Advances in Materials Science and Engineering

Volume 2013 (2013), Article ID 502702, 6 pages

http://dx.doi.org/10.1155/2013/502702

Research Article

High Pressure Elastic Behavior of Synthetic Mg₃Y₂(SiO₄)₃ Garnet up to 9 GPa

Dawei Fan,¹ Maining Ma,² Shuyi Wei,1,3 Zhiqiang Chen,⁴ and Hongsen Xie¹

¹Laboratory for High Temperature and High Pressure Study of the Earth’s Interior of Institute of Geochemistry, Chinese Academy of Sciences, Guiyang 550002, China

²Key Laboratory of Computational Geodynamics of Chinese Academy of Sciences, University of Chinese Academy of Sciences, Beijing 100049, China

³University of Chinese Academy of Sciences, Beijing 100049, China

⁴Department of Geosciences, Stony Brook University, Stony Brook, NY 11794, USA

Received 5 July 2013; Accepted 14 August 2013

Academic Editor: Pavel Strunz

Copyright © 2013 Dawei Fan et al. This is an open access article distributed under the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.

Abstract.

The compression behavior of synthetic magnesium- (Mg-) yttrium (Y) garnet Mg₃Y₂(SiO₄)₃ has been investigated upto about 8.79 GPa at 300 K using in situ angle-dispersive X-ray diffraction and a diamond anvil cell at the beamline X17C, National Synchrotron Light Source, Brookhaven National Laboratory. No phase transition has been observed within the pressure range investigated. The unit-cell parameters and volume decreased systematically with increasing pressure, and a reliable isothermal bulk modulus () and its pressure derivative () were obtained in this study. The values of zero-pressure volume , , and refined with a third-order Birch-Murnaghan equation of state are  Å³,  GPa, and . If is fixed at 4, is obtained as  GPa.

1. Introduction

Garnets are an important constituent of the upper mantle and mantle transition zone of the Earth and play a fundamental role in high pressure and high temperature petrogenetic processes [1, 2]. Garnets are also important components of subducted oceanic crust, and it is suggested that garnet-rich subducted crust can be gravitationally trapped in the lowermost part of the mantle transition zone [3–6]. Therefore, accurate knowledge of the physical properties of garnets is essential to infer appropriate compositional models for the upper mantle and mantle transition zone of the Earth. In addition, garnet is the major host of the rare-earth element (REE) both in metamorphic rocks and mantle rocks, and the latter may undergo partial melting in the mantle [7]. Thus, there is a considerable interest in the study of the thermodynamic behavior of REE in garnet that could help to understand the evolution of REE patterns in magmas and in the residual solids [7–9], especially garnets in igneous and metamorphic rocks.

Garnets have the general formula X₃Y₂(SiO₄)₃, centered cubic lattice (space group Ia–3d), and display 8-fold dodecahedral (X), 6-fold octahedral (Y), and tetrahedral (Si) crystallographic sites. This unique behavior makes the garnet structure flexible in accommodating various chemical substitutions with different ionic radii, suggesting that garnets could be composition diverse where X = Mg²⁺, Fe²⁺, Ca²⁺, Mn²⁺, Y³⁺; Y = Al³⁺, Fe³⁺, Cr³⁺, and Y³⁺. Chemical substitutions at octahedral and triangular dodecahedral sites may change the relative bond lengths/interatomic distances and angles, which will result in affecting their elastic properties [6].

Yttrium is a silvery-metallic transition metal chemically similar to the lanthanides, and it has often been classified as a “rare earth element”. Yttrium is almost always found combined with the lanthanides in rare-earth minerals [10, 11]. It is used in the production of a large variety of synthetic garnets [12], and yttria is used to make yttrium iron garnets (Y₃Fe₅O₁₂, YIG), which are very effective microwave filters. YIG is also very efficient as an acoustic energy transmitter and transducer [13]. Yttrium aluminium garnet (Y₃Al₅O₁₂, YAG) is used in a number of industrial applications, either in the pure phase form or as a composite [14].

To date, the elastic properties of pyrope have been studied extensively by multianvil apparatus and diamond anvil cell [6, 15–22]. However, nowadays, there are no studies available on the elastic behavior of rare-earth silicate garnet at high pressure. In addition, yttrium not only can substitute for Mg at the dodecahedral site but also can substitute for Al at the octahedral site in the silicate garnet. In this paper, we report the elastic measurements of magnesium- (Mg-) yttrium (Y) garnet [Mg₃Y₂(SiO₄)₃], a synthetic rare-earth silicate garnet, up to pressures of 8.79 GPa at room temperature. Along with the previous results for pyrope [6, 15–22], the compositional dependence of the bulk modulus is discussed.

2. Sample and Experiment

The Mg₃Y₂(SiO₄)₃ sample used in our high pressure powder X-ray diffraction experiments was synthesized with a multianvil pressure apparatus (YJ-3000T) installed at the Institute of Geochemistry, Chinese Academy of Sciences. Details about the apparatus have been described by Xie et al. [23]. The pressurization system of this press consists of six WC anvils, with their tips truncated as  mm², which are simultaneously pushed by six hydraulic rams so that high pressure is generated in the experimental assembly. The experimental assembly, YJ-3000T, used in this study, is schematically illustrated in Figure 1. The experimental temperature was measured and controlled with a Pt₉₄Rh₆-Pt₇₀Rh₃₀ thermocouple (type B). The starting materials used in the synthesizing experiments were stoichiometric amounts of high purity MgCO₃, Y₂O₃, and SiO₂ and were placed one night at 800°C for removing carbonates. The mixture was then melted at 1400°C which produced, after quenching, a homogeneous glass. The homogeneous glass was crushed into a fine powder using acetone. The starting mixtures were encapsulated in platinum capsules. The synthesizing pressure and temperature conditions were 4 GPa and 1000°C for 24 h. The crystal structure of sample was confirmed by using powder X-ray diffraction method (X’Pert Pro MPD system). Their compositions were confirmed by using electron microprobe analysis (EPMA-1600).

Figure 1: Experimental assembly used in the high pressure synthesizing experiments with a multianvil pressure apparatus (YJ-3000T) installed at the Institute of Geochemistry, Chinese Academy of Sciences.

In this investigation, we conducted in situ high-pressure angle dispersive X-ray diffraction experiments at the beamline X17C, National Synchrotron Light Source (NSLS), Brookhaven National Laboratory, using a 0.37677 Å X-ray beam and CCD detector, and the beamline 4W2, Beijing Synchrotron Radiation Facility (BSRF), using a 0.6199 Å X-ray beam and Mar345 detector. We generated the high pressure by using a symmetrical diamond-anvil cell, equipped with two diamonds anvils (culet face diameter: 500 μm) and tungsten-carbide supports. In these high pressure experiments, T301 stainless steel plates with an initial thickness of 200 μm were used as gaskets, with their central part preindented to a thickness of about 50 μm and then drilled through into a hole of 200 μm diameter. The finely ground Mg₃Y₂(SiO₄)₃ powder, plus a couple of tiny ruby balls together with a methanol : ethanol : water mixture (16 : 3 : 1 by volume) which is a hydrostatic pressure-transmitting medium up to about 10 GPa [24], was loaded into the gasket hole. The ruby fluorescence method [25] was employed to determine the experimental pressure. The X-ray diffraction patterns (collecting time = 10 min) were integrated to generate the conventional one-dimensional profiles using the Fit2D program [26]. The sample was equilibrated for about 10 min before diffraction data measurement, and subsequently the pressure was raised up to 8.79 GPa. Unit-cell parameters were refined by Le Bail fitting using the GSAS package [27, 28] and user interface EXPGUI [29] up to 8.79 GPa (Table 2). Background was fitted using the Chebyschev polynomial, and X-ray peak shapes were fitted using the pseudo-Voigt profile function proposed by Thomson et al. [30].

3. Result and Discussion

The powder X-ray diffraction data of Mg₃Y₂(SiO₄)₃ at ambient conditions revealed that this phase has a cubic structure (Ia–3d), with unit-cell dimensions of  Å. The observed and calculated X-ray diffraction patterns of Mg₃Y₂(SiO₄)₃ at ambient conditions are listed in Table 1. The volume of Mg₃Y₂(SiO₄)₃ unit cell at ambient conditions is  Å³.

Table 1: Observed and calculated X-ray diffraction patterns of Mg₃Y₂(SiO₄)₃ at ambient conditions.

h k l
(Å)
(Å)

2 2 0
4.24142
4.24233
−0.00021

3 2 1
3.20735
3.20690
0.00014

4 0 0
2.99925
2.99978
−0.00018

4 2 0
2.68323
2.68308
0.00006

4 2 2
2.44947
2.44931
0.00007

4 3 1
2.35309
2.35322
−0.00006

5 2 1
2.19082
2.19073
0.00004

4 4 0
2.12145
2.12116
0.00014

6 1 1
1.94676
1.94651
0.00013

4 4 4
1.73204
1.73192
0.00007

6 4 0
1.66432
1.66398
0.00020

5 5 2
1.63324
1.63287
0.00023

6 4 2
1.60366
1.60345
0.00013

8 0 0
1.50014
1.49989
0.00017

Calculated d-spacings are based on the cubic unit-cell dimensions of a = 11.9995 Å.

Table 2: Cell parameters versus pressure for Mg₃Y₂(SiO₄)₃.

P (GPa)
a (Å)
V (Å³)

0.0001
11.9995 (4)
1727.8 (2)

0.70
11.9810 (8)
1719.8 (4)

1.69
11.9568 (9)
1709.0 (4)

2.62
11.9325 (9)
1699.0 (4)

3.44
11.9128 (8)
1690.6 (3)

5.14
11.8741 (9)
1674.2 (4)

6.84
11.8399 (9)
1659.7 (4)

7.97
11.8204 (9)
1651.6 (5)

8.79
11.8034 (9)
1644.4 (5)

Numbers in brackets are error in last digits.

The high pressure X-ray diffraction data were collected up to 8.79 GPa at ambient temperature. Typical X-ray diffraction spectrums at selected pressure is shown in Figure 2. The diffraction patterns at each pressure of the study are similar to one another up to 8.79 GPa, with Bragg peaks shifted to higher than . No phase transition occurs within the pressure range investigated. Previous experiments have shown that some of the rare-earth garnets become amorphous at high pressure and room temperature, Gd₃Ga₅O₁₂, Gd₃Sc₂Ga₃O₁₂, and Y₃Fe₅O₁₂ become amorphous at 84, 58, and 50 GPa, [31] respectively, whereas Mg₃Y₂(SiO₄)₃ in this study remains crystalline cubic up to 9 GPa. In addition, the garnets may transfer to perovskite phase at high pressure and high temperature [32]. And for the rare-earth garnets, the amorphous-to-perovskite phase transition requires a very high pressure (~80 GPa) and high temperature (~2000 K) [32, 33]. So, laser heating combined with diamond anvil cell is needed in the amorphous-to-perovskite phase transition study of Mg₃Y₂(SiO₄)₃ for further research.

Figure 2: Representative X-ray diffraction patterns of Mg₃Y₂(SiO₄)₃ up to 8.79 GPa.

The effect of pressure on the unit-cell parameters and volume of Mg₃Y₂(SiO₄)₃ are shown in Table 2. The pressure-volume data have been fitted to the third-order Birch-Murnaghan equation of state (III-BM-EoS) [34] to determine the elastic parameters

where , , , and are the zero-pressure volume, high-pressure volume, isothermal bulk modulus, and its pressure derivative, respectively. The results from a least-squares fitting using an EosFit program [35] are  Å³,  GPa, and , respectively. When is set as 4, the isothermal bulk modulus is determined as  GPa. The unit-cell volume data as a function of pressure and the compression curve calculated from these fitted parameters are plotted in Figure 3.

Figure 3: Volume compression of synthetic Mg₃Y₂(SiO₄)₃ at high pressure and room temperature.

To assess the quality of the Birch-Murnaghan equation of state fit obtained from the plot of unit-cell volume against pressure, the relationship between the Eulerian strain ( and the normalized pressure ( was plotted [35], and it is shown in Figure 4. The - plot provides a visual indication of which higher order terms, such as , are significant in the equation of state. The Mg₃Y₂(SiO₄)₃ data showed a relatively large positive slope (Figure 4). This indicates that the pressure derivative of the bulk modulus () was larger than 4. Therefore, the value, estimated to be 8.5(9), was consistent with the - plot analysis.

Figure 4: Eulerian strain-normalized pressure (-) plot of the data based on the Birch-Murnaghan equation of state. The solid line represents the linear fit.

Table 3 and Figure 3 show a comparison of this study and the previous studies for pyrope at room temperature. So far, the elasticity of pyrope has been studied intensively [6, 15–22], and various reports on of pyrope converge to  GPa. The value of 145(3) GPa obtained in this study for Mg₃Y₂(SiO₄)₃ is about 15% smaller than the values of pyrope. However, the parameters and are usually strongly correlated in an EoSfit [36], so we cannot just compare the bulk modulus and neglect its pressure derivative. Therefore, we compared the results of this study with Hazen et al. and Zou et al. by fixing to 4.0. From Table 3, we can find that the bulk moduli of Hazen et al. [20] and Zou et al. [6] by fixing to 4.0 are 174(3) and 171(1) GPa, respectively. The value of 158(2) GPa obtained in this study for Mg₃Y₂(SiO₄)₃ by fixing to 4.0 is still about 10% smaller than the values of pyrope by fixing to 4.0. There are two possible sources for of this study for Mg₃Y₂(SiO₄)₃ smaller than the results of pyrope for Mg₃Al₂(SiO₄)₃. First, the ionic radius of Al and Y is increasing [Al³⁺ (0.51 Å) < Y³⁺ (0.89 Å)]. Fan et al. [37] studied the grossular-andradite solid solution using high pressure X-ray diffraction and showed the bulk modulus of grossular-andradite solid solution decreases with the increasing andradite content. They considered that the ionic radii of Al³⁺ (0.51 Å) smaller than those of Fe³⁺ (0.64 Å) had a significant influence on bulk modulus of grossular-andradite solid solution. In addition, Liu et al. [38] also suggested that the differences in the elastic behavior of lead fluorapatite and calcium apatites were attributed to the different ionic sizes of Pb²⁺ (1.19 Å) and Ca²⁺ (1.00 Å). Second, we consider that the electronegativity number may be another factor for this situation (1.61 for Al compared with 1.22 for Y). Electronegativity is a chemical property that describes the ability of an atom to attract electrons [39, 40]. An atom’s electronegativity is affected by its atomic weight and the distance of its valence electrons from the charged nucleus [39, 41]. The higher the associated electronegativity number is, the greater an element or compound attracts electrons [41]. The electronegativity is larger, the attraction for bonding electron is stronger, and the electron density between cation and anion is greater, resulting in the fact that crystals have greater compressed resisted capacity [42, 43]. The ionic radius and electronegativity may be having a significant influence on bulk modulus [41, 44]. The smaller of ionic radius and larger electronegativity, the stronger of attraction for bonding electron, the greater of electron density between cation and anion, resulting in crystals have greater compressed resisted capacity [41, 44]. Therefore, we infer that the ionic radius and electronegativity is the main reason for the bulk moduli of this study smaller than the values of pyrope.

Table 3: Elastic parameters derived from the Birch-Murnaghan EoS of Mg₃Y₂(SiO₄)₃ garnet, as compared with previous studies of pyrope garnet.

Sample
(GPa)

Reference

Pyrope

171 (3)
1.8 (7)
Sato et al. (1978) [15]

175 (1)
4.5 (5)
Levien et al. (1979) [17]

172.8a
3.8 (1.0)
Leger et al. (1990) [18]

174 (3)
4.0a
Hazen et al. (1994) [20]

171 (2)
4.4 (2)
Zhang et al. (1998) [22]

167 (6)
4.6 (3)
Zou et al. (2012) [6]

171 (1)
4.0a
Zou et al. (2012) [6]

Mg₃Y₂(SiO₄)₃
145 (3)
8.5 (9)
This study

158 (2)
4.0a
This study

Fixed at this value during data processing.

Numbers in brackets are error in last digits.

4. Conclusion

The measurements on a synthetic Mg₃Y₂(SiO₄)₃ at pressures up to 8.79 GPa were carried out using angle-dispersive X-ray diffraction technique. No phase transition has been observed within the pressure range investigated. The equation of state for the Mg₃Y₂(SiO₄)₃, fitted using the third-order Birch-Murnaghan equation of state, gives Å³,  GPa, and . The value of the bulk modulus in this study for Mg₃Y₂(SiO₄)₃ is smaller than that of pyrope reported previously, which can be attributed to the different ionic radii and electronegativity.

Acknowledgments

This work is supported by the National Natural Science Foundation of China (Grant nos. 41374107, 41004035, and 41274105) and the Western Doctor Special Fund of the West Light Foundation of the Chinese Academy of Sciences (2011, to Fan Dawei). Use of the National Synchrotron Light Source, Brookhaven National Laboratory, was supported by the U.S. Department of Energy, Office of Science, Office of Basic Energy Sciences, under Contract no. DE-AC02-98CH10886. The 4W2 High Pressure Station, Beijing Synchrotron Radiation Facility (BSRF), is supported by the Chinese Academy of Sciences (Grant nos. KJCX2-SW-N20, KJCX2-SW-N03).

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