| Citation: | Yi-Ning Wu, Yong-Feng Wang. An FTIR Study of Kyanite in the Maobei Kyanite-Bearing Eclogites from the Sulu Orogenic Belt, Eastern China. Journal of Earth Science, 2018, 29(1): 21-29. doi: 10.1007/s12583-017-0774-0
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Kyanite is the high-pressure phase of the Al2SiO5 polymorphs. Though generally being accessory, kyanite represents an important component mineral in many high-and ultrahigh-pressure (UHP) metamorphic rocks, such as eclogites, gneisses, granulites, and schists (e.g., Kotková and Janák, 2015; Klonowska et al., 2014; Beane and Field, 2007; Hollis et al., 2006; Terry et al., 2000). In particular, kyanite has also experienced UHP metamorphism accompanying its host rocks from continental subduction zones as indicated by the discovery of coesite inclusions inside kyanite and the geobarometric constraints on many kyanite eclogites worldwide (e.g., Kotková and Janák, 2015; Hu et al., 2001; Terry et al., 2000). Thus kyanite could potentially provide some insight into the physical state of its host rocks from subduction zones.
Knowledge of water concentration in kyanite might be important. First, kyanite may be a possible carrier to transport some water in subducted crust and, after potential transformation to AlSiO3OH during deep subduction, may transport some water into the deep earth (Schmidt et al., 1998; Bell and Rossman, 1992), which in turn may well influence the geodynamics of the deep earth. Second, the nominally anhydrous minerals (NAMs) may possibly release some amount of water because of decreasing solubility of structural hydroxyl with dropping pressure during exhumation, which had been suggested to facilitate the retrogression of eclogites (e.g., Chen et al., 2007; Zheng et al., 2003). Third, water in the constituent minerals from eclogites is of significance because it may strongly affect the rheological properties of eclogites (e.g., Zhang and Green, 2007). These arguments point to the importance of kyanite pertinent to the geodynamical processes in subduction zones.
Many studies have demonstrated that kyanite, one of the NAMs, from different occurrences usually displays remarkable OH absorption peaks indicative of defect-related water in their infrared spectrum (Bell et al., 2004; Beran et al., 1993; Bell and Rossman, 1992; Rossman and Smyth, 1990; Beran and Götzinger, 1987; Wilkins and Sabine, 1973). However, most of these previous studies used the calibration of Beran and Götzinger (1987) to calculate the water concentration in kyanite, which had been argued to greatly overestimate the water concentration in kyanite (Bell et al., 2004). Besides, the homogeneity of water within a kyanite has not yet been examined. Therefore, more work on water concentration and distribution in kyanite is required to place closer constraints on water storage and transport in subduction zones.
To constrain the exact water concentration that can be stored and transported by eclogites, we have collected fresh kyanite-bearing eclogites from Maobei in the Sulu orogenic belt, eastern China to investigate in detail the water concentration of kyanite. We aim to expand the current dataset on the water concentration in kyanite from eclogites and understand the water distribution in kyanite. For comparison, we also gave the results of water contents in coexisting garnet and omphacite from the Maobei eclogites.
The Sulu orogenic belt is the eastern extension of the Dabie-Sulu orogenic belt, displaced about 530 km to the northeast from the Dabie orogenic belt by the sinistral Tanlu fault (Fig. 1). It was formed by the Triassic collision between the Yangtze Craton and the North China Craton and bounded by the Yantai-Qingdao-Wulian fault in the north and the Jiashan-Xiangshui fault in the south. The Sulu orogenic belt consists of ultrahigh-pressure (UHP) and high-pressure (HP) belts, which are unconformably overlain by the Jurassic clastic strata and the Cretaceous volcanoclastic cover, and intruded by the post-orogenic Mesozoic granitic plutons (Zhang et al., 1995). The UHP belt is composed mainly of UHP gneisses overprinted by amphibolite facies conditions, in addition to minor eclogites, garnet peridotites, quartzites, and marbles. Coesite-bearing eclogites are widely found in gneisses, peridotites, and marbles. Coesite and quartz pseudomorph after coesite are present as inclusions in garnet, omphacite, kyanite, and epidote, or as an intergranular phase in eclogite (e.g., Zhang et al., 2009; Liou and Zhang, 1996). The P-T conditions of UHP metamorphism are 2.9–4.3 GPa and 680–880 ℃ for the Sulu UHP belt (see Zhang et al., 2009). Geochronological studies by analyses of zircon hosted by various gneisses and associated eclogites show that these rocks have protolith ages of 910–574 Ma and UHP metamorphic ages of 240–220 Ma (Liu et al., 2004).
The Maobei complex forms a large lens with a reverse 'S' shape as revealed by geological mapping and drilling (Fig. 1). This complex forms a layered body dipping steeply at angles of 60°–70° in the subsurface (Zhang et al., 2006). The Chinese Continental Scientific Drilling (CCSD) main hole with a final depth of 5 158 m has penetrated into the Maobei complex from its eastern margin (Fig. 1). Geochemical and geochronological studies suggest that the protolith of this complex is a Neoproterozoic layered intrusion consisting of a base of olivine-gabbro, a main body of gabbro, and minor granodiorite (Zhang et al., 2006). This complex is mainly composed of lenses of eclogites and garnet peridotites and hosted by granitic gneisses. Dozens of stone-pits aiming to collect quartz crystals are scattered around the CCSD main hole. Foliated eclogites with various amounts of kyanite, rutile, phengite, and/or quartz are well exposed in these stone-pits. For this study, we collected four fresh kyanite-bearing eclogites from the Maobei complex (Fig. 1).
At hand specimen scale, the eclogite samples under study show remarkable foliation and lineation manifested by the oriented alignment of elongate garnet, omphacite, and kyanite grains (Fig. 2). Kyanite-rich and kyanite-quartz-rich layers, which are concordant with the lineation, are observed in some eclogites. For microstructural observations and fabric analyses, we prepared thin sections normal to the foliation plane and parallel to the lineation (i.e., the XZ section), with a final polishing of 0.05 μm using colloidal alumina.
Under a petrographic microscope, all the eclogite samples are medium-to coarse-grained with garnet and omphacite constituting > 75%–85% of the total volume. Minor mineral components including kyanite, quartz, rutile, zoisite, and/or phengite vary in mode from sample to sample. Garnet occurs as large anhedral, elongate grains in the matrix (Fig. 3a) or as small inclusions in omphacite and kyanite. The matrix garnet grains sometimes elongate up to ~8 mm in length and their oriented alignment defines the lineation in eclogites. Some garnet grains contain many minute mineral inclusions (including omphacite, rutile, quartz, and/or kyanite), showing a typical poikiloblastic texture.
Omphacite also occurs either as a matrix phase (~0.3–1.7 mm in size) or as inclusions within garnet and/or kyanite. Retrogression of omphacite is rare and generally absent at the contacts with matrix kyanite (Fig. 3b). However, intensive symplectization of omphacite often occurs adjacent to and along the kyanite-quartz-rich veins (Fig. 3c). Coesite inclusions with radial fractures are sometimes observed inside garnet and omphacite, suggesting that these rocks have experienced UHP metamorphism.
Kyanite (~0.1–0.7 mm) occurs as euhedral, elongate crystals either scattering in the matrix (Figs. 3a and 3b) or concentrating in the kyanite-rich and/or kyanite-quartz-rich veins (Figs. 3c and 3d). In the kyanite-quartz-rich veins, zoisite is often observed coexisting with kyanite and quartz (Fig. 3c).
For analyses of structurally bound water in kyanite, garnet, and omphacite, doubly-polished sections with a thickness of 190–210 μm were prepared for FTIR measurements. A Nicolet 6700 spectrometer coupled with a Continuμm IR microscope at the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences (GPMR-CUG), Wuhan, was used for unpolarized micro-FTIR transmission spectral analyses of the polished sections. Before measurements were made, the polished sections were dried in a vacuum oven at 120 ℃ for more than 24 h. Infrared spectra were obtained in situ at room temperature and pressure over a wavenumber range of 2 500–4 500 cm-1 using a KBr beam splitter and an MCT detector. After each infrared spectrum of a grain was measured, a background spectrum was determined and then subtracted from the spectrum of that grain for normalization. For each spectrum, a total of 128 scans were accumulated with a resolution of 4 cm-1. The aperture size was 50×50 μm to 100×100 μm depending on grain sizes. Optically clean, crack-free areas, usually centered in the core region of each grain, were carefully selected for the measurements. To check the homogeneity of water concentration within minerals, we also measured by unpolarized FTIR along a profile (usually parallel to the long axis of the target grains) across the selected grains.
Water concentration was calculated by a modified form of the Beer-Lambert Law
|
c=Δ/(I×t) |
(1) |
where c is the hydroxyl concentration (ppm H2O by weight), Δ is the integrated area (cm-1) of absorption bands in the region of interest, I is the integral specific absorption coefficient (ppm-1 cm-2), and t is thickness (cm). Based on the calibration parameter from Bell et al. (2004) for kyanite, from Bell et al. (1995) for garnet, and from Koch-Müller et al. (2007) for omphacite, the Eq. (1) can be rewritten as
|
c=α×Δ′ |
(2) |
with Δ' being the integrated area of absorption bands normalized to 1 cm thickness, and α being 0.147, 0.710, and 0.092 for kyanite, garnet, and omphacite, respectively. The Eq. (2) was then used to calculate water concentrations in minerals according to their corresponding integrated area. To facilitate comparison with the results of previous studies on omphacite, we also gave the water concentration of omphacite calculated using the calibration for augite from Bell et al. (1995). However, the Bell's calibration leads to significant overestimation of water concentration in omphacite, while the Koch-Müller's calibration is considered most accurate currently for omphacite (Skogby et al., 2016). Baseline corrections were manually performed using the Omnic software and the obtained area beneath the OH peaks was multiplied by 3 to give the Δ' values (Kovács et al., 2008; Sambridge et al., 2008). Uncertainties in the obtained results mainly derive from a combination of baseline correction and use of an unpolarized IR beam on unoriented anisotropic minerals, in addition to errors on sample thickness. On the whole, the total uncertainty in the calculated water concentration is generally estimated to be around 30% (e.g., Demouchy et al., 2015; Denis et al., 2015; Xia et al., 2010). To minimize the uncertainties, the following measures were taken: (1) the sample thickness was measured with a digital micrometer and reported as an average of 10 measurements covering the whole section; and (2) more than 10 different grains in the same sample were analyzed (Withers, 2013; Kovács et al., 2008).
The typical infrared spectra and FTIR results for kyanite, garnet, and omphacite are presented in Fig. 4 and Table 1, respectively. Kyanite displays consistent and significant absorption bands in their IR spectra (Fig. 4a). These bands can be divided into two groups: a triplet of strong sharp bands at 3 440, 3 410, and 3 386 cm-1 and a doublet of broad bands at 3 276 and 3 261 cm-1. The band at 3 386 cm-1 dominates the former group, which is typical for kyanite from crustal rocks (Wieczorek et al., 2004). Similar IR spectra are reported from other natural kyanites from several different geological environments (Bell et al., 2004; Beran et al., 1993; Rossman and Smyth, 1990; Beran and Götzinger, 1987) and are attributed to bound OH in the kyanite structure. Kyanites contain water concentrations of 21 wt ppm–41 wt ppm (see Table 1).
| Sample | Garnet | Omphacite | Kyanite | ||||||
| CH2O (wt ppm) | Measured grains | CH2O (wt ppm)1 | CH2O (wt ppm)2 | Measured grains | CH2O (wt ppm) | Measured grains | |||
| MB1-3 | 46 | 13 | 321 | 492 | 12 | 41 | 34 | ||
| MB7-1 | 83 | 12 | 425 | 652 | 13 | 37 | 21 | ||
| MB11-1 | - | - | 548 | 840 | 4 | 21 | 14 | ||
| MB17 | 66 | 16 | 302 | 463 | 15 | 22 | 11 | ||
| 1. Water concentration calculated using the calibration parameter from Koch-Müller et al. (2007); 2. water concentration calculated using the calibration parameter from Bell et al. (1995). | |||||||||
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Due to extensive cracking and abundant inclusions, FTIR analyses for garnet in the sample MB11-1 were unsuccessful. For the other three samples, garnet shows broadly similar hydroxyl absorption bands in the region of 3 600–3 700 cm-1, which can be divided into two groups: 3 645–3662 cm-1 and 3 623–3 631 cm-1 (Fig. 4b). The latter is slightly weaker in intensity than the former and sometimes even disappears. These bands are commonly observed in garnet from eclogites and mantle peridotites (e.g., Sheng et al., 2007; Katayama et al., 2006; Xia et al., 2005; Matsyuk et al., 1998; Withers et al., 1998; Beran et al., 1993; Bell and Rossman, 1992; Aines and Rossman, 1984), and are considered to result from vibrations of tetrahedral (OH)44- clusters replacing SiO44- tetrahedra (Beran et al., 1993). Other bands common in garnet, like those around 3 400 and 3 570 cm-1 (e.g., Sheng et al., 2007; Xia et al., 2005; Su et al., 2002; Matsyuk et al., 1998; Bell and Rossman, 1992), are absent in the Maobei eclogites. The calculated water concentrations of garnet are highly variable even in the same sample. The average water concentration ranges from 46 wt ppm (sample MB1-3) to 83 (sample MB7-1) wt ppm (Table 1).
Infrared spectra of omphacite from all samples are roughly similar and can be divided into three groups of absorption bands: (Ⅰ) 3 440–3 460; (Ⅱ) 3 500–3 530, and (Ⅲ) 3 600–3 625 cm-1 (Fig. 4c). These bands are analogous to those reported by previous studies for omphacite (e.g., Skogby et al., 2016; Huang et al., 2014; Koch-Müller et al., 2007, 2004; Katayama et al., 2006; Katayama and Nakashima, 2003). The intensity of absorption bands for each group differs, with the group-I bands usually being the strongest and the group-Ⅲ bands being the weakest. Sometimes, additional strong sharp bands around 3 670 cm-1 also occur, especially from regions close to grain boundaries and cracks. However, spectra with such bands are disregarded during calculation of water concentration, for they are thought to indicate the presence of amphibole due to alteration (e.g., Koch-Müller et al., 2004). As expected, water contents calculated using the calibration parameter of Bell et al. (1995) are much higher than those calculated using the calibration of Koch-Müller et al. (2007) (Table 1). Like in garnet, water concentrations in omphacite also vary considerably, ranging from 302 wt ppm to 548 wt ppm (Table 1).
We have attempted to perform FTIR profile analyses on garnet and omphacite, but failed owing to widespread cracks and/or alterations in both minerals. Ten large (0.5–0.7 mm) kyanite grains from different samples had been selected to carry out the FTIR profile analyses. Due to the occasional presence of inclusions and/or cracks along the profile across each kyanite grain, it is not convenient to present the profile results according to the absolute position of each spectrum. Instead, each spectrum in a profile is arranged in their relative position from one end to the other end of the measured grains. As shown in Fig. 5, the distribution of water concentration in kyanite is generally homogeneous; no systematic differences in water concentration between core and rim were observed. The small variations of water concentration (see for example Fig. 5a) within some grains probably reflect errors related to baseline correction and are within the uncertainty (~30%).
The FTIR profile analyses (Fig. 5) reveal a homogeneous water distribution within kyanite from the Maobei eclogites, which implies that kyanite most likely does not lose its water significantly during exhumation. Similarly, such a homogeneous distribution of water in other minerals (like olivine and orthopyroxene) is commonly considered to signify preservation of their initial water concentration (e.g., Wang et al., 2016; Demouchy et al., 2015). On the contrary, diffusional loss of water in minerals is usually manifested by higher water concentration in the core and lower water concentration in the rim (e.g., Tian et al., 2017; Li et al., 2008; Demouchy et al., 2006; Peslier and Luhr, 2006). Omphacite in contact with matrix kyanite is free of retrogression (Fig. 3b), suggesting insignificant water release from kyanite during exhumation, which is consistent with the above inference. Intensive symplectization of omphacite occurred adjacent to and along the kyanite-quartz-rich veins (Fig. 3c), and was explained as being induced by water released from the veins itself rather than the minerals. Water in the kyanite-quartz-rich veins was probably derived from the breakdown of lawsonite by the reaction: lawsonite=kyanite+zoisite+coesite+H2O. A precursor lawsonite phase can be assumed by the coexistence of quartz, kyanite, and zoisite in the veins (Fig. 3c).
The preservation of initial water concentration in kyanite is probably facilitated by the very rapid exhumation of its host eclogites. Xia et al. (2005) explored the water concentration of garnet within eclogites from the Dabie terrane and found an inhomogeneous distribution of water within garnet from sample to outcrop scale. They suggested that the exhumation of the subducted crust should be fast while the mobility of fluids should be limited; otherwise, any heterogeneity of water in garnet would be easily erased. Water concentrations in garnets from the Maobei eclogites are also quite heterogeneous, implying fast exhumation and limited fluid mobility for these eclogites.
The calculated average water concentration in kyanite in this study ranges from 21 wt ppm to 41 wt ppm (Table 1). These values are far below those reported by many previous studies (Beran et al., 1993; Rossman and Smyth, 1990; Beran and Götzinger, 1987; Wilkins and Sabine, 1973). Though varying with occurrences, water concentrations in kyanite from eclogites reported by these studies are generally large, from several hundred to more than one thousand ppm by weight (Beran et al., 1993; Rossman and Smyth, 1990; Beran and Götzinger, 1987), which are much higher than those in this study. This huge disparity is due to two reasons. First, these previous studies utilized the calibration of Beran and Götzinger (1987) while we used the calibration of Bell et al. (2004). The former had been shown to substantially overestimate (up to a factor of 15) the water concentration in kyanite (Bell et al., 2004). Second, many of the spectra presented in these previous studies contain absorption bands at high wave numbers (~3 600 cm-1), which are suggested to be related to intergrowth of hydrous minerals (Beran and Götzinger, 1987). In contrast, such absorption bands are absent in the infrared spectra of kyanite from the Maobei eclogites. When calculated from the calibration of Bell et al. (2004), water concentrations in kyanite reported by previous studies vary between 3 wt ppm and 230 wt ppm, with most of them less than 50 wt ppm (see the review by Johnson, 2006). These values are then comparable to those of kyanite in this study.
Eclogite represents an important component in subudction zones. Due to breakdown of some hydrous minerals (like amphibole and epidote) at shallow depth, water stored as structurally bound hydrogen within NAMs, such as garnet, omphacite, coesite, rutile, kyanite, etc., becomes a major source of water in deep subducted crust. As the volumetrically dominant mineral phases, garnet and omphacite are generally considered to control the water storage of anhydrous eclogites and the water contents that can be recycled to mantle depth (e.g., Sheng et al., 2007; Katayama et al., 2006). However, garnet generally contains much lower water contents than coexisting omphacite (e.g., Konzett et al., 2008; Sheng et al., 2007; Katayama et al., 2006), even excluding the influence of calibration parameters. The same is true for the Maobei eclogites (see Table 1). These facts suggest that omphacite is the major nominally anhydrous water carrier in eclogites.
The water concentrations in kyanite from the Maobei eclogites are lower compared with those in garnet and omphacite (Table 1), suggesting that kyanite is not a major water carrier in these samples. Considering its lower volume fraction, we concluded that the contribution of kyanite to the total water concentrations of the Maobei eclogites is negligible. This further implies that kyanite does not play an important role, unlike garnet and omphacite (Katayama et al., 2006; Katayama and Nakashima, 2003), in transporting water into the deep mantle during subduction of oceanic crust. But if kyanite transforms to hydrous AlSiO3OH (Schmidt et al., 1998), it may become more important in transporting water into the deep earth (Bell et al., 2004).
In this study, we carried out a detailed FTIR analyses on kyanite, garnet, and omphacite from the Maobei eclogites and reached the following conclusions.
1. Kyanites from the Maobei eclogites most likely preserves their initial water contents at depth.
2. Kyanites have water contents comparable to those reported by previous studies when calculated using the most recent calibration but lower than in coexisting garnet and omphacite from the Maobei eclogites.
3. Kyanite contributes little to transport water into the deep earth till its possible transformation to AlSiO3OH.
ACKNOWLEDGMENTS: We thank Profs. Ke-Qing Zong, Hai-Jun Xu, and Qiang Liu for help during the field work. Dr. Da-Peng Wen is greatly thanked for assistance with the FTIR measurements. We also appreciate Prof. Jun-Feng Zhang for his constructive discussion and suggestions. Two anonymous reviewers are thanked for their thoughtful comments and suggestions. This study was supported by the National Natural Science Foundation of China (Nos. 41372224 and 41590623). The final publication is available at Springer via https://doi.org/10.1007/s12583-017-0774-0.| Aines, R. D., Rossman, G. R., 1984. The Hydrous Component in Garnet: Pyralspites. American Mineralogist, 69: 1116-1126. https://doi.org/10.2138/am-1998-7-815 |
| Beane, R. J., Field, C. K., 2007. Kyanite Deformation in Whiteschist of the Ultrahigh-Pressure Metamorphic Kokchetav Massif, Kazakhstan. Journal of Metamorphic Geology, 25(2): 117-128. https://doi.org/10.1111/j.1525-1314.2007.00692.x |
| Bell, D. R., Rossman, G. R., 1992. Water in Earth's Mantle: The Role of Nominally Anhydrous Minerals. Science, 255(5050): 1391-1397. https://doi.org/10.1126/science.255.5050.1391 |
| Bell, D. R., Ihinger, P. D., Rossman, G. R., 1995. Quantitative Analysis of Trace OH in Garnet and Pyroxenes. American Mineralogist, 80(5/6): 465-474. https://doi.org/10.2138/am-1995-5-607 |
| Bell, D. R., Rossman, G. R., Maldener, J., et al., 2004. Hydroxide in Kyanite: A Quantitative Determination of the Absolute Amount and Calibration of the IR Spectrum. American Mineralogist, 89(7): 998-1003. https://doi.org/10.2138/am-2004-0710 |
| Beran, A., Götzinger, M. A., 1987. The Quantitative IR Spectroscopic Determination of Structural OH Groups in Kyanites. Mineralogy and Petrology, 36(1): 41-49. https://doi.org/10.1007/bf01164368 |
| Beran, A., Langer, K., Andrut, M., 1993. Single Crystal Infrared Spectra in the Range of OH Fundamentals of Paragenetic Garnet, Omphacite and Kyanite in an Eklogitic Mantle Xenolith. Mineralogy and Petrology, 48(2/3/4): 257-268. https://doi.org/10.1007/bf01163102 |
| Chen, R. X., Zheng, Y. F., Gong, B., et al., 2007. Origin of Retrograde Fluid in Ultrahigh-Pressure Metamorphic Rocks: Constraints from Mineral Hydrogen Isotope and Water Content Changes in Eclogite-Gneiss Transitions in the Sulu Orogen. Geochimica et Cosmochimica Acta, 71(9): 2299-2325. https://doi.org/10.1016/j.gca.2007.02.012 |
| Denis, C. M. M., Alard, O., Demouchy, S., 2015. Water Content and Hydrogen Behaviour during Metasomatism in the Uppermost Mantle beneath Ray Pic Volcano (Massif Central, France). Lithos, 236/237: 256-274. https://doi.org/10.1016/j.lithos.2015.08.013 |
| Demouchy, S., Jacobsen, S. D., Gaillard, F., et al., 2006. Rapid Magma Ascent Recorded by Water Diffusion Profiles in Mantle Olivine. Geology, 34(6): 429-432. https://doi.org/10.1130/g22386.1 |
| Demouchy, S., Ishikawa, A., Tommasi, A., et al., 2015. Characterization of Hydration in the Mantle Lithosphere: Peridotite Xenoliths from the Ontong Java Plateau as an Example. Lithos, 212-215: 189-201. https://doi.org/10.1016/j.lithos.2014.11.005 |
| Hollis, J. A., Harley, S. L., White, R. W., et al., 2006. Preservation of Evidence for Prograde Metamorphism in Ultrahigh-Temperature, High-Pressure Kyanite-Bearing Granulites, South Harris, Scotland. Journal of Metamorphic Geology, 24(3): 263-279. https://doi.org/10.1111/j.1525-1314.2006.00636.x |
| Hu, S. X., Sun, J. G., Ling, H. F., et al., 2001. The Lanshantou Kyanite-Bearing Eclogite with Coesite Inclusions in the Sulu Ultrahigh-Pressure Metamorphic Belt and Its PTt Path. Acta Geologica Sinica—English Edition, 75(4): 409-420. https://doi.org/10.1111/j.1755-6724.2001.tb00059.x |
| Huang, J. X., Li, P., Griffin, W. L., et al., 2014. Water Contents of Roberts Victor Xenolithic Eclogites: Primary and Metasomatic Controls. Contributions to Mineralogy and Petrology, 168(6): 1092. https://doi.org/10.1007/s00410-014-1092-5 |
| Johnson, E. A., 2006. Water in Nominally Anhydrous Crustal Minerals: Speciation, Concentration, and Geologic Significance. Reviews in Mineralogy and Geochemistry, 62(1): 117-154. https://doi.org/10.2138/rmg.2006.62.6 |
| Katayama, I., Nakashima, S., 2003. Hydroxyl in Clinopyroxene from the Deep Subducted Crust: Evidence for H2O Transport into the Mantle. American Mineralogist, 88(1): 229-234. https://doi.org/10.2138/am-2003-0126 |
| Katayama, I., Nakashima, S., Yurimoto, H., 2006. Water Content in Natural Eclogite and Implication for Water Transport into the Deep Upper Mantle. Lithos, 86(3/4): 245-259. https://doi.org/10.1016/j.lithos.2005.06.006 |
| Klonowska, I., Majka, J., Janák, M., et al., 2014. Pressure-Temperature Evolution of a Kyanite-Garnet Pelitic Gneiss from reskutan: Evidence of Ultra-High-Pressure Metamorphism of the Seve Nappe Complex, West-Central J mtland, Swedish Caledonides. Geological Society, London, Special Publications, 390(1): 321-336. https://doi.org/10.1144/sp390.7 |
| Koch-Müller, M., Matsyuk, S. S., Wirth, R., 2004. Hydroxyl in Omphacites and Omphacitic Clinopyroxenes of Upper Mantle to Lower Crustal Origin beneath the Siberian Platform. American Mineralogist, 89(7): 921-931. https://doi.org/10.2138/am-2004-0701 |
| Koch-Müller, M., Abs-Wurmbach, I., Rhede, D., et al., 2007. Dehydration Experiments on Natural Omphacites: Qualitative and Quantitative Characterization by Various Spectroscopic Methods. Physics and Chemistry of Minerals, 34(9): 663-678. https://doi.org/10.1007/s00269-007-0181-7 |
| Konzett, J., Libowitzky, E., Hejny, C., et al., 2008. Oriented Quartz+Calcic Amphibole Inclusions in Omphacite from the Saualpe and Pohorje Mountain Eclogites, Eastern Alps—An Assessment of Possible Formation Mechanisms Based on IR-and Mineral Chemical Data and Water Storage in Eastern Alpine Eclogites. Lithos, 106(3/4): 336-350. https://doi.org/10.1016/j.lithos.2008.09.002 |
| Kotková, J., Janák, M., 2015. UHP Kyanite Eclogite Associated with Garnet Peridotite and Diamond-Bearing Granulite, Northern Bohemian Massif. Lithos, 226: 255-264. https://doi.org/10.1016/j.lithos.2015.01.016 |
| Kovács, I., Hermann, J., O'Neill, H. S. C., et al., 2008. Quantitative Absorbance Spectroscopy with Unpolarized Light: Part Ⅱ. Experimental Evaluation and Development of a Protocol for Quantitative Analysis of Mineral IR Spectra. American Mineralogist, 93(5/6): 765-778. https://doi.org/10.2138/am.2008.2656 |
| Li, Z. X. A., Lee, C. T. A., Peslier, A. H., et al., 2008. Water Contents in Mantle Xenoliths from the Colorado Plateau and Vicinity: Implications for the Mantle Rheology and Hydration-Induced Thinning of Continental Lithosphere. Journal of Geophysical Research, 113(B9): B09210. https://doi.org/10.1029/2007jb005540 |
| Liou, J. G., Zhang, R. Y., 1996. Occurrences of Intergranular Coesite in Ultrahigh-P Rocks from the Sulu Region, Eastern China; Implications for Lack of Fluid during Exhumation. American Mineralogist, 81(9/10): 1217-1221. https://doi.org/10.2138/am-1996-9-1020 |
| Liu, F. L., Xu, Z. Q., Liou, J. G., et al., 2004. SHRIMP U-Pb Ages of Ultrahigh-Pressure and Retrograde Metamorphism of Gneisses, South-Western Sulu Terrane, Eastern China. Journal of Metamorphic Geology, 22(4): 315-326. https://doi.org/10.1111/j.1525-1314.2004.00516.x |
| Matsyuk, S. S., Langer, K., H sch, A., 1998. Hydroxyl Defects in Garnets from Mantle Xenoliths in Kimberlites of the Siberian Platform. Contributions to Mineralogy and Petrology, 132(2): 163-179. https://doi.org/10.1007/s004100050414 |
| Peslier, A., Luhr, J., 2006. Hydrogen Loss from Olivines in Mantle Xenoliths from Simcoe (USA) and Mexico: Mafic Alkalic Magma Ascent Rates and Water Budget of the Sub-Continental Lithosphere. Earth and Planetary Science Letters, 242(3/4): 302-319. https://doi.org/10.1016/j.epsl.2005.12.019 |
| Rossman, G. R., Smyth, J. R., 1990. Hydroxyl Contents of Accessory Minerals in Mantle Eclogites and Related Rocks. American Mineralogist, 75: 765-780 http://rruff.info/doclib/am/vol75/AM75_775.pdf |
| Sambridge, M., Gerald, J. F., Kovacs, I., et al., 2008. Quantitative Absorbance Spectroscopy with Unpolarized Light: Part Ⅰ. Physical and Mathematical Development. American Mineralogist, 93(5/6): 751-764. https://doi.org/10.2138/am.2008.2657 |
| Schmidt, M. W., Finger, L. W., Angel, R. J., et al., 1998. Synthesis, Crystal Structure, and Phase Relations of AlSiO3OH, a High-Pressure Hydrous Phase. American Mineralogist, 83(7/8): 881-888. https://doi.org/10.2138/am-1998-7-820 |
| Sheng, Y. M., Xia, Q.-K., Dallai, L., et al., 2007. H2O Contents and D/H Ratios of Nominally Anhydrous Minerals from Ultrahigh-Pressure Eclogites of the Dabie Orogen, Eastern China. Geochimica et Cosmochimica Acta, 71(8): 2079-2103. https://doi.org/10.1016/j.gca.2007.01.018 |
| Skogby, H., Janák, M., Broska, I., 2016. Water Incorporation in Omphacite: Concentrations and Compositional Relations in Ultrahigh-Pressure Eclogites from Pohorje, Eastern Alps. European Journal of Mineralogy, 28(3): 631-639. https://doi.org/10.1127/ejm/2016/0028-2533 |
| Su, W., You, Z. D., Cong, B. L., et al., 2002. Cluster of Water Molecules in Garnet from Ultrahigh-Pressure Eclogite. Geology, 30(7): 611. https://doi.org/10.1130/0091-7613(2002)030<0611:cowmig>2.0.co;2 doi: 10.1130/0091-7613(2002)030<0611:cowmig>2.0.co;2 |
| Terry, M. P., Robinson, P., Ravna, E. J. K., 2000. Kyanite Eclogite Thermobarometry and Evidence for Thrusting of UHP over HP Metamorphic Rocks, Nord yane, Western Gneiss Region, Norway. American Mineralogist, 85(11/12): 1637-1650. https://doi.org/10.2138/am-2000-11-1207 |
| Tian, Z. Z., Liu, J., Xia, Q.-K., et al., 2017. Water Concentration Profiles in Natural Mantle Orthopyroxenes: A Geochronometer for Long Annealing of Xenoliths within Magma. Geology, 45(1): 87-90. https://doi.org/10.1130/g38620.1 |
| Wang, Y. F., Ren, H. P., Jin, Z. M., 2016. Water and Fabric in an Ophiolitic Peridotite from a Supra-Subduction Zone. Contributions to Mineralogy and Petrology, 171(3): 22. https://doi.org/10.13039/501100001809 |
| Wieczorek, A., Libowitzky, E., Beran, A., 2004. A Model for the OH Incorporation in Kyanite Based on Polarised IR Spectroscopic Investigations. Schweizerische Mineralogische und Petrographische Mitteilungen, 84: 333-343 doi: 10.1007/s12583-017-0774-0 |
| Wilkins, R. W. T., Sabine, W., 1973. Water Content of Some Nominally Anhydrous Silicates. American Mineralogist, 58: 508-516 doi: 10.1007/BF01164492.pdf |
| Withers, A. C., 2013. On the Use of Unpolarized Infrared Spectroscopy for Quantitative Analysis of Absorbing Species in Birefringent Crystals. American Mineralogist, 98(4): 689-697. https://doi.org/10.2138/am.2013.4316 |
| Withers, A. C., Wood, B. J., Carroll, M. R., 1998. The OH Content of Pyrope at High Pressure. Chemical Geology, 147(1/2): 161-171. https://doi.org/10.1016/s0009-2541(97)00179-4 |
| Xia, Q.-K., Sheng, Y. M., Yang, X. Z., et al., 2005. Heterogeneity of Water in Garnets from UHP Eclogites, Eastern Dabieshan, China. Chemical Geology, 224(4): 237-246. https://doi.org/10.1016/j.chemgeo.2005.08.003 |
| Xia, Q.-K., Hao, Y. T., Li, P., et al., 2010. Low Water Content of the Cenozoic Lithospheric Mantle beneath the Eastern Part of the North China Craton. Journal of Geophysical Research, 115(B7): B07207. https://doi.org/10.1029/2009jb006694 |
| Zhang, J. F., Green, H. W. II, 2007. Experimental Investigation of Eclogite Rheology and Its Fabrics at High Temperature and Pressure. Journal of Metamorphic Geology, 25(2): 97-115. https://doi.org/10.1111/j.1525-1314.2006.00684.x |
| Zhang, R. Y., Hirajima, T., Banno, S., et al., 1995. Petrology of Ultrahigh-Pressure Rocks from the Southern Su-Lu Region, Eastern China. Journal of Metamorphic Geology, 13(6): 659-675. https://doi.org/10.1111/j.1525-1314.1995.tb00250.x |
| Zhang, R. Y., Liou, J. G., Ernst, W. G., 2009. The Dabie-Sulu Continental Collision Zone: A Comprehensive Review. Gondwana Research, 16(1): 1-26. https://doi.org/10.1016/j.gr.2009.03.008 |
| Zhang, Z. M., Liou, J. G., Zhao, X. D., et al., 2006. Petrogenesis of Maobei Rutile Eclogites from the Southern Sulu Ultrahigh-Pressure Metamorphic Belt, Eastern China. Journal of Metamorphic Geology, 24(8): 727-741. https://doi.org/10.1111/j.1525-1314.2006.00665.x |
| Zheng, Y. F., Fu, B., Gong, B., et al., 2003. Stable Isotope Geochemistry of Ultrahigh Pressure Metamorphic Rocks from the Dabie-Sulu Orogen in China: Implications for Geodynamics and Fluid Regime. Earth-Science Reviews, 62(1/2): 105-161. https://doi.org/10.1016/s0012-8252(02)00133-2 |
| [1] | CONTENTS[J]. Journal of Earth Science, 2024, 35(4): . |
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| 1. | Haiqi Yuan, Jian Wang, Zhipeng Xie, et al. Ultrahigh-Pressure Metamorphism and P-T-t Paths for the Eclogites from the Central Areas of Sulu Orogen, Eastern China. Minerals, 2023, 13(3): 362. doi:10.3390/min13030362 | |
| 2. | Haiqi Yuan, Jian Wang, Keiko Hattori. Ultrahigh-Pressure Metamorphism and P-T Path of Xiaoxinzhuang Eclogites from the Southern Sulu Orogenic Belt, Eastern China, Based on Phase Equilibria Modelling. Minerals, 2022, 12(2): 216. doi:10.3390/min12020216 | |
| 3. | Souravi Bardhan, Shubham Roy, Sanghita Das, et al. Real-time sensitive detection of Cr (VI) in industrial wastewater and living cells using carbon dot decorated natural kyanite nanoparticles. Spectrochimica Acta Part A: Molecular and Biomolecular Spectroscopy, 2022, 273: 121061. doi:10.1016/j.saa.2022.121061 | |
| 4. | Peng Feng, Lu Wang, Michael Brown, et al. Separating multiple episodes of partial melting in polyorogenic crust: An example from the Haiyangsuo complex, northern Sulu belt, eastern China. GSA Bulletin, 2020, 132(5-6): 1235. doi:10.1130/B35210.1 |
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Yi-Ning Wu, Yong-Feng Wang. An FTIR Study of Kyanite in the Maobei Kyanite-Bearing Eclogites from the Sulu Orogenic Belt, Eastern China. Journal of Earth Science, 2018, 29(1): 21-29. doi: 10.1007/s12583-017-0774-0
| Sample | Garnet | Omphacite | Kyanite | ||||||
| CH2O (wt ppm) | Measured grains | CH2O (wt ppm)1 | CH2O (wt ppm)2 | Measured grains | CH2O (wt ppm) | Measured grains | |||
| MB1-3 | 46 | 13 | 321 | 492 | 12 | 41 | 34 | ||
| MB7-1 | 83 | 12 | 425 | 652 | 13 | 37 | 21 | ||
| MB11-1 | - | - | 548 | 840 | 4 | 21 | 14 | ||
| MB17 | 66 | 16 | 302 | 463 | 15 | 22 | 11 | ||
| 1. Water concentration calculated using the calibration parameter from Koch-Müller et al. (2007); 2. water concentration calculated using the calibration parameter from Bell et al. (1995). | |||||||||
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CSV
| Sample | Garnet | Omphacite | Kyanite | ||||||
| CH2O (wt ppm) | Measured grains | CH2O (wt ppm)1 | CH2O (wt ppm)2 | Measured grains | CH2O (wt ppm) | Measured grains | |||
| MB1-3 | 46 | 13 | 321 | 492 | 12 | 41 | 34 | ||
| MB7-1 | 83 | 12 | 425 | 652 | 13 | 37 | 21 | ||
| MB11-1 | - | - | 548 | 840 | 4 | 21 | 14 | ||
| MB17 | 66 | 16 | 302 | 463 | 15 | 22 | 11 | ||
| 1. Water concentration calculated using the calibration parameter from Koch-Müller et al. (2007); 2. water concentration calculated using the calibration parameter from Bell et al. (1995). | |||||||||
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