplest solution mechanism of SiO2 in the SiO2–H2O fluids under the conditions of the present experiments can be described with the equation;
In the SiO2–H2O fluids, all the terminal oxygens in the SiO4 groups have been replaced by OH groups. In the Si2O7 groups, all six terminal oxygens (nonbridging oxygens) have been replaced by OH groups. There is no H+ bonded to the single bridging oxygen model in this model (see also Fig. 4C). These silicate structures are, therefore, analogous to the rhenate structures in ReO2–H2O, ReO2–SiO2–H2O, and Na2O–ReO2–SiO2–H2O fluids in which Re4+, instead of Si4+, occupies the central position in the oxygen tetrahedra (compared Fig. 4B, C).
Silicate species in Na2O–SiO2–H2O also include Si2O7 groups. In this latter system, the solution mechanism of silica, not including possible NaOH complexes, can be written as;
with the structure of the silicate species illustrated in Fig. 4E. Here, as in expression (2), both H+ and Na+ form bonding with terminal oxygen in the tetrahedra. Their proportion is governed by the value of n.
The Raman band near 650 cm−1 in the spectra of fluids in the ReO2–SiO2–H2O system at the highest temperatures and pressures and in the spectra SiO2–H2O fluids at all temperatures and pressures, remains assigned to –O– bending vibrations. This means that the 650 cm−1 band in the spectra of ReO2–SiO2–H2O fluids implies that some of the SiO4 tetrahedra are more polymerized than an isolated SiO4 tetrahedron. However, whether this bridging oxygen is from Re–O–Re, Re–O–Si, or Si–O–Si bridges cannot be determined from the Raman spectra. In the sketch in Fig. 4D, this feature in ReO2–SiO2–H2O fluid is assumed to be Si–O–Si bridges resembling the structural features of SiO2–H2O fluids.
Because an intense 780 cm−1 band remains in the ReO2–SiO2–H2O fluid spectra, isolated SiO4 groups coexist with the more polymerized complexes in those fluids. The 900 cm−1 band in the spectra of high temperature and pressure ReO2–SiO2–H2O fluids and in all the fluids from the SiO2–H2O system is assigned to Si–O stretch vibrations this polymerized silicate complex. This assignment is consistent with the assignment of the 650 cm−1 band because the 900 cm−1 together with that near 650 cm−1 is considered typical whenever Si2O7 entities (with one Si–O–Si bridge per Si) exist in the structure (Furukawa et al. 1981).
Rhenium is considerably heavier than Si. So, if we assume that the 900 cm−1 should be assigned to Re–O stretch vibrations in hypothetical Re2O7 or ReSiO7 complexes, it is likely, that the frequency of Re–O stretch vibrations in such complexes would be at frequencies quite different, and likely lower much lower, than that of the Si–O stretch vibrations in an Si2O7 complex (Brawer and White 1975). It is concluded, therefore, that most likely the polymerized species in ReO2–SiO2–H2O fluid is Si2O7.
From this structural interpretation of the ReO2–SiO2–H2O spectra, the ReO2 + SiO2 solution mechanism in aqueous can be formulated with an expression such as:
Schematic structure of coexisting silicate and rhenate complexes in the ReO2–SiO2–H2O fluids are illustrated in Fig. 4D.
In SiO2-bearing systems that also include Na2O such as in the system Na2O–ReO2–SiO2–H2O, the spectra of their fluid comprise the same three bands as in the spectra of fluids in the Na2O–ReO2–H2O. These bands were assigned to Re–O vibrations in ReO4 groups (Figs. 3B and 5C). There is no evidence for polymerized rhenate complexes in the Na2O–ReO2–H2O fluids. In addition, in the Na2O–ReO2–SiO2–H2O fluid spectra, there is a weak band near 780 cm−1. This band becomes more intense with increasing temperature and pressure (Figs. 5C and 6C). As in fluid spectra of other SiO2-bearing systems, this band is assigned to Si–O stretch vibrations in isolated SiO4 groups. However, none of the other bands assigned to Si–O stretch vibrations of silicate species such as in the spectra of the Na2O-free ReO2–SiO2–H2O fluids and ReO2-free Na2O–SiO2–H2O fluids were observed in the Na2O–ReO2–SiO2–H2O fluid spectra (Fig. 5). The silicate species in Na2O–ReO2–SiO2–H2O fluids is, therefore, only isolated SiO4 tetrahedra where both H+ and Na+ form bonding with the terminal oxygen in this species.
The complete solution mechanism of rhenate and silicate in Na2O–ReO2–SiO2–H2O fluids can then be written as:
as also illustrated in the structural schematic in Fig. 4F.
3.1.2 High-frequency range (3000–4000 cm−1)
The high-frequency range of the Raman spectra of the aqueous fluids, between 3000 and 4000 cm−1, comprises Raman bands assigned to O–H stretch vibrations from H2O molecules and from OH-groups bonded to cations such as Si4+ and alkali metals, for example (Walrafen et al. 1986; Mysen and Virgo 1986; Le Losq et al. 2011). Bonding of OH-groups to rhenium cations to form Re–OH bonds also result in O–H stretch vibrations that give rise to Raman bands in this frequency range. This Raman intensity envelope, with peak maximum typically between 3550 and 3600 cm−1, will be referred to as the 3600 cm−1 envelope.
The exact frequency or frequencies of Raman bands assigned to O–H vibrations in OH groups bonded to various metal cations depends somewhat on the electronic properties of the metal cation because electronic properties of the metal cation(s) will affect the strength, and, therefore, the frequency of O–H vibrations of the O–H bonds. For example, the frequency decreases as the metal cation becomes more electropositive (Mysen and Virgo 1986). Hydrogen bonding also will cause a frequency change (Walrafen et al. 1988, 1999; Frantz et al. 1993; Le Losq et al. 2015).
Quantitative evaluation of various possible OH-environments based on interpretation of the 3600 cm−1 envelope alone can be challenging, however, because of the often small frequency differences between of individual Raman bands of different OH stretch vibrations in the 3600 cm−1 envelope. Temperature and to some degree, pressure, also affect the topology and frequency of the 3600 cm−1 envelope at least in part because the extent of hydrogen bonding is sensitive to temperature and pressure (Walrafen et al. 1988; Frantz et al. 1993; Kawamoto et al. 2004; Hoffmann and Conradi 1997; Sahle et al. 2013). Hydrogen bonding does, however, diminish rapidly with increasing temperature (Walrafen et al. 1988; Frantz et al. 1993; Foustoukos and Mysen 2012). Signals from hydrogen bonding typically cannot be detected at temperature above about 600–650 °C (Foustoukos and Mysen 2012). Effects of composition on the 3600 cm−1 envelope topology are not likely, therefore, to be significantly affected by effects of hydrogen bonding because for the most part experiments were conducted and above this temperature.
The high-frequency envelope in the temperature and pressure range of the present experiments (550–900 °C and about 380–1710 MPa) has a single maximum between 3500 and 3600 cm−1. This envelope is slightly asymmetric to its low-frequency side of the ~ 3600 cm−1 intensity maximum (Figs. 7 and 8). This asymmetry may be because of different metal-OH bonds, hydrogen bonding, or both. The asymmetry also can be observed in spectra of pure H2O (Fig. 7A, B), which also illustrate how the abundance of hydrogen bonding decreases with increasing temperature (Frantz et al. 1993; Hoffmann and Conradi 1997; Foustoukos and Mysen 2012). This abundance evolution is reflected in decreasing intensity of O–H vibrations on the low-frequency side of the O–H envelope in the high-temperature spectra of pure H2O (Walrafen et al. 1988, 1999; Frantz et al. 1993).
Information on how the high-frequency spectra from Re- and Si-bearing fluid systems respond to temperature and pressure variations was extracted from difference spectra where Raman bands from lower temperature and pressure were subtracted from those recorded at higher temperature and pressure. These spectra were normalized to the same Raman measurement conditions before subtraction.
Difference spectra for pure H2O are illustrated in Fig. 7B. The sharp intensity dip near 3550 cm−1 in these spectra as well as in those from fluids from the other system reflects the fact that the peak maxima of these envelopes shift to lower frequencies with increasing temperature. Therefore, when subtracting a higher-from a lower-temperature spectrum a negative dip will occur near the intensity maximum of the lower-temperature spectrum.
The latter complication aside, the intensity on the low-frequency side of the high-frequency envelope from pure H2O becomes less pronounced the higher the temperature, features that are similar to those originally reported by Walrafen et al. (1988) (Fig. 7B). This spectral evolution also is the primary cause of the decreased full width at half height (FWHH) of this envelope as the temperature is increased (Fig. 7C). This decrease reflects decreasing abundance of hydrogen bonding.
The spectral topologies of the high-frequency envelope from fluids in all systems resemble one another (Fig. 8). The spectra become narrower with increasing temperature (Fig. Fig. 8E, J, M, P). There are, however, differences in detail depending on the specific system considered because the rate of change of FWHH with temperature, ∂FWHH/∂T, differs somewhat in the spectra of the various systems (Fig. 8P, Q). This FWHH change with temperature is emphasized in the difference spectra (Fig. 8B, D, G, I, L, O).
The FWHH of spectra of fluids from the Na2O–ReO2–H2O system is greater than that in the fluid spectra from the Na-free, ReO2–H2O system (Fig. 8A, E, F, J; see also summary in Fig. 8P). Moreover, the ∂FWHH/∂T of spectra in the Na2O–ReO2–H2O system exceeds that of the compositionally simpler and Na-free ReO2–H2O system spectra (Fig. 8Q). One might infer that these differences reflect some effect on the OH bond strength of dissolved rhenate complexes when Na2O is added to the ReO2–H2O system.
To create Re-OH bonding in Na2O–ReO2–H2O fluids, one or more terminal oxygen in the ReO4 tetrahedra is replaced with one or more OH groups and one or more ONa groups. Details of how Na-OH complexes may be linked to rhenate and/or rhenate/silicate structures in the aqueous fluids cannot be inferred from existing information. The Na+ might form isolated NaOH groups analogous to the NaOH groups detected from NMR spectra of hydrous Na2O–SiO2 melts (Cody et al. 2005). However, more complex structures involving, for example, Na+ linked to nonbridging oxygen in ReO4 groups but also comprising Na–OH bonds, might also be involved.
The latter differences resemble those between the Re-free SiO2–H2O and Na2O–SiO2–H2O high-frequency spectra (Fig. 8C, D, F, H, I, J). The structural interpretation of those differences spectra likely reflects effects of different O–H bond strength depending on the extent to which the OH-group forms bonding with Si4+ and Na+. In the SiO2–H2O fluids, there can be only Si–OH bonding. The wider 3600 cm−1 envelope from Na2O–SiO2–H2O fluid compared with the spectra of SiO2–H2O fluid is because there is some Na–OH bonding in the Na2O–SiO2–H2O fluid. The O–H stretch vibrations from the OH-groups in Na-OH bonds result in Raman bands on the low-frequency side of the 3600 cm−1 envelope (Mysen and Virgo 1986; Mysen 2018).
In high-frequency spectra of fluids equilibrated with ReO2 + SiO2 (ReO2–SiO2–H2O) or ReO2 + SiO2 + Na2O (Na2O–ReO2–SiO2–H2O), the evolution of their 3600 cm−1 envelopes is affected by the presence of SiO2 (Fig. 8K, L, N, O). For example, for ReO2–SiO2–H2O fluids, the temperature-dependent asymmetry on the low-frequency side of their 3600 cm−1 Raman intensity envelope is less pronounced than in the 3600 cm−1 envelope in spectra of fluids in the SiO2-free ReO2–H2O system (Fig. 8A, B, D, G). Moreover, the ∂FWHH/∂T of the 3600 cm−1 envelope in the ReO2–SiO–H2O and SiO2–H2O systems is essentially identical (Fig. 8Q). This similarity may reflect greater abundance of the SiO2 components than the ReO2 components in the ReO2–SiO2–H2O fluid, so that the evolution of the FWHH with temperature is dominated by the width of intensity contributions from OH-groups in Si–OH bonds in both systems. It is unlikely that these effects could reflect hydrogen bonding because at the high temperatures of these experiments, hydrogen bonding cannot be detected in aqueous fluids (Foustoukos and Mysen 2012).
Addition of SiO2 to the Na2O–ReO2–H2O fluids results in 3600 cm−1 envelopes resembling that of fluid in the ReO2–SiO2–H2O system (Fig. 8K, N) more than the 3600 cm−1 envelope in the NaO–ReO2–H2O spectra (Fig. 8F). This similarity can also be seen in the temperature-dependent FWHH, but this ∂FWHH/∂T differs significantly from the ∂FWHH/∂T of Na2O–ReO–H2O (Fig. 8Q). It is also notable that the temperature evolution of the 3600 cm−1 from Na2O–SiO2–H2O fluids is significantly different from that of the Na2O–ReO2–SiO2–H2O fluids (Figs. 8H, I, N, O, Q). This may be consistent with Si–OH bonding dominating in both the ReO–SiO2–H2O and Na2O–ReO2–SiO2–H2O fluids.
3.2 Species abundance in aqueous fluid
Integrated areas Raman bands from scattering of bonds in species dissolved in fluid, in principle can be transformed to species abundance. This can be done provided that a specified Raman intensity is calibrated against integrated intensity of Raman bands assigned to the same type of vibrations in spectra of a material with similar local structure and with known concentration of the type of bonding under consideration (Mysen 2015, 2018). However, in order for this method to yield reliable results, it is necessary that the optical absorption of the unknown and known materials does not differ.
This method has been applied successfully to abundance measurements of silicate species from Si–O vibrations in SiO2-saturated aqueous fluids in equilibrium with quartz and TiO2-saturated fluid in equilibrium with rutile (Mysen 2015, 2018). The method also has been used to report equilibria between structural units in silica-saturated H2O at high temperature and pressure (Zotov and Keppler 2002; Mysen 2010). However, whenever the speciation changes or other local structural features surrounding a structural complex change, this method cannot be used.
In the present systems, a crystalline material to serve as calibrant for abundance in fluid could be ReO2, for example. However, as seen in Fig. 1, the ReO2 crystals are considerably darker than surrounding fluid. These crystals do, therefore, absorb a larger fraction of the incident laser light and a weaker Raman signal will be recorded from the sample than from a clear and colorless sample such as the surrounding aqueous fluids. Quantitative estimates of abundance of dissolved components in fluids in equilibrium with crystalline ReO2, therefore, could not be carried out. As a result, only relative abundance variations from the fluid spectra will be discussed here.
An example of low-frequency Raman spectra from fluids in the four Re-bearing compositions recorded at 700 °C (but, therefore, at different pressures) illustrates how the overall composition of a system effects on the integrated intensity of Raman bands assigned to Re–O vibrations (Fig. 9), and, therefore, at least in principle, abundance of Re-components in fluids. Spectra recorded at different temperatures (and pressures) than those shown in Fig. 9 resemble those in Fig. 9.
For the 960 cm−1 band, the intensity at 700 °C, which is proportional to the abundance of isolated ReO4 complexes in fluid in most of the systems under study, increases from that of the ReO2–H2O fluids (referenced as 100%) to as much as 163% for this band in the Raman spectrum of fluid in the Na2O–ReO2–H2O system at the same temperature, but different pressure (Fig. 9). This intensity (and abundance) increase is 143% for the fluids in chemically more complex system, Na2O–ReO2–SiO2–H2O. It decreases to 23% for the ReO2–SiO2–H2O system compared with the spectrum of ReO2–H2O system (Fig. 9).
The relative Re-species abundance differences illustrated in terms of different Raman intensity in the example in Fig. 9 very likely are near minimum values because the pressures in those 4 systems at 700 °C illustrated in this Figure are different and range from 380 to 1450 MPa for the Na2O-bearing systems and from about 1000 to 1710 MPa for the data from fluids in systems without Na2O (see exact pressures in Fig. 2 and also attached to each system designation for the 700°C spectra in Fig. 9).
Compared with alkali-free, but SiO2-bearing systems, the ReO2 solubility difference could differ by as much as a factor of 15–16 at temperatures near 800 °C compared to about a factor slightly less than 10 near 600–700 °C (Fig. 10). The solubility difference between the two Na2O-bearing systems (Na2O–ReO2–SiO2–H2O and Na2O–ReO2–H2O) is near 2 at the lowest temperatures to about 3 at the highest temperatures (Fig. 10).
Density of the aqueous fluids has been suggested to be a more appropriate means with which to compare solubility in the fluids in the various systems at temperatures and pressures because density is linked to both temperature and pressure (Kennedy 1950; Burnham et al. 1969; Wagner and Pruss 2002; Sanchez-Valle 2013) and because fluid density has been shown to be a variable that can be correlated oxide solubility in the fluid (Manning 1994; Pokrovski et al. 2005). For example, the rhenium solubility in fluid in the Na2O–ReO2–H2O system can increase by 400–500% between 700 and 900 °C because pressure increases from 770 to 1075 MPa in this temperature range in this system. The H2O density increases from ~ 0.7 to ~ 0.9 g/cm3 (Burnham et al. 1969).
The intensity ratio changes of the 960 cm−1 band with temperature (and pressure) is consistent with the increased Re abundance as the density of aqueous fluid increases. It is also clear, for example, that for the systems where only isolated ReO4 groups exist in the fluid (ReO2–H2O, ReO2–SiO2–H2O, and Na2O–ReO2–SiO2–H2O), the relative rhenium concentration in fluid at constant fluid density increases by about an order of magnitude between ReO2–SiO2–H2O and ReO2–H2O and by another approximately order of magnitude from ReO2–H2O fluids and Na2O–ReO2–SiO2–H2O fluids (Fig. 11). The data for the NaO–ReO2–H2O fluids differ because in this case some of the ReO2 in the aqueous solution exists in more polymerized form than isolated ReO4 tetrahedra. The integrated intensity of the 960 cm−1 band from those fluids is not, therefore, an appropriate expression of the ReO2 solubility in the aqueous fluids.
In order to understand better the role of SiO2 in the structural complexes of the solutes in the aqueous fluids, it is instructive to assess the differences in integrated areas of bands assigned to Si–O vibrations in fluids with and without ReO2 in the system. As an example, the degree of polymerization of Si–O species in SiO2-bearing, but ReO2-free fluids generally is greater than when both ReO2 and SiO2 are present such as Na2O–SiO2–H2O compared with Na2O–ReO2–SiO2–H2O, for example. In the Na2O–ReO2–SiO2–H2O fluids, for all practical purposes there is evidence only for isolated OH-containing SiO4 entities (the 780 cm−1 band in those spectra). Even in the latter case, the intensity ratio of the 780 cm−1 band [assigned to Si–O− stretch vibrations in Si(OH)4 complexes] to that of the simpler ReO2-free Na2O–SiO2–H2O system is only about 0.2 as compared with about 0.6 for the intensity ratio of the 780 cm−1 band, ReO2–SiO2–H2O/SiO2–H2O (Fig. 10B).
It follows from these observations that not only does Na2O affect the structure and solubility of ReO2 complexes in aqueous fluids, but SiO2 also has an influence on those properties. In all systems, however, Si4+ and Re4+ in aqueous fluid remain in fourfold coordination with oxygen.
The Re solubility in aqueous fluids can vary by more than an order of magnitude in the temperature–pressure regime of the deep crust and upper mantle because of formation of complexes that also involves chemical interaction with other solutes. The solubility of such Re-bearing complexes is, in particular, dependent on the presence of alkali metals in the fluid. In this respect, the solubility behavior of rhenium in aqueous fluids resembles that of Ti4+ and Zr4+ (Antignano and Manning 2008; Hayden and Manning 2011; Wilke et al. 2012, 2013; Mysen 2012, 2015, 2022).
It is likely that the electronic properties of the metal cation in metal oxide-bearing fluids (i.e., alkali metals versus alkaline earth) could also affect Re solubility. In the case of SiO2 solubility, for example, increasing electronegativity of the metal cation results in decreased silicate solubility at the same temperature and pressure such as when comparing the effects of Mg2+, Ca2+, and Na+ on solubility of SiO2, for example (Mysen et al. 2013; Mysen 2018).
Aqueous fluids from dehydrating slabs infiltrating overlying peridotite source can trigger partial melting in the peridotite wedge in subduction zones (Peacock 1993; Iwamori 1998; Schmidt and Poli 2014). It follows that the Re/Os budget in subduction zone peridotite affected by such fluids will depend on both the composition of the source of the fluid under which dehydration takes place. Such variations, in turn, can affect the Re-Os isotope systematics of source regions of magma in the Earth's upper mantle and, therefore, the Re-Os isotope systematics of magma itself.
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Mysen, B. Rhenium solubility and speciation in aqueous fluids at high temperature and pressure. Prog Earth Planet Sci 10, 58 (2023). https://doi.org/10.1186/s40645-023-00590-y