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The lower mantle represents approximately 56% of the Earth's total volume and is located 660–2900 km below the Earth's surface in between the transition zone and the outer core.[1] The Preliminary reference Earth model (PREM) separates the lower mantle into three sections, the uppermost (660–770 km), mid-lower mantle (770–2700 km), and the D" layer (2700–2900 km).[2] Pressures and temperature at the lower mantle ranges from 24-127 GPa[2] and 1900-2600K.[3] It has been proposed that the composition of the lower mantle is pyrolitic[4] containing three major phases of bridgmanite, ferropericlase and calcium-silicate perovskite. The pressure conditions in the lower mantle was shown to induce a spin transition of iron-bearing bridgmanite and ferropericlase[5] which may affect both mantle plume dynamics[6][7] and lower mantle chemistry.[5]

Contents

Physical propertiesEdit

The lower mantle was initially labelled as the D-layer in Bullen's spherically symmetric model of the Earth.[8] The PREM seismic model of the Earth's interior separated the D-layer into three distinctive layers defined by the discontinuity in seismic wave velocities,[2]

  • 660–770 km: A discontinuity in compression wave velocity (6-11%) followed by a steep gradient is indicative of the transformation of the mineral ringwoodite to bridgmanite and ferropericlase and the transition between the transition zone layer to the lower mantle.
  • 770–2700 km: A gradual increase in velocity indicative of the adiabatic compression of the mineral phases at the lower mantle.
  • 2700–2900 km: The D" layer is considered the transition between the lower mantle to the outer core.

Temperatures of the lower mantle ranges from 1960 K at the topmost layer to 2630 K at a depth of 2700 km.[3] Models of the temperature of the lower mantle approximates convection as the primary heat transport contribution while conduction and radiative heat is considered negligible. As a result, the lower mantle's temperature gradient as a function of depth is approximately adiabatic.[1] Calculation of the geothermal gradient observed a decrease from 0.47 K/km at the uppermost lower mantle to 0.24 K/km at 2600 km.[3]

CompositionEdit

The lower mantle is mainly composed of three components, bridgmanite, ferropericlase and calcium-silicate perovskite (CaSiO3-perovskite). The proportion of each component has been a subject of discussion historically where the bulk composition is suggested to be,

  • Pyrolitic: derived from petrological composition trends from upper mantle peridotite suggesting homogeneity between the upper and lower mantle with a Mg/Si ratio of 1.27. This model implies that the lower mantle is composed of 75% bridgmanite, 17% ferropericlase and 8% CaSiO3-perovskite by volume.[4]
  • Chondritic: suggests that the Earth's lower mantle was accreted from composition of chondritic meteorite suggesting a Mg/Si ratio of approximately 1. This infers that bridgmanite and CaSiO3-perovskites are major components.

Laboratory multi-anvil compression experiments of pyrolite simulated conditions of the adiabatic geotherm and measured the density using in situ X-ray diffraction. It was shown that the density profile along the geotherm is in agreement with the PREM model.[9] First principle calculation of the density and velocity profile across the lower mantle geotherm of varying bridgmanite and ferropericlase proportion observed a match to the PREM model at an 8:2 proportion. This proportion is consistent with the pyrolitic bulk composition at the lower mantle.[10] Furthermore, shear wave velocity calculations of a pyrolitic lower mantle compositions considering minor elements resulted in a match with the PREM shear velocity profile within 1%.[11] On the other hand, Brillouin spectroscopic studies at relevant pressures and temperatures revealed that a lower mantle composed of greater than 93% bridgmanite phase has corresponding shear-wave velocities to measured seismic velocities. The suggested composition is consistent with a chondritic lower mantle.[12] Thus, the bulk composition of the lower mantle is currently a subject of discussion.

Spin transition zoneEdit

The electronic environment of two iron bearing minerals in the lower mantle (bridgmanite, ferropericlase) transitions from a high-spin (HS) to a low-spin (LS) state.[5] Fe2+ in ferropericlase undergoes the transition between 50-90 GPa. Bridgmanite contains both Fe3+ and Fe2+ in the structure, the Fe2+ occupy the A-site and transition to a LS state at 120 GPa. While Fe3+ occupy both A- and B-sites, the B-site Fe3+ undergoes HS to LS transition at 30-70 GPa while the A-site Fe3+ exchanges with the B-site Al3+ cation and becomes LS.[13] This spin transition of the iron cation results in the increase in partition coefficient between ferropericlase and bridgmanite to 10-14 depleting bridgmanite and enriching ferropericlase of Fe2+.[5] The HS to LS transition are reported to affect physical properties of the iron bearing minerals. For example, the density and incompressibility was reported to increase from HS to LS state in ferropericlase.[14] The effects of the spin transition on the transport properties and rheology of the lower mantle is currently being investigated and discussed using numerical simulations.

ReferencesEdit

  1. ^ a b Kaminsky, Felix V. (2017). The Earth's lower mantle : composition and structure. Cham: Springer. ISBN 9783319556840. OCLC 988167555.
  2. ^ a b c Dziewonski, Adam M.; Anderson, Don L. (1981). "Preliminary reference Earth model". Physics of the Earth and Planetary Interiors. 25 (4): 297–356. doi:10.1016/0031-9201(81)90046-7. ISSN 0031-9201.
  3. ^ a b c Katsura, Tomoo; Yoneda, Akira; Yamazaki, Daisuke; Yoshino, Takashi; Ito, Eiji (2010). "Adiabatic temperature profile in the mantle". Physics of the Earth and Planetary Interiors. 183 (1–2): 212–218. doi:10.1016/j.pepi.2010.07.001. ISSN 0031-9201.
  4. ^ a b Ringwood, Alfred E. (1976). Composition and petrology of the earth's mantle. McGraw-Hill. ISBN 0070529329. OCLC 16375050.
  5. ^ a b c d Badro, J. (2003-04-03). "Iron Partitioning in Earth's Mantle: Toward a Deep Lower Mantle Discontinuity". Science. 300 (5620): 789–791. doi:10.1126/science.1081311. ISSN 0036-8075.
  6. ^ Shahnas, M.H.; Pysklywec, R.N.; Justo, J.F.; Yuen, D.A. (2017-05-09). "Spin transition-induced anomalies in the lower mantle: implications for mid-mantle partial layering". Geophysical Journal International. 210 (2): 765–773. doi:10.1093/gji/ggx198. ISSN 0956-540X.
  7. ^ Bower, Dan J.; Gurnis, Michael; Jackson, Jennifer M.; Sturhahn, Wolfgang (2009-05-28). "Enhanced convection and fast plumes in the lower mantle induced by the spin transition in ferropericlase". Geophysical Research Letters. 36 (10). doi:10.1029/2009GL037706. ISSN 0094-8276.
  8. ^ Bullen, K.E. (1942). "The density variation of the earth's central core". Bulletin of the Seismological Society of America. 32: 19–29.
  9. ^ Irifune, T.; Shinmei, T.; McCammon, C. A.; Miyajima, N.; Rubie, D. C.; Frost, D. J. (2010-01-08). "Iron Partitioning and Density Changes of Pyrolite in Earth's Lower Mantle". Science. 327 (5962): 193–195. doi:10.1126/science.1181443. ISSN 0036-8075.
  10. ^ Wang, Xianlong; Tsuchiya, Taku; Hase, Atsushi (2015). "Computational support for a pyrolitic lower mantle containing ferric iron". Nature Geoscience. 8 (7): 556–559. doi:10.1038/ngeo2458. ISSN 1752-0894.
  11. ^ Hyung, Eugenia; Huang, Shichun; Petaev, Michail I.; Jacobsen, Stein B. (2016). "Is the mantle chemically stratified? Insights from sound velocity modeling and isotope evolution of an early magma ocean". Earth and Planetary Science Letters. 440: 158–168. doi:10.1016/j.epsl.2016.02.001.
  12. ^ Murakami, Motohiko; Ohishi, Yasuo; Hirao, Naohisa; Hirose, Kei (May 2012). "A perovskitic lower mantle inferred from high-pressure, high-temperature sound velocity data". Nature. 485 (7396): 90–94. doi:10.1038/nature11004. ISSN 0028-0836.
  13. ^ Badro, James (2014-05-30). "Spin Transitions in Mantle Minerals". Annual Review of Earth and Planetary Sciences. 42 (1): 231–248. doi:10.1146/annurev-earth-042711-105304. ISSN 0084-6597.
  14. ^ Lin, Jung-Fu; Speziale, Sergio; Mao, Zhu; Marquardt, Hauke (April 2013). "EFFECTS OF THE ELECTRONIC SPIN TRANSITIONS OF IRON IN LOWER MANTLE MINERALS: IMPLICATIONS FOR DEEP MANTLE GEOPHYSICS AND GEOCHEMISTRY: SPIN TRANSITION IN LOWER MANTLE". Reviews of Geophysics. 51 (2): 244–275. doi:10.1002/rog.20010.