Hydrogen mobility in transition zone silicates
 Razvan Caracas^{1}Email authorView ORCID ID profile and
 Wendy R. Panero^{2}
DOI: 10.1186/s4064501701198
© The Author(s). 2017
Received: 31 August 2016
Accepted: 27 February 2017
Published: 29 March 2017
Abstract
We study the hydrogen mobility in ringwoodite and wadsleyite considering multiple chargebalanced defects, including Mg < = > 2H, Si < = > Mg + 2H, and the hydrogarnet defect, Si < = > 4H, using molecular dynamics simulations based on the density functional theory at transition zone pressures and temperatures between 1500 and 2500 K. We determine the diffusion coefficients and study in detail the mechanism of hydrogen mobility during lengthy simulations. Our results show that temperature, water concentration, and defect mechanism have a significant effect on mobility. We find that the fastest diffusion is for the Mg < = > 2H defect, while H is more mobile when incorporated as Si < = > Mg + 2H than as hydrogarnet defects. The computed diffusivities for ringwoodite are larger than for wadsleyite: at 2000 K, diffusivity is 1.13 × 10^{−09} m^{2}/s for ringwoodite compared to 0.93 × 10^{−09} m^{2}/s for wadsleyite. In general, the hydrogen atoms spend on the order of tens of picoseconds or more trapped in or around the vacancy sites with net migration between sites over timescales of tens of femtoseconds. At 2500 K, some of these hydrogen excursions take place over several angstroms, while at 2000 K, they do not always result in net diffusion. At 1500 K, most of the defects fail to make excursions from their defect sites resulting in diffusion.
Keywords
Diffusion Transition zone Wadsleyite Ringwoodite Transport Electrical conductivity Defects HydrogenIntroduction
The incorporation of water in major mantle minerals affects the physical properties of these minerals, even with low concentrations of water. The introduction of water as hydrogen defects reduces seismic wave velocities (e.g., Jacobsen and Smyth 2006), enhances deformation (Kavner 2003), and increases electrical conductivity (Huang et al. 2005; Yoshino et al. 2009).
The transition zone is dominated by polymorphs of olivine, in which wadsleyite (I2/m) is stable from 410–520 km depth, transforming to ringwoodite (Fd3m), stable from 520–660 km depth. As synthesized in the laboratory, each of these polymorphs can store water in excess of 2 wt%, making them the primary focus for detecting water in the deep mantle. Wadsleyite incorporates hydrogen predominantly through Mg < = > 2H defects (Smyth et al. 1997) while ringwoodite accommodates hydrous defects through multiple defect mechanisms, dominated by the same Mg < = > 2H defect, but also with the hydrogarnet defect, Si < = > 4H, and minor Si < = > Mg + 2H (Panero 2010; Panero et al. 2013).
The amount of water actually stored in the transition zone, however, may be significantly less than the total capacity. While an inclusion of ringwoodite in diamond suggests that localized regions of hydrated ringwoodite are possible (Pearson et al. 2014), seismic velocity and phase boundaries (Houser 2016) and electrical conductivity of the transition zone are more consistent with a mantle significantly undersaturated in water.
Electrical conductivity of the Earth’s mantle varies significantly with depth and tectonic regime, including in the transition zone, in which the conductivity at the base of the transition zone is greater than the upper part of the transition zone (e.g., Kelbert et al. 2009; Shimizu et al. 2010). This variability is likely a complex function of temperature, composition (particularly H, Fe, and redox), and tectonic history. Indeed, the electrical conductivity of ringwoodite and wadsleyite vary as a function of water and iron content (e.g., Huang et al. 2005; Yoshino et al. 2009), with likely significant contributions from both proton and polaron conductivities. While disagreement remains as to the absolute values of conductivity in these materials, the electrical conductivity of hydrous ringwoodite is consistently found to be greater than hydrous wadsleyite for comparable water contents and experimental conditions but with different dependencies on absolute water content.
Direct measurements of hydrogen diffusivity in wadsleyite and ringwoodite under transition zone pressures and conditions are limited (Hae et al. 2006; Ohtani and Zhao 2009; Sun et al. 2015), in which these measurements include the complicating effects of iron that appears to enhance electrical conductivity through protonpolaron exchange mechanisms. The hydrogen diffusivity data are consistent with the electrical conductivity in which the H conductivity in ringwoodite exceeds that of wadsleyite.
We therefore calculate the diffusivity of hydrogen in ringwoodite at mantlerelevant conditions from ab initio molecular dynamics. While this is a wellestablished standard technique for melts and fluids (e.g., Tse 2002; Schweiger et al. 2008; Mookherjee et al. 2008), it is an unusual approach for solids due to the length of required calculations for appropriate statistics. For the latter, the large majority of the previous calculations (e.g., Bunson et al. 1999; Ammann et al. 2011) instead resolved to determine the activation energy along an assumed diffusion path, which combined with the concentration of vacancies, allowed to estimate the diffusion coefficients. Our approach is more daring: we insert hydrogen in the structures as defects in exchange for cations and obtain the selfdiffusion coefficients directly from long molecular dynamics simulations; consequently, we also capture the diffusion path.
With these considerations, we investigate in detail the mobility of hydrogen in ringwoodite as a function of temperature, defect mechanism, and defect geometry. We compare our results to calculations in wadsleyite and further consider the effects of shear and strain on wadsleyite. We also examine the pathway through which hydrogen diffuses to suggest the consequences of interactions with point defects and dislocations in hydrogen diffusivity. We estimate the effect of hydrogen on the electrical conductivity of the major minerals of the Earth’s transition zone through the NernstEinstein relation and assess the contribution of hydrogen to the measured mantle conductivity.
Methods/experimental
We perform firstprinciples molecular dynamics simulations. We allow the atoms to move in a crystal according to the Newtonian dynamics (molecular dynamics) under the action of interatomic forces computed within the density functional theory (DFT) (first principles). We use the planaraugmented wavefunction (PAW) formulation (Blochl 1994) of the DFT the VASP implementation (Kresse and Hafner 1993; Kresse and Joubert 1999) to compute the forces. The exchangecorrelation energy is expressed in the PerdewBurkeErnzerhof form (Perdew et al. 1996) of the generalized gradient approximation. We employ a 500 eV cutoff for the kinetic energy, 700 eV for the augmented cutoff, and the Γ point to sample the reciprocal space.
We use isokinetic NVT ensembles, where the velocity of the atoms is rescaled at each time step to fit the temperature, T, at fixed volume, V, and number of atoms, N, in the simulation box. The isokinetic NVT can be seen as an extreme version of the NoseHoover thermostat where the oscillation period of the temperature is set to the time step. We perform the simulations at volumes corresponding to transition zone pressures.
In all our calculations, we allow for long simulation times, between 70 and 200 ps at each condition with a time step of 1 fs. A 70 ps simulation requires the equivalent of about 500 processor days of computing time.
For ringwoodite, we consider several hydrogen incorporation mechanisms (Panero 2010): Mg^{2+} < = > 2H^{+}, Si^{4+} < = > Mg^{2+} + 2H^{+}, and the hydrogarnet substitution, Si^{4+} < = > 4H^{+}. We consider two different H/O atomic ratios per simulation cell: 1/32 and 2/32 each in two different geometries: a 2 × 1 × 1 supercell of the conventional cell and a 2 × 2 × 2 supercell of the primitive cell, with 16 Mg_{2}SiO_{4} formula units. The simulations are run at 1500, 2000, and 2500 K with the same initial specific volume of ringwoodite, corresponding to about 25 GPa. Temperature and the substitution mechanisms affect the actual pressure of the simulations, but in all cases, the pressure remains in an interval of about 23 to 33 GPa. Over this pressure range, we do not expect the values of the diffusivity to change significantly.
We compare the ringwoodite diffusivities to the Mg^{2+} < = > 2H^{+} defect on the M3 site in wadsleyite, the only active defect mechanism (Tsuchiya and Tsuchiya 2009), in a simulation box of one unit cell, or eight molecular units. To accelerate the diffusion, we also study the effect of strain. In order to compensate for the smaller simulation sizes, the simulation times of wadsleyite are longer, on the order of 100 ps.
Where r(t) is the position in threedimensional space at time, t. MSD is computed after an initial variable thermalization type of at least 2 ps, and tt _{ 0 } window glides over the entire remaining simulation time. Values less than ~1.0 × 10^{−10} m^{2}/s are an indication that the hydrogen atoms jump on a timescale similar to or greater than the total simulation time, and we include diffusivities for calculations only when the MSD is a linear function of time. Otherwise, we interpret that there are insufficient statistics to obtain reliable diffusion coefficients.
Where R is the gas constant and T is temperature in Kelvin.
Results and discussion
Calculations on Hbearing ringwoodite and wadsleyite
Defect  Mineral  H/O ratio  H_{2}O wt%  Geometry  P (GPa)  T (K)  D_{H} (10^{−9} m^{2}/s)  log(σ) (S/m) 

Mg < = > 2H  Rw  1/32  0.81  2 × 1 × 1 C  23.6  2000  0.569  0.03 
1/16  1.63  2 × 2 × 2 P  25.0  2000  1.132  −1.12  
1/16  1.63  2 × 1 × 1 C  24.7  2000  ^{a}  
1/32  0.81  2 × 2 × 2 P  25.1  2000  ^{a}  
1/32  0.81  2 × 2 × 2 P  25.1  2000  ^{a}  
1/32  0.81  2 × 1 × 1 C  27.1  2500  8.215  1.09  
1/16  1.63  2 × 1 × 1 C  26.8  2500  1.077  0.51  
1/32  0.81  2 × 2 × 2 P^{b}  27.0  2500  8.215  1.09  
1/32  0.81  2 × 2 × 2 P^{b}  27.0  2500  10.005  1.18  
1/16  1.63  2 × 2 × 2 P  26.7  2500  43.727  2.12  
Si <= > Mg + 2H  Rw  1/32  0.80  2 × 1 × 1 C  22.1  2000  0.217  −0.40 
1/16  1.60  2 × 1 × 1 C  24.6  2000  0.796  0.47  
1/32  0.80  2 × 1 × 1 C  30.3  2500  2.698  0.60  
1/16  1.60  2 × 1 × 1 C  26.6  2500  5.448  1.20  
Si < = > 4H  Rw  1/16  1.62  2 × 1 × 1 C  24.0  2000  0.077  −0.54 
1/8  3.27  2 × 1 × 1 C  25.2  2000  0.027  −0.70  
1/16  1.62  2 × 1 × 1 C  32.6  2500  0.263  −0.11  
1/8  3.27  2 × 1 × 1 C  27.0  2500  0.263  0.20  
Mg < = > 2H and Si < = > Mg + 2H  Rw  1/16  1.62  2 × 2 × 2 P  28.0  2000  0.452  0.23 
1/16  1.62  2 × 2 × 2 P  29.8  2500  0.74  0.35  
Mg < = > 2H  Wd  1/16  1.63  1 × 1 × 1  21.5  1500  0.024  −0.94 
1/16  1.63  1 × 1 × 1 5% strain  36.9  1500  0.003  −1.80  
1/16  1.63  1 × 1 × 1 7% shear  21.6  1500  0.107  −0.29  
1/16  1.63  1 × 1 × 1 11% shear  20.2  1500  0.617  0.47  
1/16  1.63  1 × 1 × 1  21.8  2000  0.926  0.52  
1/16  1.63  1 × 1 × 1  23.6  2500  88.43^{c}  2.41 
Hydrogen diffusivity
Defect  Mineral  H/O ratio  H_{2}O wt%  Geometry  D _{0}(m^{2}/s)  H (kJ/mol) 

Mg < = > 2H  R  1/16  1.63  2 × 2 × 2 P  9.73E02  303.8 
1/32  0.81  2 × 1 × 1 C  4.16E04  224.5  
Si < = > Mg + 2H  R  1/16  1.60  2 × 1 × 1 C  1.19E05  159.9 
1/32  0.80  2 × 1 × 1 C  6.44E05  209.5  
Si < = > 4H  R  1/8  1.62  2 × 1 × 1 C  5.05E04  260.9 
1/16  3.27  2 × 1 × 1 C  2.26E06  188.3  
Mg < = > 2H and Si < = > Mg + 2H  R  1/16  1.62  2 × 2 × 2 P  5.32E04  232.4 
Mg < = > 2H  W  1/16  1.63  1 × 1 × 1  5.62E05  183.2 
The hydrogen atoms typically spend several tens of picoseconds in one given cation vacancy site in between the diffusion jumps. The shape of their local trajectory depends on this site. Diffusion is realized in rapid (<100 fs) transfers between stable defect sites. During a time that is on the order of up to a tenth of a picosecond, the hydrogen atoms may undergo an excursion that can be up to several angstroms long. There are cases, especially at low temperature (1500 K) when the outcome of such an excursion is cut short and the atoms return to the initial cage. But at 2000 and 2500 K, most of these excursions result in a net displacement. This is the mechanism of the diffusion. The diffusion trajectory is a function of defect.
H migration in ringwoodite
Figure 2 shows a part of the trajectories of the four H atoms that substitute one Si atom for the Si < = > 4H defect. The H atoms remain around the initial vacancy. After 11 ps in the simulation one of them exits the vacancy, moves away around an O atom (Fig. 2) to be trapped in an empty adjacent octahedron, inside which it moves around describing a donut shape. Finally, the H atom undergoing the excursion falls back into a Si vacancy close to the other three hydrogen atoms but situated at a distance of one unit cell from the initial defect. During this time, it covers the equivalent net distance of one lattice parameter. The case analyzed here corresponds to one substituted Si in a 2 × 1 × 1 conventional supercell. As expected, the H diffuses along the shortest path, the y or zaxis. In Fig. 2b, c, it is clearly seen a diffusion pattern similar to a channel. An increase in temperature by 500 K leads to an increase in diffusion by more than one order of magnitude.
In case of the Si < = > Mg + 2H substitution, an excess Mg lies on the Si vacancy site; the H atoms are on the outer parts of the SiO_{6} tetrahedra. The pathway to initiate diffusion passes through an empty interoctahedral space. Not all H excursions result in net diffusion (Fig. 3) at 2000 K.
All Mg < = > 2H defects exchange H atoms during the course of the simulations; their diffusion paths follow not only the directions of the unit cell axis, as in the cases discussed above, but also along a diagonal.
H migration in wadsleyite
In wadsleyite, static calculations of H defects show that pairs of H in the Mg < = > 2H defect tend to align with the OH dipoles parallel to the zaxis (Tsuchiya and Tsuchiya 2009). In our dynamical simulations at the lowest temperatures in our simulations (1500 K), the H atoms explore the vacancy site, in trans positions. At 2000 K, they escape easily from their initial sites and wander around to realize a net diffusion.
At 2500 K and 23.6 GPa in wadsleyite (Table 1), MSD shows net displacements for all oxygen, silicon, and magnesium atoms in the structure, and therefore, we interpret that this calculation reflects a melt, consistent with the melting temperature of wadsleyite. The hydrogen diffusivity calculated in this simulation, 88.10^{−9} m^{2}/s, then reflects the diffusivity of H in a molten system. Our hydrogenbearing calculations show the presence of melt of lower temperatures than both previous freezing simulations on anhydrous liquid Mg_{2}SiO_{4} (De Koker et al. 2008) and recent static experimental data (Liebske and Frost 2012) consistent with meltingpoint depression for hydrated materials.
Energy considerations
Factors affecting diffusion rate: phase, substitution mechanism, concentration, and temperature
Consistently, lower hydrogen diffusivities are found in the other two defects. Hydrogen in the Si < = > Mg + 2H defect diffuse faster at each temperature than hydrogen in Si < = > 4H defects for all concentrations and supercell geometries calculated. Doubling the water content in each calculation changes the inferred hydrogen diffusivity by a factor of two but with opposite effect: it increases mobility of hydrogen associated with the Si < = > Mg + 2H defect yet decreases when associated with the Si < = > 4H defect.
The simulations with the combined Mg < = > 2H and Si < = > Mg + 2H defects yield diffusion coefficients that fall, as expected, between the equivalent concentration Mg < = > 2H calculations and the Si < = > Mg + 2H calculations. While each defect is active in ringwoodite, the Mg < = > 2H defect is dominant, particularly at concentrations below 1 wt% (Panero et al. 2013). Therefore, as the mechanism with both the greatest hydrogen diffusivity and greatest concentration, we consider the diffusivity of hydrogen in the Mg < = > 2H defect to control the diffusivity of hydrogen in ringwoodite.
The experimental hydrogen diffusion data for ringwoodite extrapolated to 2000 K falls in the middle of the range of values we obtained in our simulations (Ohtani and Zhao 2009; Sun et al. 2015). The inferred activation enthalpy in 2000–2500 K for ringwoodite in the fastest mechanism is 300 kJ/mol, significantly greater than the experimental value for ironbearing polycrystalline and singlecrystal ringwoodite, 140 and 101 kJ/mol, respectively. In contrast, the activation enthalpy in wadsleyite, 180 kJ/mol, is more similar to the polycrystalline, ironbearing experimental measurements in wadsleyite of 123 kJ/mol. The presence of iron, additional defects, or experimental strain may explain the difference. Our computed activation enthalpies are larger than the ones obtained from static simulations (Verma and Karki 2009), by almost one order of magnitude in case of ringwoodite. Table 2 lists the diffusivity fits to our computed diffusion coefficients.
For wadsleyite however, the extrapolated experimental data (Hae et al. 2006) are greater than our theoretical results. As with the Ohtani and Zhao (2009) data, these experiments are measured in an ironbearing polycrystalline sample, which may explain their faster diffusivities values.
At 2000 K, the H diffusion in wadsleyite for the Mg < = > 2H defect is 0.93 × 10^{−9} m^{2}/s. This is 16% less than the fastest value of 1.13 × 10^{−9} m^{2}/s computed for ringwoodite for the same defect and at the same temperature, consistent to the experimental hydrogen diffusivity data (Hae et al. 2006; Ohtani and Zhao 2009) (Table 1).
To explore if the discrepancies with previously published diffusivities as discussed above are due to lattice strain, we calculated the diffusion under various systems of strains applied to the wadsleyite structure at 1500 K. We found that a 5% uniaxial strain along the xaxis reduces the diffusivity by one order of magnitude according to the mean squaredisplacement analysis. However, as the values are already below 10^{−10} m^{2}/s, they do not show diffusion; rather, they reflect an enhancement of the H localization. When pure sheared is applied, the values increase by about one order of magnitude for 7% shear and almost two orders for 10% shear. It is only this last case where actual net hydrogen transfers between the lattice sites is observed. While large strain values are highly unlikely to exist in a natural setting, we show that residual strains in experiments may lead to an underestimate of diffusivity due to H localization.
Electrical conductivity of the transition zone
Finally, we use the NernstEinstein relation to obtain the electrical conductivity from the diffusion coefficients. The values are reported on the last column of Table 1. They correspond to diffusivity inside single crystals.
The last column of Table 1 lists the computed conductivities for each simulation. For ringwoodite, the highest values computed at 2500 K are on the order of 1.1 to 2.1 log(σ) (S/m). They correspond to the Mg < = > 2H defect that dominate the transport properties. Values at 2000 K are one order of magnitude lower. For wadsleyite, the computed log values of the conductivity are on the order of 0.5 log(σ) (S/m) at 2000 K.
Our values fall between the same order of magnitude down to two orders of magnitude below experimental values (Huang et al. 2005; Sun et al. 2015). This is most probably due to crystallinity: the diffusion along the grain boundaries plays a major role in the total transport. Measurements on real crystals show values order of magnitude higher as obtained for single crystal (Sun et al. 2015) than polycrystalline samples (Ohtani and Zhao 2009).
We conclude from our suite of calculations in ringwoodite that increased concentration of defects significantly enhances proton migration in the crystal, consistent with the concentrationdependent electrical conductivity (Huang et al. 2005). We find that hydrogen clearly rests in chargeneutral defect sites within the crystal for the majority of the simulation time, and therefore, it is the increased density of defects that leads to an increased conductivity through shortened hopping distance for the hydrogen. As with any diffusionlimited processes, the proton conductivity will be dominated by the fastest diffusing species, which in the case of ringwoodite, is the hydrogen atoms associated with the dominant Mg < = > 2H defect.
We find that the associated inferred conductivity of ringwoodite is greater than that of wadsleyite at realistic mantle conditions. The computed values of the conductivity and the difference between ringwoodite and wadsleyite are fully consistent with an increase in conductivity at the base of the Earth’s mantle (Kelbert et al. 2009; Shimizu et al. 2010) and may help signal the presence of significant (~1 wt%) water in the transition zone.
Conclusions
We study the main three mechanisms of incorporating hydrogen into the ringwoodite structure via chemical substitutions: Mg < = > 2H, Si < = > Mg + 2H, and the hydrogarnet defect, Si < = > 4H. We perform firstprinciples molecular dynamics simulations lasting up to a couple hundred picoseconds. Three Mg < = > 2H calculations at 2000 K did not yield sufficient migration statistics to results in a reliable diffusivity in 200 ps of simulation time, which highlights that the starting conditions and the thermal history of the calculations may play a factor in the quantitative results.
We find that temperature and defect concentration increase the rate of the H diffusion. More isometric geometries, like the 2 × 2 × 2 primitive supercell also show faster diffusion than more anisotropic, like the 2 × 1 × 1 conventional supercell, similar to the reduction of diffusivity found in wadsleyite for 5% strain. We find that the Mg < = > 2H defect mechanism yields the greatest H diffusion rates, with the hydrogarnet substitution, Si < = > 4H, showing the slowest diffusion.
During the simulation time of several tens of picoseconds, the H atoms travel over several lattice sites. However, during their path, they spend a considerable amount of time pinned in the defect sites. The diffusion is realized via jumps between the vacancy sites; during these jumps, the hydrogen atoms move around the neighboring O atoms, such as to continuously form OH bonds. They try to avoid at all cost the Mg cations, which are also positively charged; usually they stay in the void octahedral space. There is no obvious relation in the energy fluctuations during the simulations and the positions of the hydrogen atoms in the lattice—be they in the vacancy sites or during the diffusive jumps.
The Mg < = > 2H defects are more mobile in ringwoodite than wadsleyite. This result agrees with the proton conductivity inferences of Yoshino et al. (2009) and Huang et al. (2005), as well as the observed increase in electrical conductivity with depth through the transition zone (e.g., Khan et al. 2011; Olsen 1998).
Notes
Abbreviations
 MSD:

Mean square displacements
Declarations
Acknowledgements
The calculations were performed on the ADA machine at the IDRIS Supercomputing Center, France, under eDARI grant x2016106368.
Funding
RC was funded by the Extreme Physics and Chemistry directorate of the Deep Carbon Observatory. WRP was funded by NSF via grant EAR 0955647.
Authors’ contributions
RC and WRP proposed the topic, conceived and designed the study, analyzed the data, and constructed the manuscript. RC ran the calculations. Both authors read and approved the final manuscript.
Competing interests
The authors declare that they have no competing interests.
Open AccessThis article is distributed under the terms of the Creative Commons Attribution 4.0 International License (http://creativecommons.org/licenses/by/4.0/), which permits unrestricted use, distribution, and reproduction in any medium, provided you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made.
Authors’ Affiliations
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