Abstract

Experimental and theoretical evidence for the coupled substitution of B and H in synthetic forsterite and a natural olivine is presented. The intensities of OH bands at 3704 cm−1 (//z), 3598 cm−1 (//x,y), and 3525 cm−1 (//x) in a heterogeneous B-doped synthetic forsterite crystal matches the zoning of B concentration measured by ion probe. The two anti-symmetric stretching vibrations of BO3 groups occur at 1301 cm−1 (//x) and 1207 cm−1 (//z) for the 10B and at 1256 and 1168 cm−1 for the 11B isotope. A microscopic model of the mixed (B,H) defect that accounts for experimental observations is obtained from quantum mechanical calculations. The BO3 group lies on the (O3-O1-O3) face of the vacant Si site and the H atom is bonded to the O2 atom at the remaining apex. The occurrence of the same OH bands associated with ν3 BO3 vibrations in a natural olivine sample from Pakistan confirms the occurrence of this defect in nature. The three diagnostic OH bands can be used as a signature of H associated with boron substitution in olivine and forsterite, leading to a quantitative analysis of their contribution to H-defects.

Introduction

The coupled substitution of B and H for Si, formally written as B(OH)Si–1O–1, is not considered a major hydrogen incorporation mechanism in olivine because most natural samples contain too little B (less than a few wt. ppm B) (Kent and Rossman 2002). However, this mechanism could be dominant in samples with anomalously high B concentrations (Kent and Rossman 2002). It has once been proposed to explain a B-rich olivine from the Tayozhnoye Fe deposit in Russia (Grew et al. 1991; Sykes et al. 1994). Unfortunately, due to the presence of other types of OH defects in natural samples, significant uncertainty remains in the position of the OH bands associated with the B(OH)Si–1O–1 substitution and in the nature of the defect (Sykes et al. 1994). In addition, attempts to synthesize B-doped forsterite with associated H defects were not successful (Berry et al. 2007).

In this letter, we identify for the first time the coupled H and B substitution in a synthetic forsterite sample by experiment and theory. The corresponding defect generates characteristic infrared (IR) absorption bands, which compare well with those obtained from a quantum-mechanical modeling of mixed B and H defects in tetrahedral sites of forsterite. The IR analysis of a natural B-bearing olivine from the same origin as that studied by Gose et al. (2008, 2010) confirms the B(OH)Si–1O–1 substitution as a H-incorporation mechanism in nature.

Samples and methods

The forsterite crystal was synthesized by Lemaire et al. (2004) from hydrous melt at 2 GPa by cooling from 1400 to 1275 °C under medium-to-high silica activity. A single, unoriented, double-polished slice (~1.0 × 0.7 mm2 and 240 μm thick) was used for IR measurements. A crystal from the same batch was studied by Ingrin et al. (2013). Two samples of B-bearing olivine from the Kaghan Valley (Pakistan) were used (Gose et al. 2010). One is the piece containing 72 wt. ppm H2O described by Kovács et al. (2008). It is a parallelepiped of 1.882 × 1.936 × 1.962 mm3 with faces perpendicular to the crystal axes, and was used for recording OH stretching bands. The other crystal was cut in two thin slices (380 and 285 μm thick) to study the polarization of the B-O stretching vibrations in the (x,y) and (x,z) planes, respectively. The OH IR signature of both samples is identical to the one reported by Gose et al. (2010). Previous TEM studies on the forsterite (Lemaire et al. 2004) and Pakistan olivine (Gose et al. 2010) have shown the absence of inclusions down to the sub-micrometer scale.

IR spectra were acquired with a Bruker Hyperion 3000 FTIR-microscope attached to a Bruker Vertex 70 spectrometer equipped with a liquid-N2-cooled MCT detector in the laboratory of infrared and Raman spectrochemistry (LASIR, Université Lille 1). A Linkam FTIR600 heating-cooling stage with ZnSe windows was used for low-temperature conditions (see Ingrin et al. 2013 for more details). Spot sizes of 100 × 100 and 60 × 60 μm2 were used for low-temperature and room-temperature measurements, respectively, and 256 scans were accumulated per spectrum. Polarized spectra were recorded with a wire grid polarizer on a KRS-5 substrate in the microscope.

The B content was determined with a Cameca IMS 1270 ion microprobe at CRPG. A 13 kV, 16 nA O primary beam was focused on a 25 μm diameter area, and the 10 kV positive secondary ions was measured at a mass resolution of 1500 with an energy offset of 60 V through an energy slit of 30 V. A single collector was used in ion-counting mode, and each analysis consisted of 25 successive cycles including the masses of 9.6 (for background), and those of 10B, 11B, and 30Si (reference mass), with measurement times of 4, 8, 4, and 4 s, respectively (waiting time 1 s). The beam centering, and the mass and energy calibrations were checked before each measurement, after a 2 min presputtering. NBS 614, NBS 617, and UTR2 glasses were used to determine the relative sensitivity factor of B/Si. The B/Si ratio for each spot was derived from the measured 11B/30Si ratio.

Theoretical calculations were performed within the density functional theory framework, using the approach and parameters of Balan et al. (2011, 2014). The ionic core of B was described by the norm-conserving pseudo-potential previously used in Ferlat et al. (2006).

Results and discussion

We discovered in a forsterite batch (run no. 6) synthesized by Lemaire et al. (2004) a heterogeneous single crystal displaying the whole range of OH bands observed among crystals from the same synthesis experiment (spectra 6a to 6e in Fig. 2 of Lemaire et al. 2004). Ion probe analyses show a strong B enrichment at the edge compared with the core of the crystal (160–230 vs. 2–4 wt. ppm, respectively). The presence of B is very probably linked to diffusion from the glass sleeve used in the high-pressure assembly. Significant differences are observed between the edge and core IR spectrum at room temperature (Fig. 1). The edge spectrum displays an additional strong OH band at 3598 cm−1 and weaker bands at 3525 and 3704 cm−1. The broad band at 3216 cm−1 is also enhanced (Fig. 1a1), but its direct relationship with the presence of B is doubtful. The three bands at lower wavenumbers correspond to those observed at 3598, 3527, and 3220 cm−1 by Lemaire et al. (2004) with respective maximum intensities along y, x, and z axes. These OH bands have different thermal behaviors, leading to different shifts and narrowing at −194 °C (Fig. 1b1; Table 1). As previously reported, the strongest changes are observed for the 3598 cm−1 band (Ingrin et al. 2013). Similar OH bands have been observed in samples annealed in high-pressure assemblies surrounded by BN sleeves (Bollinger et al. 2014). Between 1050 and 1500 cm−1, the edge spectrum displays four bands at 1301, 1256, 1207, 1167 cm−1, and possibly two additional bands at 1156, 1132 cm−1 (Fig. 1a2, 1b2), which are not related to pure forsterite. The four intense bands are also observed in the samples studied by Lemaire et al. (2004); they are polarized along x (1301, 1256) and z (1207, 1167) (Fig. 2a). They occur in a frequency range where asymmetric ν3 vibration modes of BO3 groups are generally active (Weir and Schroeder 1964), which suggests the occurrence of BO3 groups subparallel to the (x,z) plane. Considering the previously reported replacement of SiO4 tetrahedra by BO3 groups in synthetic anhydrous diopside and forsterite (Halenius et al. 2010a, 2010b), it is likely that BO3 groups also occur in forsterite (the ν3 bands in diopside are shifted to higher frequencies (>1300 cm−1) due to the occurrence of B-O-Si linkages in the tetrahedral chains). The bands at 1167 and 1256 cm−1 in the forsterite spectra are similar to those at 1164 and 1257 cm−1 in the B-rich olivine from the Tayozhnoye deposit (Sykes et al. 1994). The bands at 1207 and 1301 cm−1 likely correspond to the isotopic shift of the bands at 1167 and 1256 cm−1, respectively, due to 10B (20.9 ± 0.1% from ion probe measurements). The ratios of the bands area support this interpretation (A1301/A1256 = 22 ± 3%; A1207/A1168 = 26 ± 10%). An estimate of the H content coupled to the B substitution at the crystal edge using the calibration coefficients of Kovács et al. (2010) (i.e., k = 0.57; [Si]) or Bell et al. (2003) gives ~150 ± 60 or 50 ± 20 wt. ppm H2O, respectively; which requires the presence of either 180 ± 70 or 60 ± 25 wt. ppm B. Thus, the analysis of 160–250 wt. ppm of B at the crystal edge is consistent with a nearly stoichiometric coupled substitution of B and H.

To confirm the above interpretation, theoretical defect models were obtained by replacing a Si by a B atom and by setting one H atom on the O2 atom (Pbnm space group). Two stable defect configurations were obtained after energy minimization (Fig. 3; Table 2; CIF file in Electronic Annexes1). In the most stable B_H_1 configuration, the BO3 group lies on the (O3-O1-O3) face of the tetrahedral site, inclined at 17° from the (x,y) plane in a similar way to CO3 in the (F, CO3) defect in apatite (Yi et al. 2013). The O2H group points out of the tetrahedral site. As expected from the theoretical approximation level, the theoretical B-O frequencies are underestimated by ~4% (e.g., Patton et al. 1997). However, the polarization and the splitting of the ν3 B-O stretching modes and the corresponding isotopic shifts compare well with experiment (Table 2). The O2H stretching occurs at 3626 cm−1 and is dominantly polarized along y. It corresponds to the band measured at 3598 cm−1 (Fig. 3). The O2H geometry is similar to that of the O2H group in the (4H)Si defect model (Balan et al. 2011), explaining why its stretching frequency almost coincides with one from the (4H)Si defect at low temperature. Although not fully understood, the stronger temperature dependence of the B-related band probably stems from anharmonic coupling to a low-frequency vibration mode (Balan et al. 2014). This further confirms the importance of the local geometry of the defect in the control of anharmonic vibrational properties (Martin et al. 2006). The B_H_2 configuration is less stable by 26.5 kJ/mol, leading to a theoretical B_H_2/B_H_1 abundance ratio of ~12.7%. The O2-H group points to the O1 oxygen. It is dominantly polarized along x with stretching frequency of 3515 cm−1 (Fig. 3) and could correspond to the weaker band at 3525 cm−1.

In the Pakistan olivine samples (Fig. 2b), the ν3 B-O bands are observed at 1167 (z) and 1254 cm−1 (x) (1205 and 1299 cm−1 for 10B) at room temperature. The OH contribution to the spectrum is complex and nine bands can be identified (Figs. 2c and 2d), among which three have frequencies, polarization, and temperature-induced shifts close to those ascribed to the mixed B and H defects in forsterite (Table 1). This confirms the original suspicions of Gose et al. (2010) and Mosenfelder et al. (2011) that this sample displays some OH bands associated with B-H substitution. These three bands at 3699, 3598, and 3521 cm−1 represent about 40% of the total OH band area in the Pakistan olivine spectra. They are superposed on the three bands ascribed to the (4H)Si defect (3613, 3579, and 3566.5 cm−1; representing less than 10% of the OH band area), and to a broad band ascribed to interstitial OH groups (3549 cm−1 at room temperature; 3568 cm−1 at −194 °C) (Ingrin et al. 2013; Balan et al. 2014). Considering that the integral absorbance weakly depends on temperature, the broader contribution at 3579.5 cm−1 (FWHM ~30 to 40 cm−1) at room temperature may correspond to the two bands at 3608.5 and 3592 cm−1 at −194 °C. There is no indication that these bands are linked to the presence of B. The significant proportion of B-associated OH bands in the Pakistan olivine brings into question the IR absorbance calibration for [Si] substitution proposed by Kovács et al. (2010). Their [Si] calibration factor (k = 0.57) more likely represents that of OH bands linked to B substitution. The “sensu strict” [Si] calibration factor may be closer to that of Bell et al. (2003) calibration or even lower (Withers et al. 2012).

Our results provide strong evidence for the coupled substitution of H and BO3 for silica tetrahedra in synthetic forsterite and a natural olivine. The related defects can be quantitatively determined by three OH bands at ~3700, 3600, and 3520 cm−1 with specific polarizations. Note that a band not linked to B and mainly polarized along x, instead of y, is sometimes observed at ~3600 cm−1 in olivine (e.g, Withers et al. 2011). Although not fully understood, the pleochroic band at 3700 cm−1 is systematically observed in B-rich samples. As TEM studies ruled out the presence of serpentine or amphibole inclusions (which also lead to different spectral features; Miller et al. 1987; Matsyuk and Langer 2004), this band is likely related to B substitution and could be a fingerprint of OH and B association. Further confirmation of the presence of B can be gained from the ν3 BO3 vibrations at 1150–1350 cm−1. We provide evidence for the isotopic splitting of the infrared ν3 vibration bands of BO3 groups, which has previously received insufficient attention in the study of B-rich/doped minerals. The present results confirm the usefulness of a detailed FTIR analysis to identify the complexity of H-defects in nominally anhydrous minerals and represent a significant step toward a complete identification of H-defects in mantle olivine and the understanding of their specific effects on the properties of peridotites. This Letter also highlights the importance of chemically composite defects at tetrahedral sites in the incorporation of volatile elements (H, B, F) in minerals (Crépisson et al. 2014). It confirms that the incorporation of planar molecular groups on the triangular face of tetrahedral sites is more common than originally thought (e.g., Halenius et al. 2010b; Yi et al. 2013).

Acknowledgments

This work was supported by the ANR grant ( NT09-566853) provided to J. Ingrin and by the Bolyai Postdoctoral Fellowship Program and a postdoctoral grant ( PD101683) of the Hungarian Scientific Research Found provided to I. Kovács. The PULI spectral database (puli.mfgi.hu) provided digital spectra. We thank Ian Swainson, Fabio Bellatreccia, and Henrik Skogby for their helpful suggestions to improve the manuscript.

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1
Deposit item AM-14-1017, CIF. Deposit items are stored on the MSA web site and available via the American Mineralogist Table of Contents. Find the article in the table of contents at GSW (ammin.geoscienceworld.org) or MSA (www.minsocam.org), and then click on the deposit link.

Supplementary data