Open Access

FTIR and Raman spectroscopy characterization of fluorine-bearing titanian clinohumite in antigorite serpentinite and chlorite harzburgite

  • Kenneth T Koga1, 2, 3Email author,
  • Carlos J Garrido4,
  • José A Padrón-Navarta5,
  • Vicente López Sánchez-Vizcaíno6 and
  • María T Gómez-Pugnaire7
Earth, Planets and Space201466:60

https://doi.org/10.1186/1880-5981-66-60

Received: 14 November 2013

Accepted: 26 May 2014

Published: 26 June 2014

Abstract

Titanian clinohumite is an accessory phase found in peridotites, and it can be a key repository of volatile and other trace elements in sub-arc mantle. To characterize spectroscopic variations due to volatile elements in the phase, we have investigated the infrared spectroscopic characteristics of a suite of naturally occurring Ti clinohumite minerals with varying F and Ti concentrations. Samples were ultramafic rocks from Cerro del Almirez, Spain and Cima di Gagnone, Switzerland. The infrared spectra corresponding to OH vibrations showed systematic variation in regard to the abundance of F in Ti clinohumite. In particular, the intensity ratios of infrared absorption spectra at 3,565 and 3,390 cm-1 correlated linearly with the abundance of F independently of the crystal orientation. Raman spectra did not corroborate the Fourier transform infrared (FTIR) results. This intensity ratio provides an alternative analytical criterion for the characterization of Ti clinohumite.

Findings

Introduction

Titanian clinohumite (TiChu) is a member of the humite group minerals that constitute a polysomatic series with olivine (Thompson 1978; Veblen 1991, 1992). The generalized mineral formula of humite group minerals is [n(M2SiO4)M1 - xTi x (OH, F)2 - 2xO2x] where 0 < x < 0.5, M represents divalent cations (mostly Mg with minor Fe, Mn, and Ni), and n is one for norbergite, two for chondrodite, three for humite, and four for clinohumite. Clinohumite is the humite group mineral whose crystal structure is most closely related to olivine because it has the highest proportion of filled tetrahedral sites.

TiChu is a common accessory mineral in hydrous ultrabasic rocks including antigorite serpentinite (Damour 1879; Brugnatelli 1904; De Quervain 1938; Bearth 1967; Möckel 1969; Trommsdorff and Evans 1980), metaperidotite from high-pressure metamorphic terrains (Möckel 1969; Evans and Trommsdorff 1983; López Sánchez-Vizcaíno et al. 2005), and kimberlite xenoliths (McGetchin and Silver 1970; Matsyuk and Langer 2004). Despite its accessory character, TiChu is thought to play an important role in the storage of water (McGetchin and Silver 1970), fluorine (Engi and Lindsley 1980), boron and lithium (Scambelluri et al. 2004), and the high field strength elements Nb and Ta (Scambelluri et al. 2001; Garrido et al. 2005) in upper mantle ultrabasic rocks. Furthermore, natural mantle olivine usually contains TiChu as defects and patches (Kitamura et al. 1987; Wirth et al. 2001; Berry et al. 2005; Mosenfelder et al. 2006a, 2006b), which may be an effective mechanism for incorporating hydrogen into this nominally anhydrous mantle mineral (Wirth et al. 2001; Berry et al. 2005; Mosenfelder et al. 2006b).

The OH/F ratio of TiChu plays a particularly important role in the stabilization of TiChu at high temperature (Engi and Lindsley 1980; Trommsdorff and Evans 1980; Evans and Trommsdorff 1983), and it is crucial for its stabilization at mantle temperatures beyond the antigorite stability field in hydrous ultrabasic systems (Engi and Lindsley 1980; Trommsdorff and Evans 1980). This is possibly due to the effect of the OHF-1 substitution that reduces the repulsion of H-H bonds within the brucite layers of the clinohumite crystal structure (Fujino and Takeuchi 1978; Ribbe 1979). Because of its potential role as a repository phase for H, F, and Ti in ultramafic rocks, characterizations of naturally occurring TiChu can provide greater insight into fluid transport in subduction zones.

TiChu is one of the trace minerals in ultramafic lithologies that is often overlooked because its submicroscopic intergrowth with olivine can easily be missed during electron microprobe analysis and its geochemical significance has only recently been discovered. We present a Fourier transform infrared (FTIR) transmittance of TiChu with variable OH/F ratios from high-pressure hydrous ultramafic rocks. Previous spectroscopic studies of natural clinohumite are scarce (Miller et al. 1987; Matsyuk and Langer 2004; Berry et al. 2005; Hermann et al. 2007) and have not explored the potential effect of the compositional variation in this mineral in detail. We found that the FTIR spectrum of natural clinohumite in the range of the OH absorbance bands (3,800 to 3,200 cm-1) systematically changes with the OH/F ratio. Combined with wavelength-dispersive X-ray spectroscopy (WDS) electron microprobe data, we propose a calibration that quantitatively correlates the absorbance spectrum with the OH/F ratio for this mineral. This calibration gives an alternative assessment of OH-F substitutions in TiChu by FTIR, which is probably most applicable to inclusions in minerals and fine grains in experimental changes.

Sample location and petrography

We analyzed a wide variety of petrographic types of TiChu from the Cerro del Almirez ultramafic body, Spain. López Sánchez-Vizcaíno et al. (2005) provided a detailed account of the petrology of TiChu in this massif. Our samples can be divided into: TiChu associated with antigorite serpentinite (atg-serpentinite), chlorite harzburgite (chl-harzburgite), and enstatite-rich veins within chl-harzburgite. TiChu associated with atg-serpentinite is almost fluorine free and occurs as dispersed grains embedded in a matrix of flaky antigorite (type serp-1; Al96-20), as veins with millimeter- to centimeter-sized agglomerations of TiChu and olivine (type serp-2; Al96-15B), and as rare small grains formed together with chlorite after relic Ti-rich clinopyroxene grains (type serp-3; Al96-20). TiChu associated with chl-harzburgite is exclusively F-OH-TiChu and occurs as single grains in the matrix of chl-harzburgite minerals (type hz-1; Al96-10), as rare patches, intergrowths, and lamellae within olivine (type hz-2), and as individual grains within enstatite-chlorite veins (type hz-3; Al01-7B). We also studied a third textural type occurring in carbonate-rich lenses near the contact with the country rock. These samples display a ‘sunny-side up’ texture characterized by yellow cores of F-rich TiChu sequentially rimmed by light yellow and then clear olivine (type 4; Al98-29A).

In addition, we analyzed three fluorine-bearing TiChu samples from a garnet metaperidotite in an ultramafic lens enclosed in kyanite schist from the Cima di Gagnone (Central Alps, Ticino, Switzerland). These samples have already been described by Evans and Trommsdorff (1983) (all are from locality 304; samples MG-304-B). TiChu grains occur here in brown patches within a matrix of olivine, orthopyroxene, and spherical aggregates of chlorite interpreted as breakdown products from garnet. These TiChu samples expand the compositional range of TiChu investigated here to low OH/F and XTi compositions.

Analytical methods

Electron microprobe analysis

Major elemental compositions of TiChu were measured on the same spots from which FTIR spectra were collected; this was done using a SX-100 CAMECA electron microprobe (EMP) at the Laboratoire Magmas et Volcans (Clermont-Ferrand, France) with a 15-kV accelerating voltage, a 30-nA sample current, and a counting time ranging from 10 to 30 s using thallium acid phthalate (TAP), and pentaerythritol (PET) refraction crystals. Fluorine analyses were performed following the procedure of Moune et al. (2007) but modified to a 40-nA sample current and 30-s acquisition time using three TAP crystals. Fluorine concentrations were determined using CaF2 calibration standards. The estimated precision of F depended on the concentrations and ranged from 2% to 32% relative deviation in repeated analyses. The detection limit was 300 ppm or lower.

FTIR sample preparation and measurements

Micro-FTIR spectroscopy analyses were made on double-sided polished sample slabs prepared on glass slides with Crystalbond™ that were subsequently dissolved off with acetone and then rinsed thoroughly with ethanol. For spectral calibration, we measured the slab thickness with a micrometer, and the value had a precision of ±5 μm.

We collected in situ FTIR spectra using a Bruker™ HYPERION microscope at the Laboratoire Magmas et Volcans, Université Blaise-Pascal (Clermont-Ferrand, France). The FTIR spectra were acquired using the Video Assisted Measure option of the Bruker™ OPUS software (v. 5.0). For each spot, we acquired one spectrum in unpolarized infrared (IR) light and two spectra in polarized IR light taken at orthogonal orientations corresponding to maximum and minimum pleochroism under polarized light. The IR polarizer was gold-coated thallium bromide iodide, and it had 87% polarization efficiency. The IR source was a mid-IR lamp, and a KBr beam splitter was used. Spectra were collected with a × 15 IR objective and a nitrogen-cooled mercury cadmium telluride (MCT) detector, and the values were calculated over the range of 4,000 to 700 cm-1 at 4 cm-1 resolution by averaging 100 scans. The spot sizes were adjusted from 50 × 50 to 30 × 30 μm square areas to measure an optically clear, homogenous part of crystal. Every sample measurement consisted of a background measurement followed by acquisition of spectra from several grains.

Raman spectroscopy

Laser Raman measurements on the same samples were acquired at the Ecole Normale Supérieur (ENS), in Lyon, France using a Jobin-Yvon LabRam HR800 spectrometer equipped with a charge-coupled device (CCD) detector. An argon ion laser from Spectra Physics, which was set at a wavelength of 632.8 nm, was used to excite Raman scattering. Final spectra were obtained by averaging three spectra with an acquisition time of 30 s for shift ranges of 500 to 2,000 cm-1 (aluminosilicate framework domain, TOT) and 3,200 to 3,800 cm-1 (OH stretching domain) relative to the laser light wavelength.

Results

Compositional variations of titanian clinohumite

Table 1 shows the composition of TiChu samples used in this study. An averaged value for each sample is reported although not every crystal in a sample is necessarily homogenous. The degree of heterogeneity was inferred from the standard deviations. For example, because the analytical uncertainty of FeO is approximately ±0.5 wt.%, the standard deviation of a homogeneous sample should give roughly the same value. Thus, larger variations of MgO, FeO, and TiO2 in samples Al96-20 and Al98-29A were due to the compositional heterogeneity. The analytical spots for FTIR, Raman, and the electron microprobe were all at the same coordinates and identified by the sample textures. The correlations of FTIR spectra and TiChu compositions were established from the analyses for each point rather than averaged sample compositions.
Table 1

Titanian clinohumite from Cerro del Almirez, Spain (Al) and Cima di Gagnone, Switzerland (MG)

 

Sample: rock type

Al96-20: Ant serp

Al96-15B: TiCl vein Serp

Al96-10: Px lamella

Al96-1C: Chl harz

Al01-7B: En vein

Al98-29A: Marble

MG-304B: Chl perid

SiO2

35.8

(9)

36.4

(5)

36.8

(1)

36.2

(2)

36.9

(4)

36.8

(4)

36.2

(4)

TiO2

5.4

(1)

5.3

(2)

5.6

(2)

4.9

(1)

4.8

(1)

2.4

(1.1)

1.9

(6)

FeO

7.1

(2)

8.7

(5)

8.1

(6)

8.3

(1)

8.9

(2)

9.1

(8)

8.4

(3)

MnO

0.36

(4)

0.32

(3)

0.39

(3)

0.13

(2)

0.10

(5)

0.10

(3)

0.08

(4)

MgO

47.8

(1.2)

47.3

(5)

47.6

(4)

47.7

(2)

48.1

(3)

49.4

(1.0)

49.8

(4)

NiO

0.14

(3)

0.16

(1)

0.15

(2)

0.25

(1)

0.19

(1)

0.19

(1)

0.14

(2)

F

0.02

(2)c

0.02

(2)c

0.014

(4)d

0.49

(5)

0.62

(4)

1.58

(50)

1.78

(21)

H2Oa

2.71

(26)

2.73

(2)

2.74

(2)

2.50

(2)

2.47

(3)

2.02

(23)

1.91

(10)

Total

99.6

(8)

101.0

(5)

101.5

(3)

100.8

(4)

102.1

(6)

101.6

(3)

100.4

(5)

n

4

16

5

5

4

8

5

Ti

0.45

(19)

0.43

(2)

0.46

(1)

0.41

(1)

0.39

(1)

0.20

(9)

0.16

(5)

Fe

0.66

(7)

0.80

(4)

0.74

(6)

0.76

(1)

0.81

(1)

0.82

(7)

0.76

(3)

Mn

0.03

(2)

0.03

(0)

0.04

(0)

0.01

(0)

0.01

(0)

0.01

(0)

0.01

(0)

Mg

7.87

(64)

7.73

(6)

7.74

(5)

7.80

(1)

7.77

(1)

7.97

(12)

8.10

(5)

Ni

0.01

(2)

0.01

(0)

0.01

(0)

0.02

(0)

0.02

(0)

0.02

(0)

0.01

(0)

F

0.005

(10)

0.006

(10)

0.009

(10)

0.17

(2)

0.21

(1)

0.54

(17)

0.61

(7)

OHb

1.10

(32)

1.12

(3)

1.07

(3)

1.02

(3)

1.01

(2)

1.07

(5)

1.08

(3)

TiCl compositions are an average of several electron probe analyses on a rock sample shown as weight percent, and the number of points used for the average is indicated as ‘n.’ Large standard deviations of the average represent the extent of sample heterogeneity, as indicated by italics. Numbers in parentheses indicate the uncertainty expressed as the last digits of reported values, as in ‘1.07 (5)’ corresponds to 1.07 ± 0.05. aH2O weight percent was calculated from the stoichiometric balance of OH. bOH was calculated from the stoichiometric balance. cThree low F abundance measurements were below the detection limit and the relative standard deviations were more than 100%; hence, these values should be considered as maximum possible values. dThe value verified by a secondary ion mass spectrometer.

Figure 1 shows notable compositional variation due to exchange vectors. The mole fractions of F and Ti in their respective crystallographic sites formed a negative correlation. This has been described elsewhere as being the result of the exchange vectors of OH-F and TiO2-M(OH)2 (Evans and Trommsdorff 1983). Our samples showed a coherent variation that corresponds to these exchange vectors. Consequently, F-rich TiChu is OH and Ti poor, and vice versa.
Figure 1

Plot of X F versus X Ti . It shows TiChu’s F-OH exchange reaction follows a compositional vector TiO2Mg-1 F-2. XF is F/(F + OH) in moles. XTi is the fraction of Ti in the Mg-site.

FTIR spectra

Figure 2 shows a series of unpolarized Ti-clinohumite spectra. Here, we focus on the spectrum wavenumbers between 3,700 and 3,250 cm-1 that correspond to the absorbance bands of hydroxyl groups. Spectra were baseline-corrected and normalized to 1-cm thickness. The shape of the spectra and the relative strength of the bands varied significantly for F-rich and F-poor TiChu (Figure 2). The spectra of all investigated F-poor TiChu are characterized by two weak bands at 3,565 and 3,528 cm-1 of similar strength (typically between 2 to 7 absorbance units), and a stronger, wider band between 3,415 and 3,394 cm-1 with a shoulder at lower wavenumbers. For example, the strong band at 3,390 cm-1 was present in all spectra from the F-rich to F-poor clinohumites. This spectrum is similar to those described elsewhere (Kitamura et al. 1987; Miller et al. 1987; Kurosawa et al. 1997; Berry et al. 2005; Matsyuk and Langer 2004). We did not observe the broad 3,840 cm-1 band reportedly present in a high F clinohumite (Satish-Kumar and Niimi 1998).
Figure 2

FTIR spectra showing the characteristic TiChu OH bands. Fluorine concentration increases towards the lower spectra. As F increases, the relative heights of 3,565 and 3,528 change, as well as the height of the large peaks around 3,400 to 3,390. From these observations, at a first order, F-rich and F-poor TiChu are easily identified by their FTIR spectra in OH regions. For clarity, the spectra are ordinate-shifted.

The shape of the spectra was largely orientation independent (Figure 3). The similarity of the shape implies constant relative peak heights, although there may be significant changes in absorption. However, closer inspection of the relative heights of the stronger bands at 3,415 and 3,394 cm-1 showed that they were dependent on crystal orientation as there were more prominent shoulders in stronger spectra. On the contrary, the wavenumbers for the weaker bands at 3,565 and 3,528 cm-1 remained constant, but their relative height varied slightly with orientation.
Figure 3

Two polarized and one unpolarized spectra of TiChu. General similarities of the spectra are noticeable, although subtle variations of relative peak heights are also present, which indicates that some infrared (IR) absorbers are not parallel.

The spectrum of F-rich TiChu was characterized by the 3,565 cm-1 band being more intense than the 3,528 cm-1 band. The 3,528 cm-1 band was weaker than that of the 3,565 cm-1 band for F-poor specimens, and the exact peak position was obscured by the larger 3,565 cm-1 band (Figure 2, sample MG304B). In this case, deconvolution of the spectra from 3,570 to 3,520 cm-1 identified the presence of the 3,528 cm-1 band. These results indicate that the shape of TiChu spectra depends on its composition, and the intensity ratio of the 3,565 to 3,528 cm-1 peaks appears to be sensitive to the F/OH ratio (Figure 2).

Laser micro-Raman spectroscopy

Figure 4 shows the laser micro-Raman spectra for TiChu with variable F content. The spectra were similar for all samples and displayed Raman bands characteristic of TiChu in the aluminosilicate framework domain (500 to 1,100 cm-1, Figure 4a; Frost et al. 2007). However, we did not detect many of the reported weak bands, which was probably a result of the weak excitation laser used in this study. In particular, our Raman observation in the OH band region differed significantly from that of Frost et al. (2007), who described several peaks of Raman shift in the region of 3,527 to 3,578 cm-1, whereas we detected a weak band at 3,565 cm-1. The IR absorption peaks corresponded to all the reported OH Raman bands. We did not detect a clear variation in the locations of low-frequency Raman bands among clinohumites with variable OH/F ratios (Figure 4a). All clinohumites showed a band at 3,412 to 3,398 cm-1 with variable strength in the OH stretching domain (3,200 to 3,750 cm-1, Figure 4b). The strength of the band is probably related to the OH/F ratio and orientation of the sample. The peak was well developed in the F-poor samples; F-rich samples lost their 3,200 to 3,750 cm-1 Raman signal, which is consistent with the lower OH abundance.
Figure 4

Raman spectra of TiChu with varying F content. Here, (a) low- and (b) high-frequency regions of TiChu Raman signals show identical peak positions (at 536, 602, 755, 780, 828, 845, 861, and 963). Variations of their shapes and relative heights are due to crystal orientations. While Raman spectra are useful to identify microinclusions and intergrowth of TiChu, they do not provide obvious indications of compositional variations. The order of spectra is the same for both figures.

Discussion

Orientation-independent spectral shapes

For crystalline material (except for that with cubic symmetry), polarized spectra normally vary in intensity depending on the orientation of the crystal with respect to the photon vibration vector. This type of behavior is also expected for TiChu, which is orthorhombic. However, the polarized IR spectra of orthogonal orientations, which were collected on randomly oriented Ti-clinohumite crystals, showed a general similarity in shape. Specifically, it should be noted that relative heights of some peaks were constant while absolute intensities of spectra varied significantly from one to the other. Polarized and unpolarized spectra also showed similar shapes (Figure 3). However, there were minor deviations from this generalization; for example, there were significant variations in shoulder peak intensities at 3,415 and 3,400 cm-1 depending on the crystal orientation.

We examined the similarity of the spectra shapes by plotting the ratios of peak intensities at 3,565, 3,528, and 3,390 cm-1. If the spectra obtained for two orthogonal orientations are symmetric, then the plot of the intensity ratios for one orientation against the other should result in a perfect correlation. Figure 5 shows the intensity ratios of (a) the 3,565 and 3,390 cm-1 bands and (b) the 3,565 and 3,628 cm-1 bands. The good correlation (Figure 5a) demonstrates that the intensities of the 3,565 and 3,390 cm-1 bands vary proportionally with respect to the orientation. The correlation improved for an unpolarized spectra against one of the polarized orientations, which was probably due to the averaging effect by the unpolarized photon vector.
Figure 5

Intensity ratios. (a) Plot of the peak height ratios for 3,565 and 3,390 for unpolarized and orthogonally oriented polarized spectra. Dashed line shows a 1:1 slope. Correlation coefficients are 0.85 and 0.95 for polarized-polarized and unpolarized-polarized datasets, respectively. (b) Plot of the peak height ratios for 3,565 and 3,528 unpolarized and orthogonally oriented polarized spectra. No significant correlations were found.

Infrared light absorption in the range of 3,200 to 3,700 normally represents the interaction of photons with OH stretching vibrations. Therefore, the variation in IR absorption depends on the angle between the photon vibration vector and the stretching vibration vector. If the orientations of the crystallographically distinct OH bonds corresponding to the 3,565 and 3,390 cm-1 bands are parallel in the TiChu crystal, there should be a perfect correlation between the intensity ratios. However, Figure 5a shows moderate scatter around a general correlation, which suggests that these OH bond orientations deviate from the parallel. This deviation from the parallel was not significant enough to invalidate the correlation of Figure 5a. It should also be noted that the correlations of peak intensity ratios for other vibration bands were weak or nonexistent (Figure 5b).

Correlation of IR spectra and chemical composition

Because each IR absorption band shown here represents an OH bond in a certain crystallographic site, inherent relationships can be expected between the shape of the IR spectra and the chemical composition, especially in the case of OH-F exchange in TiChu. A detailed study of oriented clinohumites should enable the exact nature of OH-F substitutions to be identified, as well as the site preferences for these elements. The linear relationship between the intensity ratio of 3,565/3,390 and F abundance (Figure 6) implies a near parallel OH bond orientation. Furthermore, because the intensity ratio of 3,565/3,390 was more or less independent of the orientation, the ratio can be used to quantitatively calibrate the correlation between the shape of the IR spectrum and the F abundance.
Figure 6

Plot of the F wt.% versus 3,565/3,390 intensity ratio showing a strong correlation between peak height ratios (i.e., the spectra shape) and F concentration. The linear regression resulted in F (wt.%) = -0.36 + 2.3 R3,565/3,390 where r2 = 0.938. Small dots are the polarized spectra data, and large symbols are the unpolarized data with symbols corresponding to the key in Figure 1.

The spectroscopy results show that the shape and strength of the FTIR spectrum of TiChu is sensitive to the XF value (XF = F/(F + OH) in atoms per formula unit). A robust correlation was present between F wt.% and the unpolarized intensity ratio of 3,565/3,390 bands (R3,565/3,390; Figure 6). Using this correlation, it is possible to estimate the approximate composition of clinohumite from FTIR spectra. The weighted regression in Figure 6 gives the following formula:
F wt . % = - 0.36 + 2.3 R 3 , 565 / 3 , 390 , where r 2 = 0.938 .

The uncertainties of the regression are not reported here because the intention of this study was to demonstrate the presence of a composition-spectra correlation. This formula is useful in estimating F content upon detection of clinohumite by spectroscopic methods. It is clear that a calibration based on Raman spectra would be more versatile in natural sample applications.

Application of the correlation to complex natural situations

Fluorine abundance in solid materials can often be measured using an electron microprobe, as in the case of the large TiChu crystals in this study, but accurate F measurements by an electron microprobe are not routine and require some developments (Ottolini et al. 2000). Estimation of the chemical composition from IR spectra is probably a useful alternative for cases such as complex intergrowths of TiChu with olivine. Clinohumite crystals in olivine can occur as lamellae at scales ranging from several hundred nanometers to several tens of micrometers (Wirth et al. 2001; Mosenfelder et al. 2006b; Berry et al. 2007). Because a higher F abundance stabilizes TiChu at higher temperatures (Evans and Trommsdorff 1983), the identification of such lamellae in olivines can provide new information about the volatile element sink that is transported deep into the mantle.

Published FTIR spectra of F-rich TiChu from Dabie Shan, China (Hermann et al. 2007) and those obtained here for F-rich TiChu from Cima di Gagnone (Figure 2) are similar. Accordingly, FTIR spectra may allow us to infer that relatively F-poor TiChu from the Almirez chl-harzburgite formed at lower temperatures than F-rich ones from Dabie Shan or Cima di Gagnone. This grossly simplified conclusion can be made despite ignoring initial F abundances and activity in the respective protoliths, and it is supported by independent P-T estimations made in each of these localities.

Among recent reports on the hydrogen incorporation mechanisms in olivine, the presence of clinohumite-type OH defects has been proposed as one of the critical natural incorporation mechanisms (Miller et al. 1987; Berry et al. 2005; Mosenfelder et al. 2006b; Berry et al. 2007; Walker et al. 2007). Our IR characterization should not be applied to the investigation of olivine point defect structures because the reported IR spectra in olivine are suggestive of dissimilarities between TiChu structures and TiChu-like defects. For instance, forsterites synthesized under an MgO and TiO2 buffer (Berry et al. 2005) show stronger IR absorption peaks at 3,572 and 3,525 than around 3,415 to 3,390, whereas our results consistently showed stronger peaks around the 3,415 to 3,390 region than either of the peaks at 3,572 or 3,525. In Berry et al. (2005), the 3,572 and 3,525 peaks are attributed to TiChu-like OH-incorporating defects. We note that the TiChu OH stretching peaks are at 3,565 and 3,528, offsets of -7 and +3 cm-1 from that of the OH defect in olivine. Looking at the spectra qualitatively (Figure 1 in Berry et al. 2005), the defect peaks are similar to the clinohumite peaks, but these offsets are significantly beyond the uncertainty of the instrument. These disparities point to the fact that the casually termed ‘titanian clinohumite-like defect’ is structurally dissimilar to TiChu minerals apart from the fact that both have Ti in the sixfold coordinate site. Mosenfelder et al. (2006b) presents a similar conclusion based on the inconsistency of peak intensities found in experimental and natural olivine crystals with TiChu-like defects.

Declarations

Acknowledgements

This project was funded by the BQR grant from the Université Blaise Pascal Clermont Ferrand II and the Spanish Ministry of Science (MEC) grant CGL2009-12158 and CGL2012-32067. This work was carried out during the visiting professorship of CJG to the Laboratoire Magmas et Volcans, which was funded by OPGC - Université Blaise Pascal. This work was also supported by ANR SlabFlux, ANR09BLAN0338. This is Laboratory of Excellence ClerV olc contribution no. 100. JPAN is supported by HISLa-DR, Marie Curie Action under grant agreement PIOF-GA-2010-273017 from the European Union Seventh Framework Programme (FP7/2007-2013).

Authors’ Affiliations

(1)
Laboratoire Magmas et Volcans, Clermont Université, Université Blaise Pascal
(2)
Laboratoire Magmas et Volcans, CNRS UMR 6524
(3)
Laboratoire Magmas et Volcans, IRD M163
(4)
Instituto Andaluz de Ciencias de la Tierra (IACT), CSIC-UGR
(5)
Géosciences Montpellier, Université Montpellier 2 & CNRS
(6)
Department Geología, Universidad de Jaén, Escuela Politécnica Superior
(7)
Department Mineralogia y Petrología, Facultad de Ciencias, Universidad de Granada

References

  1. Bearth P: Die Ophiolithe der Zone von Zermatt-Saas Fee. Beitraege zur Geologischen Karte der Schweiz NF 132. Kümmerly & Frey, Bern; 1967.Google Scholar
  2. Berry A, Hermann J, O’Neill HSC, Foran GJ: Fingerprinting the water site in mantle olivine. Geology 2005, 33: 869–872. 10.1130/G21759.1View ArticleGoogle Scholar
  3. Berry AJ, O’Neill HSC, Hermann J, Scott D: The infrared signature of water associated with trivalent cations in olivine. Earth Planet Sci Lett 2007, 261: 134–142. 10.1016/j.epsl.2007.06.021View ArticleGoogle Scholar
  4. Brugnatelli L: Über den titanolivin der umgebung van chiesa in Val Malenco; ein beitrag zur kenntnis des titanolivin. Z Kristallogr Mineral 1904, 39: 209–219.Google Scholar
  5. Damour M: Note sur le peridot titanifère de Zermatt en Valais. Bulletin de la Societe Francaise de Mineralogie et de Cristallographie 1879, 2: 15.Google Scholar
  6. De Quervain T: Zur kenntnis des titanklinohumites (titanolivine). Schweiz Mineral Petrogr Mitt 1938, 18: 591–604.Google Scholar
  7. Engi M, Lindsley DH: Stability of titanian clinohumite: experiments and thermodynamic analysis. Contrib Mineral Petrol 1980, 72: 415–424. 10.1007/BF00371348View ArticleGoogle Scholar
  8. Evans BW, Trommsdorff V: Fluorine hydroxyl titanian clinohumite in Alpine recrystallized garnet peridotite: compositional controls and petrologic significance. Am J Sci 1983, 283A: 355–369.Google Scholar
  9. Frost RL, Palmer SJ, Bouzaid JM, Reddy BJ: A Raman spectroscopic study of humite minerals. J Raman Spectros 2007, 38: 68–77. 10.1002/jrs.1601View ArticleGoogle Scholar
  10. Fujino K, Takeuchi Y: Crystal chemistry of titanian chondrodite and titanian clinohumite of high-pressure origin. Am Mineral 1978, 63: 535–543.Google Scholar
  11. Garrido CJ, López Sánchez-Vizcaíno V, Gómez-Pugnaire MT, Trommsdorff V, Alard O, Bodinier J-L, Godard M: Enrichment of HFSE in chlorite-harzburgite produced by high-pressure dehydration of antigorite-serpentinite: implications for subduction magmatism. Geochem Geophys Geosyst 2005., 6: doi:10.1029/2004GC000791Google Scholar
  12. Hermann J, Fitz Gerald J, Malaspina N, Berry A, Scambelluri M: OH-bearing planar defects in olivine produced by the breakdown of Ti-rich humite minerals from Dabie Shan (China). Contrib Mineral Petrol 2007, 153: 417–428. 10.1007/s00410-006-0155-7View ArticleGoogle Scholar
  13. Kitamura M, Kondoh S, Morimoto N, Miller GH, Rossman GR, Putnis A: Planar OH-bearing effects in mantle olivine. Nature 1987, 328: 143–145. 10.1038/328143a0View ArticleGoogle Scholar
  14. Kurosawa M, Yurimoto H, Sueno S: Patterns in the hydrogen and trace element compositions of mantle olivines. Phys Chem Miner 1997, 24: 385–395. 10.1007/s002690050052View ArticleGoogle Scholar
  15. López Sánchez-Vizcaíno V, Trommsdorff V, Gómez-Pugnaire M, Garrido C, Müntener O, Connolly J: Petrology of titanian clinohumite and olivine at the high-pressure breakdown of antigorite serpentinite to chlorite harzburgite (Almirez Massif, S. Spain). Contrib Mineral Petrol 2005, 149: 627–646. 10.1007/s00410-005-0678-3View ArticleGoogle Scholar
  16. Matsyuk SS, Langer K: Hydroxyl in olivines from mantle xenoliths in kimberlites of the Siberian platform. Contrib Mineral Petrol 2004, 147: 413–437. 10.1007/s00410-003-0541-3View ArticleGoogle Scholar
  17. McGetchin TR, Silver LT: Compositional relations in minerals from kimberlite and related rocks in the Moses Rock dike, San Juan County, Utah. Am Mineral 1970, 55: 1738–1771.Google Scholar
  18. Miller GH, Rossman GR, Harlow GE: The natural occurrence of hydroxide in olivine. Phys Chem Miner 1987, 14: 461–472. 10.1007/BF00628824View ArticleGoogle Scholar
  19. Möckel JR: Structural petrology of the garnet peridotite of Alpe Arami (Ticino), Switzerland. Leides Geologische Mededdelingen 1969, 42: 61–130.Google Scholar
  20. Mosenfelder JL, Deligne NI, Asimow PD, Rossman GR: Hydrogen incorporation in olivine from 2–12 GPa. Am Mineral 2006, 91: 285–294. 10.2138/am.2006.1943View ArticleGoogle Scholar
  21. Mosenfelder JL, Sharp TG, Asimow PD, Rossman GR: Hydrogen incorporation in natural mantle olivines. In Earth’s deep water cycle. Edited by: Jacobsen SD, van der Lee S. Washington, D.C.: American Geophysical Union; 2006:45–56.View ArticleGoogle Scholar
  22. Moune S, Sigmarsson O, Thordarson T, Gauthier PJ: Recent volatile evolution in the magmatic system of Hekla volcano, Iceland. Earth Planet Sci Lett 2007, 255: 373–389. 10.1016/j.epsl.2006.12.024View ArticleGoogle Scholar
  23. Ottolini L, Cámara F, Bigi S: An investigation of matrix effects in the analysis of fluorine in humite-group minerals by EMPA, SIMS, and SREF. Am Mineral 2000, 85: 89–102.View ArticleGoogle Scholar
  24. Ribbe PH: Titanium, fluorine, and hydroxyl in the humite minerals. Am Mineral 1979, 64: 1027–1035.Google Scholar
  25. Satish-Kumar M, Niimi N: Fluorine-rich clinohumite from Ambasamudram marbles, southern India: mineralogical and preliminary FTIR spectroscopic characterization. Mineral Mag 1998, 62(4):509–519. 10.1180/002646198547882View ArticleGoogle Scholar
  26. Scambelluri M, Rampone E, Piccardo GB: Fluid and element cycling in subducted serpentinite: a trace-element study of the Erro-Tobbio high-pressure ultramafites (Western Alps, NW Italy). J Petrol 2001, 42: 55–67. 10.1093/petrology/42.1.55View ArticleGoogle Scholar
  27. Scambelluri M, Muntener O, Ottolini L, Pettke TT, Vannucci R: The fate of B, Cl and Li in the subducted oceanic mantle and in the antigorite breakdown fluids. Earth Planet Sci Lett 2004, 222(1):217–234. 10.1016/j.epsl.2004.02.012View ArticleGoogle Scholar
  28. Thompson JB: Biopyriboles and polysomatic series. Am Mineral 1978, 63: 239–249.Google Scholar
  29. Trommsdorff V, Evans BW: Titanian hydroxyl-clinohumite formation and breakdown in antigorite rocks (Malenco, Italy). Contrib Mineral Petrol 1980, 72: 229–242. 10.1007/BF00376142View ArticleGoogle Scholar
  30. Veblen DR: Polysomatism and polysomatic series. Am Mineral 1991, 76: 801–826.Google Scholar
  31. Veblen DR: Electron microscopy applied to nonstoichiometry, polysomatism, and replacement reactions in minerals. Mineralogical Society of America. In Minerals and reactions at the atomic scale: transmission electron microscopy. Volume 27. Edited by: Buseck PR. D.C.: Washington; 1992:181–230.Google Scholar
  32. Walker AM, Hermann J, Berry AJ, O’Neill HSC: Three water sites in upper mantle olivine and the role of titanium in the water weakening mechanism. J Geophys Res 2007, 112: B05211.Google Scholar
  33. Wirth R, Dobrzhinetskaya LF, Green HW II: Electron microscope study of the reaction olivine + H2O + TiO2 — > titanian clinohumite + titanian chondrodite synthesized at 8 GPa, 1300K. Am Mineral 2001, 86: 601–610.View ArticleGoogle Scholar

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