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Pressure induced elastic softening in framework aluminosilicate- albite (NaAlSi3O8)

  • Scientific Reports 6, Article number: 34815 (2016)
  • doi:10.1038/srep34815
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Albite (NaAlSi3O8) is an aluminosilicate mineral. Its crystal structure consists of 3-D framework of Al and Si tetrahedral units. We have used Density Functional Theory to investigate the high-pressure behavior of the crystal structure and how it affects the elasticity of albite. Our results indicate elastic softening between 6–8 GPa. This is observed in all the individual elastic stiffness components. Our analysis indicates that the softening is due to the response of the three-dimensional tetrahedral framework, in particular by the pressure dependent changes in the tetrahedral tilts. At pressure <6 GPa, the PAW-GGA can be described by a Birch-Murnaghan equation of state with  = 687.4 Å3,  = 51.7 GPa, and  = 4.7. The shear modulus and its pressure derivative are  = 33.7 GPa, and  = 2.9. At 1 bar, the azimuthal compressional and shear wave anisotropy  = 42.8%, and  = 50.1%. We also investigate the densification of albite to a mixture of jadeite and quartz. The transformation is likely to cause a discontinuity in density, compressional, and shear wave velocity across the crust and mantle. This could partially account for the Mohorovicic discontinuity in thickened continental crustal regions.


Plagioclase feldspar is one of the most important mineral solid-solution series between the end-members- albite (NaAlSi3O8) and anorthite (CaAl2Si2O8). Plagioclase is ubiquitous in crustal rocks in the Earth and terrestrial planetary bodies, including Moon1. Sodic-plagiocase or albite is a major constituent of several rock types includinggranite, granodiorite, diorite, tonalite, and basalt. The modal abundances of plagioclase in these rocks vary between 16 and 60% 2. In hydrothermal ‘Kluftalbite’ veins the modal abundance of albite rich plagioclase could be nearly 100% 3. In subducted oceanic crust, albite is widely distributed in metamorphosed mid-ocean ridge basalt (MORB) i.e., zeolite to garnet granulite facies rocks with a modal abundance ranging between ~18–22% 4. Albitization is a common metasomatic process in granitic and mafic lithologies transforming Ca-bearing plagioclase to almost pure albite5. Albite is also abundant in unconsolidated sediments, either as detrital grains of various compositions or grows as authigenic crystals of pure albite6, and has been reported in oil shales associated with organic matter7.

Albite also occurs in wide variety of planetary materials including chondrites ~10% and Martian meteorites8,9. Sodic-plagioclase has also been identified in the exposed rocks and soils at several the landing sites of the Mars Exploration Rovers10 and as a widespread component of andesitic lava flows on the surface11. In addition, the Thermal Emission Spectrometer on the Global Surveyor spacecraft orbiting Mars have also identified sodic-plagicoclase as dust particles in the atmosphere12. There is also speculation that albite may be present on Mercury13,14.

To understand the dynamics of the planetary crust it is important to gain constraints on the physical properties of planetary crusts and its constituent rocks and minerals. Physical properties of plagioclase feldspar vary strongly as a function of chemistry between the albite and anorthite end-members. For instance, the elastic parameter such as bulk modulus increases by 60% from albite to anorthite15 whereas the transport properties such as viscosity vary over three orders of magnitude at constant temperature16. It is fundamental to address how the crystal structure and chemistry influences the physical property across the plagioclase solid solution. Albite also forms a solid solution with orthoclase (KAlSi3O8) i.e., the alkali feldspar solid solution series [(Na,K)AlSi3O8]. Albite is therefore the key model crystal structure for the aluminosilicate feldspar group of mineral. The crystal structure of albite consists of linked corner-sharing TO4 tetrahedral units (where T = Al, Si) forming a three- dimensional aluminosilicate framework, often referred to as crankshaft structure.

Despite being a major component in continental and oceanic crust and occurring in wide variety of Earth and planetary settings, our knowledge of fundamental physical properties, e.g. elasticity, of albite is rather limited. This is primarily owing to its complex crystal structure and triclinic space group symmetry. In a pioneering experimental study, ultrasonic velocities were measured for plagioclase single-crystals with 9–60 mol % of anorthite. Ultrasonic measurements at 1 bar and 298 K, in adequate directions of the single-crystals allowed for the determination of 13 independent elastic constants i.e., the elastic stiffness tensor with monoclinic rather than the true triclinic symmetry were determined17. The reported values were later revised, but still used monoclinic symmetry18. More recently, the full elastic tensor for albite19, plagioclase feldspars20, and alkali feldspars21 have been reported at ambient pressure and room temperature. In addition, room pressure elastic constants for plagioclase feldspar have also been predicted using ab initio methods22. With increasing depth in the crust, i.e., with increasing temperature and pressure, the crystal structure of albite becomes thermodynamically unstable, while denser mineral phases such as jadeite and quartz replace albite23. However, the transition to from albite to a mixture of jadeite and quartz also requires elevated temperatures. It is therefore likely that albite may persist as a metastable phase to greater depths24. Thus, it is important to know the pressure-dependence of this crystal structure and its physical properties, including elasticity. Several high-pressure studies have therefore been devoted to elucidating the crystal structure and compressibility24,25,26 of albite. These studies have indicated a pressure-induced softening of bulk moduli at around 6 GPa. We still do not have any understanding of how the full elastic stiffness tensor and the bulk and shear moduli change upon compression. In order to understand the elasticity and anisotropy of planetary crusts, we have performed first principles calculations of albite with triclinic symmetry at high-pressure. The equation of state and elastic parameters of albite feldspar at high-pressures will be of crucial importance for the thermodynamic database to predict phase relations and velocity discontinuities across crust and mantle27,28,29,30,31.


The compression behavior of the albite could be described with a Birch-Murnaghan equation of state32. The unit-cell volume and cell axes predicted with LDA and GGA bracket the previous X-ray diffraction results (Fig. 1). LDA typically overbinds, whereas the GGA under-binds, i.e., unit-cell volume data are slightly larger than the experimental results (Fig. 1). The inter-axial angles from our structural optimizations of albite using GGA are in excellent agreement with the previous X-ray diffraction studies26 (Fig. 1). The unit-cell volume predicted by GGA at 0 GPa shows  >  by ~3.4%, whereas unit-cell volume predicted by LDA shows  <  by ~4.0% (Table S1, Fig. 1). The bulk moduli predicted using GGA at 0 GPa shows  <  by ~1.1% whereas the bulk moduli predicted using LDA shows  >  by ~14.5% (Table S1, Fig. 1).

Figure 1: Pressure dependence of unit-cell volume and lattice parameters.
Figure 1

(a) unit-cell volume, (b) lattice parameters a, (c) b, (d) c-axes, angular lattice parameter (e) α, (f) β, and (g) γ as a function of pressure. ‘Red’ and ‘blue’ symbols represent LDA and GGA results. Experimental results are denoted by- ‘white’ symbols24, ‘light grey’ symbols25, and ‘dark grey’ symbols26.

Albite (triclinic symmetry) has 21 non-zero independent elastic constants, cij - three diagonal and compressional elastic stiffness components with, i = j, and i = 1–3; three diagonal and shear elastic stiffness components with i = j, and i = 4–6, and 15 off-diagonal elastic stiffness components with i ≠ j and i = 1–6 33. The agreement between the predicted elastic constants at room pressures from this study and previous experimental results are quite good19 (Fig. 2). For most of the components of full elastic moduli tensor, the experimental result at ambient condition is bracketed by the predictions based on LDA and GGA. The variation of elastic stiffness components with pressure can be explained with a finite-strain formulation29,34. Typically, the elastic moduli stiffen (i.e., ) upon compression, however, in the case of albite, most of the predicted elastic moduli based on LDA and GGA exhibit anomalous behavior, (i.e., ) between 4–6 and 6–8 GPa respectively (Fig. 2). The predicted anomalous behavior in the elastic parameters is in good agreement with the single-crystal X-ray diffraction study at high-pressure26. The compressional elastic moduli exhibit the relation, > c33 > c11, and the relation persists even at higher pressure. The off-diagonal longitudinal elastic moduli exhibit the relation > c12 > c23. The diagonal shear components of elastic moduli exhibit the relation c66 ≥ c55 > c44. While diagonal shear components c55 and c44 stiffen upon compression, c66 softens upon compression with . Additional off-diagonal components also exhibit anomalous behavior upon compression (Fig. 2, Table S2a,b). The predicted elastic moduli based on LDA are mostly stiffer than the GGA, i.e., .

Figure 2: Elastic constants as a function of pressure.
Figure 2

(a) Plot of the components of the full elastic stiffness tensor vs. pressure. There are three columns and seven rows, a total of 21 graphs, each representing the 21 components of the elastic constants. Each graph is labeled with the corresponding component. ‘Red’ and ‘blue’ symbols represent LDA and GGA results respectively. Experimental results are denoted by- ‘dark grey symbols’19. At high-pressures, both LDA and GGA results indicate the anomalous behavior of the elastic stiffness components.


The compressibility and elastic stiffness tensor of albite at high-pressure can be explained by the response of the alumino-silicate framework of tetrahedral units upon compression. In the albite crystal structure there are four distinct tetrahedral sites26,35, T1o, T1m, T2o and T2m (Fig. 3). The aluminum atoms occupy the T1o site based on neutron diffraction35 and subsequent empirical and DFT studies indicated that the energetics of Al ordered in T1o sites are of the order of 30 meV lower than T2o sites36. In a recent study, it has been noted that variation in Al/Si order and exact chemistry of alkali site (Na or K) has only minor effect on the aggregate elasticity21. However, elasticity varies significantly across Na-Ca plagioclase series22. Upon compression, both the AlO4 and SiO4 tetrahedral units remain mostly rigid. The GGA and LDA predictions for the polyhedral moduli for the T1o sites are,  = 155.49 and  = 166.36 respectively. The GGA predictions for the polyhedral moduli for the T1m, T2o, and T2m sites are,  = 270.9, 229.3 and 257.4 whereas the LDA predictions for the polyhedral moduli for the T1m, T2o, and T2m sites are  = 285.2, 204.3, 285.9 respectively. The pressure-induced compression in the aluminosilicate framework structure of albite is primarily accommodated by the gradual tilting and shearing of the cages formed by the tetrahedral units and is achieved by altering the T-O-T bond angles (Fig. 3; Supplementary Movies-1–4). In feldspar, four distinct tilts are recognized, i.e., ϕ1 to (Supplementary information). In triclinic albite, owing to lower symmetry, there are two distinct components for ϕ1 and ϕ2 tilts, i.e., ϕ1 is decomposed into ϕ1o and ϕ1m. Similarly the tilt ϕ2 is decomposed into ϕ2o and ϕ2m. In the present study all the tilt component shows anomalous behavior between 4–6 and 6–8 GPa for LDA and GGA respectively. This is a clear demonstration of the “cause and effect” relationship between the pressure dependent changes in the internal structure and the elasticity (Fig. 4). The flexibility of the alumino-silicate framework of tetrahedral unit results in significant anisotropy in elasticity. The a* direction in albite is significantly softer than the b* and c* direction.

Figure 3: Crystal structure of albite as a function of pressure.
Figure 3

(a) Representation of the chains of four membered AlO4 (light blue) and SiO4 (dark blue) tetrahedral units along the [001] showing the T-O-T linkages. Also, shown are the Na atoms (golden sphere) in the slice of albite structure (0.5 < y < 0.9). (b) Plot of the tetrahedral (TO4) framework, i.e., the T-O-T (T = Si, Al) linkage vs. pressure. LDA (light red), GGA (light blue), Experiments: white open symbols24 and grey26.

Figure 4: Tetrahedral tilts of albite as a function of pressure.
Figure 4

(a) for ϕ1 (b) ϕ2 (c) ϕ3 and (d) ϕ4 tilts. Inset shows the tetrahedral ring in various orientations. Also shown are the atoms with respective labels. All the tilts exhibit anomalous behavior upon compression. At 0 GPa, the tilts compare well with previous experiments37. For the visualization of the tilts and their definition, please refer to the supplementary information (Supplementary Movies, Supplementary Figure S1).

The pressure dependence of the P-wave velocity predicted from DFT is in very good agreement with previous measurements to pressures of 2.5 GPa37,38 (Fig. 5). Recent elasticity measurements predicts stiffer velocities for the b* and c* directions19 (Fig. 5). Although, the earlier work on feldspar megacrysts37,38 are “softer” relative to recent work19 in directions perpendicular to cleavage, i.e., b* and c* directions, the comparison is in better accord with the “true” single crystal behavior in the non-cleavage direction (100). It is likely that in the earlier experiments to determine the elastic constants38,39, the closing of the cracks at low-pressure lead to significantly greater pressure derivatives (Fig. 5). Agreement between all the previous experimental studies and present results are excellent for the softer a* direction. Substantial drop in compressional wave velocity, VP occur between 4 and 8 GPa for the a* and c* crystallographic directions. These correspond to the discontinuous behavior of the individual elastic constants, c11, and c33 (Fig. 2). The pressure dependence for shear elastic constants c44 and c66 also low values between 4 and 8 GPa, which would correspond to velocity drops for VS for propagation along a* and c* directions. Pressure-induced softening of the shear elastic constants have also been reported for the tetrahedraly coordinated silica (SiO2) polymorphs that shares corners and forms 3-D framework, as in quartz40,41,42,43,44 and coesite45,46.

Figure 5: Seismic velocity and elastic anisotropy at high pressure.
Figure 5

Compressional wave, VP propagation directions (a) [100], (b) (010), (c) (001). LDA and GGA results are represented by filled red and blue symbols. Experimentally measured VP as a function of pressure for albite (An5–8)38 (open white symbols) and oligoclase (An 10–30)39 (filled black symbols) to 1 and 2 GPa respectively. The recent experimental results20 are represented by filled grey symbol. The experimentally measured velocities38,39 are softer compared to the recent experiments20 for (010) and (001). (d) Bulk compressional wave VP and shear VS velocity as a function of pressure. For comparison, velocities for quartz51, a silicate framework mineral is also shown. (e) AVP, and (f) AVS as a function of pressure. Also shown are the experimentally determined elastic anisotropy for albite20 and quartz47.

The full elastic anisotropy compares quite well with recent experimental study19 and the DFT study22 (Fig. 5). The P-wave azimuthal anisotropy, AVP decreases from 43% at 1 bar to 34% at 8 GPa to, whereas the S-wave anisotropy AVS increases slightly from 46% at 1 bar to 49% at 8 GPa. At 1 bar, the anisotropy of P-wave to S-wave velocity ratios i.e., VP/VS1 and VP/VS2 are 68 and 59% respectively. Upon compression of albite to 8 GPa, the anisotropy in VP/VS1 and VP/VS2 reduces to 58 and 36% respectively.

The slight discrepancy elasticity and anisotropy between the previous DFT study and the present study is likely related to the differences in the computational parameters used. For instance, a higher energy cut-off of 800 eV is used in this study compared to 582 eV. In addition, the present study uses projector augmented wave method (Method section) as opposed to the pseudopotential method used in earlier DFT study22.

The Mohorovicic discontinuity (Moho) marks the first major discontinuity separating the earth’s crust from the underlying denser mantle. The discontinuity is likely to be related to the changes in composition across crust and underlying mantle48,49. Across Moho the rock type is likely to change from gabbro consisting of pyroxene and plagioclase minerals to eclogite consisting of denser omphacite pyroxene and garnet. Several mineralogical transformations play important role in eclogitization and the proportion of mineral phase changes gradually across the transition rendering a continuous change in density and physical properties49. In a recent study, it has been suggested that for the thickened continental crust, the Moho could, in part, be explained by the transformation of albite (ab) to a mixture of jadeite (jd) and quartz (qtz)50. In this study, we used elasticity results of albite (ab) from this study and recent studies19,26 and combined them with the recent elasticity results of jadeite (jd)51,52 and quartz (qtz)47 to evaluate the discontinuity in compressional velocity across the univariant transformation: NaAlSi3O8 (ab) = NaAlSi2O6 (jd) + SiO2 (qtz). We used a thermodynamic code, PerpleX28 and the thermodynamic database27 to predict the phase boundary and the changes in the physical properties such as density and P-, and S-wave velocity across the boundary (Fig. 6). In our analysis, the pressure derivatives of the velocities for albite i.e., and are from this study. The pressure derivatives of the velocities for jadeite51,52 and quartz60 are estimated from previous results. The temperature derivatives of the velocities i.e., and are derived from PerpleX28. We find that at a depth of around ~40 km, the average P- and S-wave velocity of mineral assemblage consisting of jadeite and quartz is ~1.0 km/s greater than that of albite (Fig. 6). This is also very similar to the known contrast between crust and the mantle. The weighted average crustal P-wave velocity across several continental crustal settings is ~6.45 (±0.2) km/s where as the underlying average mantle velocity is ~8.09 (±0.2) km/s61 has a similar velocity contrast across the crust-mantle discontinuity.

Figure 6: Albite transformation and geophysical discontinuity.
Figure 6

(a) Plot of density (ρ), (b) Plot of compressional velocity (VP), and (c) Plot of shear wave velocity (VS) as a function of pressure and temperature across the decomposition of albite (ab) to a mixture of jadeite (jd) and quartz (qtz). (d) Plot of bulk sound velocity (Vϕ) for various mineral phases stable in SiO2-NaAlO2 join, modified from53. Mineral abbreviations- qtz, coe, and st refers to quartz, coesite, and stishovite with SiO2 stoichiometry i.e., silica polymorphs; ab and na-holl refers to albite and sodium hollandite with same stoichiometry NaAlSi3O8; ne and na-cf refers to nepheline and sodium calcium ferrite structured phase with NaAlSiO4 stoichiometry and jd refers to jadeite with NaAlSi2O6 stoichiometry. Density and bulk modulus data are derived from- qtz47; coe54; st55; ab20,26, this study; na-holl56; ne57, na-cf58,59.

Alkali oxide-Na2O is a minor component in the deep Earth mineralogical model49, metasomatism in subduction zones by Na-rich fluids could stabilize jadeite rich rocks- jadeitites and albite rich rocks- albitite which occur together with serpentinite melange62,63,64. In the deep Earth, beyond the thermodynamic stability field of albite and jadeite, alkalis including sodium could be incorporated into denser mineral phases such as Na- hollandite and calcium ferrite (cf) structured phase with NaAlSiO4 stoichiometry53. Upon compression, a series of mineral transformation and densification is likely to modify albite to jadeite + quartz/coesite/stishovite and eventually to Na-holandite53. Similarly, jadeite could also be transformed to a mixture of NaAlSiO4 (cf phase) and stishovite57. Both hollandite and cf phases have crystal structure consisting of SiO6 and AlO6 units that forms tunnels where alkali atom such as Na and K reside49,65,66,67. The density and elasticity of sodium bearing phases including albite exhibit a positive correlation. Recent experimental studies have indicated that sodium could also be incorporated in ringwoodite68. How sodium is partitioned between major mantle minerals i.e., magnesium silicates and minor aluminosilicate at high pressure remains unknown and will be important to constrain the fate of sodium in the deep Earth.


We investigated albite using density functional theory (DFT)69,70,71 [Hohenberg and Kohn, 1964; Kohn and Sham, 1965]. DFT-based studies of the energetics, equation-of state, and elasticity have been widely used to examine condensed matter including minerals that are stable in the Earth’s interior75,76,77,78,79,80. We used the local density approximation (LDA) and the semi-local generalized gradient approximation (GGA)81,82,83. In addition, we also used the projector augmented wave method (PAW)84 within the Vienna ab initio simulation package (VASP)84,85,86,87. We used an energy cut-off Ecut ranging from 400 eV to 1100 eV and k-point sampling ranging from 2 to 46 k-points in the irreducible wedge of the Brillouin zone. We find that the results are fully converged at an energy cut-off Ecut of 800 eV and a 3 × 2 × 3 k-point mesh Monkhorst-Pack88 (Supplementary Figure S2). The total energies and pressures were converged to within 1.06 meV and 0.35 GPa. We used the experimentally determined crystal structure of albite from X-ray and neutron diffraction35 as the input for the crystal structure and the starting point for a full structural optimization of the crystal structure. We performed all the calculations in the primitive unit cell (Space group: , 52 atoms). The static (T = 0 K) calculation leads to primitive symmetry instead of the symmetry observed in experiments. For the determination of the elastic stiffness tensor, we strained the crystal structure and relaxed the internal degrees of freedom while preserving the symmetry of the crystal structure. The elastic constants cijkl were obtained by relating changes in stress with the applied strain, σij = ∑klcijklεkl. We applied ±1% strains to accurately determine the stresses in the limit of small strain (εkl → 0)29,34. The Cartesian frame for the elastic constants has X2 parallel to crystallographic axis b, X3 parallel to c*, and X1 normal to X2 and X3, forming a right-handed system for triclinic symmetry. We used the petrophysical software to determine the elastic anisotropy89. The P-wave and S-wave anisotropy are defined as and respectively.

Additional Information

How to cite this article: Mookherjee, M. et al. Pressure induced elastic softening in framework aluminosilicate- albite (NaAlSi3O8). Sci. Rep. 6, 34815; doi: 10.1038/srep34815 (2016).


  1. 1.

    & Planetary Crusts: Their Composition, Origin and Evolution 404 (Cambridge University Press, 2010).

  2. 2.

    Principles of Geochemistry (3rd edition) 329 (John Wiely & Sons, New York, 1966).

  3. 3.

    Feldspars 261 (John Wiley & Sons, New York 1969).

  4. 4.

    , & Subduction factory: 1. Theoretical mineralogy, densities, seismic wave speeds, and H2O contents. J. Geophys. Res. 108, 2029, 10.1029/2001JB001127 (2003).

  5. 5.

    , , & Albitization of granitic rocks: The mechanism of replacement of oligoclase by albite. Can. Mineral. 46, 1401–1415 (2008).

  6. 6.

    Textures and geochemistry of authigenic albite from Miocene sandstones, Louisiana Gulf Coast. J. Sediment. Res. 57, 353–362 (1987).

  7. 7.

    Authigenic albite in the Green River oil shales. J. Sediment. Res. 20, 227–230 (1950).

  8. 8.

    Feldspar in chondrites. Science 148, 943 (1965).

  9. 9.

    et al. A new Martian meteorite from Morocco: the nakhlite North West Africa 817. Earth Planet. Sci. Lett. 195, 223–238 (2002).

  10. 10.

    et al. Alkaline volcanic rocks from the Columbia Hills, Gusev crater, Mars, J. Geophys. Res. 111, E09S91, 10.1029/2006JE002698 (2006).

  11. 11.

    Global mineral distributions on Mars. J. Geophys. Res. 107, 9:1–20, 10.1029/2001JE001510 (2002).

  12. 12.

    & Bright and dark regions on Mars: particle size and mineralogical characteristics based on thermal emission spectrometer data. J. Geophys. Res. 107, 10/1–10/22 (2002).

  13. 13.

    , , & Mercury’s feldspar connection: mid-ir measurements suggest plagioclase. Adv. Space Res. 19, 1507–1510 (1997).

  14. 14.

    et al. Mercury: mid-infrared (3–13.5 mm) observations show heterogeneous composition, presence of intermediate and basic soil types, and pyroxene. Meteor. Planet. Sci. 37, 1255–1268 (2002).

  15. 15.

    Equation of state of plagioclase feldspars. Contrib. Min. Pet. 146, 506–512 (2003).

  16. 16.

    & Variation of viscosity with temperature and composition in the plagioclase system. Contrib. Mineral. Petrol. 90, 83–92 (1985).

  17. 17.

    Elastic properties of plagioclases. Akad. Nauk. SSSR Bull. Geophys. Ser. 7, 633–635 (1964).

  18. 18.

    et al. Velocities of elastic waves in minerals at atmospheric pressure and increasing precision of elastic constants by means of EVM Izv. Acad Sci USSR Geol. Ser. 10, 15–24 (1974).

  19. 19.

    , & Triclinic elastic constants for low albite, Phys. Chem. Mineral. 33, 256–265 (2006).

  20. 20.

    , & Elasticity of plagioclase feldspars, J. Geophys. Res. Solid Earth, 121, 10.1002/2015JB012736 (2016).

  21. 21.

    et al. The elastic tensor of monoclinic alkali feldspars. Am. Mineral. 101, 1228–1231, 10.2138/am-2016-5583 (2016).

  22. 22.

    , & Ab initio calculations of elastic constants of plagioclase feldspars. Am Mineral. 99, 2344–2352 (2014).

  23. 23.

    The reaction albite = jadeite + quartz determined experimentally in the range 600–1200 °C. Am. Mineral. 65, 129–134 (1980).

  24. 24.

    , & The high-pressure crystal chemistry of low albite and the origin of the pressure dependency of Al-Si ordering. Am. Mineral. 79, 1042–1052 (1994).

  25. 25.

    , , , & Comparative compressibility of end-member feldspars. Phys. Chem. Mineral. 15, 313–318 (1988).

  26. 26.

    , & Compression of albite, NaAlSi3O8. Am. Mineral. 90, 1115–1120 (2005).

  27. 27.

    & An internally consistent thermodynamic data set for phases of petrological interest. J. Met. Geo. 16, 309–343 (1998).

  28. 28.

    Computation of phase equilibria by linear programming: A took for geodynamic modeling and its application to subduction zone decarbonation. Earth Planet. Sci. Lett. 236, 524–541 (2005).

  29. 29.

    & Thermodynamics of mantle minerals-I. Physical properties. Geophys. J. Int. 162, 610–632 (2005).

  30. 30.

    & Thermodynamics of mantle minerals-II. Phase equilibria. Geophys. J. Int. 184, 1180–1213 (2011).

  31. 31.

    , & Effects of chemical composition, water and temperature on physical properties of continental crust, Geochem. Geophys. Geosyst. 16, 2431–2449 (2015).

  32. 32.

    Finite strain isotherm and velocities for single crystal and polycrystalline NaCl at high-pressures and 300 K. J. Geophys. Res. 83, 1257–1268 (1978).

  33. 33.

    Physical Properties of Crystals 329 (Oxford Science Publication, Clarendon Press, Oxford, UK, 1957).

  34. 34.

    , & Elastic properties of major materials of earth’s mantle from first principles. Rev. Geophys. 39, 507–534 (2001).

  35. 35.

    & Low albite: An X-ray and neutron diffraction study. Am. Mineral. 65, 986–995 (1980).

  36. 36.

    , & The ab initio study of the stability of low temperature Al/Si ordered albite, NaAlSi3O8. Am. Mineral. 85, 1681–1685 (2000).

  37. 37.

    Tilts and tetrahedral in feldspars. (In & ed. The Feldspars) 87–113 (Manchester United Press, Crane, Russak & Co. 1974).

  38. 38.

    Compressional wave velocities in single crystals of alkali feldspar at pressures to 10 kilobars. J. Geophys. Res. 71, 3113–3116 (1966).

  39. 39.

    Elastic parameters of feldspars and quartz at high pressures. Int. Geol. Rev. 19, 569–576 (1977).

  40. 40.

    & Elastic instability in α-quartz under pressure. Phys. Rev. Lett. 69, 2220–2223 (1992).

  41. 41.

    , , & New high-pressure transformation in α-quartz. Phys. Rev. Lett. 70, 3927 (1993).

  42. 42.

    , , & High-pressure elasticity of α-quartz: Instability and ferroelastic transition. Phys. Rev. Lett. 84, 3117 (2000).

  43. 43.

    & Comment on “High-pressure elasticity of α-quartz: Instability and ferroelastic transition” Phys. Rev. Lett. 90, 079701 (2003).

  44. 44.

    , , , & Gregoryanz et al. Reply. Phys. Rev. Lett. 90, 079702 (2003).

  45. 45.

    , & Hydrostatic compression and high-pressure elastic constants of coesite silica. J. App. Phys. 103, 053508 (2008).

  46. 46.

    et al. Anomalous elastic properties of coesite at high pressure and implications for the upper mantle X-discontinuity. Earth. Planet. Sci. Lett. 412, 42–51 (2015).

  47. 47.

    , , & Elasticity of single-crystal quartz to 10 GPa. Phys. Chem. Mineral. 42, 302–212 (2015).

  48. 48.

    & The nature of the Mohorovicic discontinuity. Ann. Rev. Earth Planet. Sci. 17, 475–506 (1989).

  49. 49.

    Composition and petrology of the Earth’s mantle 618 (McGraw-Hill International series in Earth and Planetary Sciences 1975).

  50. 50.

    & Foundering of lower island-arc crust as an explanation for the origin of the continental Moho. Nature, 504, 131–134 (2014).

  51. 51.

    et al. Thermoelastic equation of state of jadeite NaAlSi2O6: An energy dispersive Rietveld refinement study of low symmetry and multiple phase diffraction. Geophys. Res. Lett. 24, 5–8 (1997).

  52. 52.

    , The effect of pressure on the elastic properties and seismic anisotropy of diopside and jadeite from atomistic scale simulation. Phys Earth Planet. Int. 192–193, 81–89 (2012).

  53. 53.

    High-pressure phase transformations of albite, jadeite and nepheline. Earth Planet. Sci. Lett. 37, 438–444 (1978).

  54. 54.

    & Elasticity of coesite. J. Geophys. Res. 82, 1334–1346 (1977).

  55. 55.

    , , & The single- crystal elastic moduli of stishovite. J. Geophys. Res. 87, 4740–4746 (1982).

  56. 56.

    , , & High-pressure phase relations in the composition of albite NaAlSi3O8 constrained by an ab initio and quasi-harmonic Debye model, and their application. Earth Planet Sci. Lett. 298, 427–433 (2010).

  57. 57.

    Elasticity of minerals, glasses, and melts, (ed. ) 45–63 (In Mineral Physics and crystallography: a handbook of physical constants 1995).

  58. 58.

    Mid-mantle anisotropy: Elasticity of aluminous phase in subducted MORB. Geophys. Res. Lett. 38, L14302, 10.1029/2011GL047923 (2011).

  59. 59.

    , , & Energetics, equation of state, and elasticity of NAL phase: Potential host for alkali and aluminum in the lower mantle. Geophys. Res. Lett. 39, L19306, 10.1029/2012GL053682 (2012).

  60. 60.

    & Ab initio studies of phonon softening and high-pressure phase transitions of α-quartz SiO2. Phys. Rev. B. 73, 094304 (2006).

  61. 61.

    & Seismic velocity structure and composition of the continental crust: A global view. J. Geophys. Res. 100, 9761–9788 (1995).

  62. 62.

    , albitites and related rocks from the Montagua Fault zone, Guatemala. J. Met. Geol. 12, 42–68 (1994).

  63. 63.

    & Guatemala jadeitites and albitites were formed by deuterium-rich serpentinizing fluids deep within a subduction zone. Geology, 27, 629–632 (1999).

  64. 64.

    , & Jadeitites and plate tectonics. Ann. Rev. Earth Planet. Sci. 43, 105–138 (2015).

  65. 65.

    et al. Potential host phase of aluminium and potassium in the Earth’s mantle. Am. Mineral. 86, 740–746 (2001).

  66. 66.

    A possible new host mineral of large-ion elements in the Earth’s deep interior. American Geophysical Union Fall Meeting, DI11C-2599 (2015).

  67. 67.

    & Crystal structures of minerals in the lower mantle (ed. & ) 69–85 (Deep Earth: Physics and Chemistry of the lower mantle and core, Wiley 2016).

  68. 68.

    et al. Incorporation of high amounts of Na in ringwoodite: Possible implications for transport of alkali into lower mantle. Am. Mineral. 101, 483–486 (2016).

  69. 69.

    & Inhomogeneous Electron Gas. Phys. Rev. B 136, B864–B871 (1964).

  70. 70.

    & Self-Consistent Equations Including Exchange and Correlation Effects. Phys. Rev. 140, 1133–1138 (1965).

  71. 71.

    et al. Reproducibility in density functional theory calculations of solids. Science, 357, 10.1126/science.aad3000 (2016).

  72. 72.

    , & Ab initio theory of thermoelasticity and phase transitions in minerals. 4, 83–170 (Energy Modeling in Minerals, European Mineralogical Union Notes in Mineralogy 2002).

  73. 73.

    & Elasticity of phase-X at high pressure. Geophys Res. Lett. 36, L08307, 10.1029/2009GL037782 (2009).

  74. 74.

    & Detecting deeply subducted crust from the elasticity of hollandite. Earth Planet Sci. Lett. 288, 349–358, 10.1016/j.epsl.2009.09.037 (2009).

  75. 75.

    & Ab initio investigation of high-pressure phase relation and elasticity in the NaAlSi2O6 system. Geophys. Res. Lett. 37, L17302 (2010).

  76. 76.

    & Theoretical and computational methods in mineral physics: Geophysical applications. Rev. Mineral. Geochem. 71, 483 (2010).

  77. 77.

    High-pressure elasticity of sodium majorite garnet, Na2MgSi5O12. Am. Mineral. 99, 2416–2423 (2014).

  78. 78.

    & The perovskite to post-perovskite transition in CaIrO3: Clapeyron slope and changes in bulk and shear moduli by density functional theory. Phys. Earth Planet. Int. 164, 50–62 (2007).

  79. 79.

    , & Thermoelasticity of Fe3+ and Al-bearing bridgemanite: Effects of iron spin crossover. Geophys. Res. Lett. 43, 5661–5670 (2016).

  80. 80.

    , , & Modeling dislocation glide in Mg2SiO4 ringwoodite: Towards rheology under transition zone conditions. Phys. Earth Planet. Int. 248, 20–29 (2015).

  81. 81.

    & Accurate and simple density functional for the electronic exchange energy: Generalized gradient approximation. Phys. Rev. B 33, 8800–8802 (1986).

  82. 82.

    et al. Atoms, molecules, solids, and surfaces: Applications of the generalized gradient approximation for exchange and correlation. Phys. Rev. B 46, 6671–6687 (1991).

  83. 83.

    , & Generalized gradient approximation made simple. Phys. Rev. Lett. 77, 3865–3868 (1996).

  84. 84.

    & From ultrasoft pseudopotentials to the projector augmented-wave method. Phys. Rev. B 59, 1758–1775 (1999).

  85. 85.

    & Efficiency of ab-initio total energy calculations for metals and semiconductors using a plane-wave basis set. Comp. Mat. Sci. 6, 15–50 (1996).

  86. 86.

    & Efficient iterative schemes for ab initio total-energy calculations using a plane-wave basis set. Phys. Rev. B 54, 11169–11186 (1996).

  87. 87.

    & Ab initio Molecular-Dynamics for Liquid-Metals. Phys. Rev. B 47, 558–561 (1993).

  88. 88.

    & Special points for Brillouin-zone integrations. Phys. Rev. B 13, 5188–5192 (1976).

  89. 89.

    A fortran program to calculate seismic anisotropy from the lattice preferred orientation of minerals. Comp. Geosci. 16, 385–393 (1990).

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M.M. is currently supported by US-NSF EAR-1634422. M.M. and K.M. acknowledges computing resources from ALCF Mira Supercomputer through grant “ElasticEarthCrust”. The work by O.H. was supported in part by the US DOE, Office of Science under Contract No. DE-AC02-06CH11357. Authors thank the reviewers and associate editor for their constructive criticism that helped to enhance the clarity of the manuscript.

Author information


  1. Earth Materials Laboratory, Earth, Ocean and Atmospheric Sciences, Florida State University, Tallahassee, FL, 32310, USA

    • Mainak Mookherjee
    •  & Dhenu Patel
  2. Géosciences Montpellier UMR CNRS 5243, Université Montpellier, 34095, Montpellier, France

    • David Mainprice
  3. Center for Simulation and Modeling, University of Pittsburgh, Pittsburgh, PA, 15260, USA

    • Ketan Maheshwari
  4. Materials Science Division, Argonne National Laboratory, Argonne, IL 60439, USA

    • Olle Heinonen
  5. Earth and Atmospheric Sciences, Cornell University, NY 14850, USA

    • Anant Hariharan


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M.M. performed the calculations and the analysis. D.M. contributed towards the geophysical discussions. K.M. and O.H. also contributed towards the calculations. D.P., A.H. and M.M. analyzed the crystal structures. D.P. is a “summer” visiting scholar in the Earth Materials Lab, EOAS, FSU and is from Maclay School, Tallahassee, Fl. All authors discussed the results. M.M. took the lead in conceiving the project and writing the article, all authors contributed.

Competing interests

The authors declare no competing financial interests.

Corresponding author

Correspondence to Mainak Mookherjee.

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