laser heated diamond anvil cell experiments

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Published: 13 November 2023

A hydrogen-enriched layer in the topmost outer core sourced from deeply subducted water

Taehyun Kim ORCID: orcid.org/0000-0003-1950-6258 1 , 2 ,
Joseph G. O’Rourke ORCID: orcid.org/0000-0002-1180-996X 2 ,
Jeongmin Lee ORCID: orcid.org/0000-0001-7712-9919 1 ,
Stella Chariton 3 ,
Vitali Prakapenka 3 ,
Rachel J. Husband 4 ,
Nico Giordano ORCID: orcid.org/0000-0001-9518-1251 4 ,
Hanns-Peter Liermann ORCID: orcid.org/0000-0001-5039-1183 4 ,
Sang-Heon Shim ORCID: orcid.org/0000-0001-5203-6038 2 &
Yongjae Lee ORCID: orcid.org/0000-0002-2043-0804 1

Nature Geoscience volume 16 , pages 1208–1214 ( 2023 ) Cite this article

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Core processes
Geodynamics

The Earth’s core–mantle boundary presents a dramatic change in materials, from silicate to metal. While little is known about chemical interactions between them, a thin layer with a lower velocity has been proposed at the topmost outer core (Eʹ layer) that is difficult to explain with a change in concentration of a single light element. Here we perform high-temperature and -pressure laser-heated diamond-anvil cell experiments and report the formation of SiO 2 and FeH x from a reaction between water from hydrous minerals and Fe–Si alloys at the pressure–temperature conditions relevant to the Earth’s core–mantle boundary. We suggest that, if water has been delivered to the core–mantle boundary by subduction, this reaction could enable exchange of hydrogen and silicon between the mantle and the core. The resulting H-rich, Si-deficient layer formed at the topmost core would have a lower density, stabilizing chemical stratification at the top of the core, and a lower velocity. We suggest that such chemical exchange between the core and mantle over gigayears of deep transport of water may have contributed to the formation of the putative Eʹ layer.

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laser heated diamond anvil cell experiments

Pressure stabilizes ferrous iron in bridgmanite under hydrous deep lower mantle conditions

The Earth’s core as a reservoir of water

Superionic iron oxide–hydroxide in Earth’s deep mantle

Data availability.

All data supporting this study are available at https://zenodo.org/record/8404634 or by contacting the corresponding authors.

Code availability

Codes to reproduce the results are available at https://zenodo.org/record/6383505#.Yj1acE3P1D8 .

Dziewonski, A. M. & Anderson, D. L. Preliminary reference Earth model. Phys. Earth Planet. Inter. 25 , 297–356 (1981).

Article Google Scholar

Hirose, K. et al. Composition and state of the core. Annu. Rev. Earth Planet. Sci. 41 , 657–691 (2013).

Badro, J. et al. A seismologically consistent compositional model of Earth’s core. Proc. Natl Acad. Sci. USA. 111 , 7542–7545 (2014).

Rubie, D. C. et al. Accretion and differentiation of the terrestrial planets with implications for the compositions of early-formed Solar System bodies and accretion of water. Icarus 248 , 89–108 (2015).

Nakajima, Y. et al. Silicon-depleted present-day Earth’s outer core revealed by sound velocity measurements of liquid Fe–Si alloy. J. Geophys. Res. Solid Earth 125 , e2020JB019399 (2020).

Badding, J. V. et al. High-pressure chemistry of hydrogen in metals: in situ study of iron hydride. Science 253 , 421–424 (1991).

Tagawa, S. et al. Experimental evidence for hydrogen incorporation into Earth’s core. Nat. Commun. 12 , 2588 (2021).

Holland, G. & Ballentine, C. J. Seawater subduction controls the heavy noble gas composition of the mantle. Nature 441 , 186–191 (2006).

Martin, H. Effect of steeper Archean geothermal gradient on geochemistry of subduction-zone magmas. Geology 14 , 753–756 (1986).

van Hunen, J. & Moyen, J.-F. Archean subduction: fact or fiction? Annu. Rev. Earth Planet. Sci. 40 , 195–219 (2012).

Bekaert, D. V. et al. Subduction-driven volatile recycling: a global mass balance. Annu. Rev. Earth Planet. Sci. 49 , 37–70 (2021).

van Keken, P. E. et al. Subduction factory: 4. Depth-dependent flux of H 2 O from subducting slabs worldwide. J. Geophys. Res. 116 , B01401 (2011).

Google Scholar

Pamato, M. G. et al. Lower-mantle water reservoir implied by the extreme stability of a hydrous aluminosilicate. Nat. Geosci. 8 , 75–79 (2015).

Nishi, M. et al. The pyrite-type high-pressure form of FeOOH. Nature 547 , 205–208 (2017).

Nishi, M. et al. Stability of hydrous silicate at high pressures and water transport to the deep lower mantle. Nat. Geosci. 7 , 224–227 (2014).

Lin, Y. et al. Evidence for the stability of ultrahydrous stishovite in Earth’s lower mantle. Proc. Natl Acad. Sci. USA 117 , 184–189 (2020).

Niu, Y. Origin of the LLSVPs at the base of the mantle is a consequence of plate tectonics – a petrological and geochemical perspective. Geosci. Front. 9 , 1265–1278 (2018).

Sun, D. et al. Slab control on the northeastern edge of the mid-Pacific LLSVP near Hawaii. Geophys. Res. Lett. 46 , 3142–3152 (2019).

Piet, H. et al. Dehydration of δ-AlOOH in Earth’s deep lower mantle. Minerals 10 , 348 (2020).

Yuan, K. & Romanowicz, B. Seismic evidence for partial melting at the root of major hot spot plumes. Science 357 , 393–397 (2017).

Brandenburg, J. P. & van Keken, P. E. Deep storage of oceanic crust in a vigorously convecting mantle. J. Geophys. Res. 112 , B06403 (2007).

Manga, M. & Jeanloz, R. Implications of a metal-bearing chemical boundary layer in D″ for mantle dynamics. Geophys. Res. Lett. 23 , 3091–3094 (1996).

Li, M. et al. Compositionally-distinct ultra-low velocity zones on Earth’s core–mantle boundary. Nat. Commun. 8 , 177 (2017).

Garnero, E. J. et al. Constraining outermost core velocity with SmKS waves. Geophys. Res. Lett. 20 , 2463–2466 (1993).

Ma, X. & Tkalčić, H. CCMOC: a new view of the Earth’s outer core through the global coda correlation wavefield. Phys. Earth Planet. Inter. 334 , 106957 (2023).

Irving, J. C. E. et al. Seismically determined elastic parameters for Earth’s outer core. Sci. Adv. 4 , eaar2538 (2018).

van Tent, R. et al. The signal of outermost-core stratification in body-wave and normal-mode data. Geophys. J. Int. 223 , 1338–1354 (2020).

Labrosse, S. et al. A crystallizing dense magma ocean at the base of the Earth’s mantle. Nature 450 , 866–869 (2007).

Davies, C. J. et al. Transfer of oxygen to Earth’s core from a long-lived magma ocean. Earth Planet. Sci. Lett. 538 , 116208 (2020).

Brodholt, J. & Badro, J. Composition of the low seismic velocity Eʹ layer at the top of Earth’s core. Geophys. Res. Lett. 44 , 8303–8310 (2017).

Grocholski, B. et al. Stability, metastability, and elastic properties of a dense silica polymorph, seifertite. J. Geophys. Res. Solid Earth 118 , 4745–4757 (2013).

Tateno, S. et al. Determination of post-perovskite phase transition boundary up to 4400 K and implications for thermal structure in D″ layer. Earth Planet. Sci. Lett. 277 , 130–136 (2009).

Nisr, C. et al. Large H 2 O solubility in dense silica and its implications for the interiors of water-rich planets. Proc. Natl Acad. Sci. USA 117 , 9747–9754 (2020).

Liu, L. et al. Formation of an Al-rich niccolite-type silica in subducted oceanic crust: implications for water transport to the deep lower mantle. Geophys. Res. Lett. 49 , e2021GL097178 (2022).

Pépin, C. M. et al. New iron hydrides under high pressure. Phys. Rev. Lett. 113 , 265504 (2014).

Kato, C. et al. Stability of fcc phase FeH to 137 GPa. Am. Mineral. 105 , 917–921 (2020).

Hirose, K. et al. Hydrogen limits carbon in liquid iron. Geophys. Res. Lett. 46 , 5190–5197 (2019).

Piet, H. et al. Superstoichiometric alloying of H and close-packed Fe–Ni metal under high pressures: implications for hydrogen storage in planetary core. Geophys. Res. Lett. 50 , e2022GL101155 (2023).

Okuchi, T. Hydrogen partitioning into molten iron at high pressure: implications for Earth’s core. Science 278 , 1781–1784 (1997).

Iizuka-Oku, R. et al. Hydrogenation of iron in the early stage of Earth’s evolution. Nat. Commun. 8 , 14096 (2017).

Frost, D. J. & McCammon, C. A. The redox state of Earth’s mantle. Annu. Rev. Earth Planet. Sci. 36 , 389–420 (2008).

Walter, M. J. Water transport to the core–mantle boundary. Natl Sci. Rev. 8 , nwab007 (2021).

Bouffard, M. et al. Convective erosion of a primordial stratification atop Earth’s core. Geophys. Res. Lett. 47 , e2020GL087109 (2020).

Helffrich, G. & Kaneshima, S. Outer-core compositional stratification from observed core wave speed profiles. Nature 468 , 807–810 (2010).

Olson, P. et al. Outer core stratification from the high latitude structure of the geomagnetic field. Front. Earth Sci. 6 , 140 (2018).

Buffett, B. Geomagnetic fluctuations reveal stable stratification at the top of the Earth’s core. Nature 507 , 484–487 (2014).

Yan, C. & Stanley, S. Sensitivity of the geomagnetic octupole to a stably stratified layer in the Earth’s core. Geophys. Res. Lett. 45 , 11005–11011 (2018).

Christensen, U. R. Geodynamo models with a stable layer and heterogeneous heat flow at the top of the core. Geophys. J. Int. 215 , 1338–1351 (2018).

Umemoto, K. & Hirose, K. Chemical compositions of the outer core examined by first principles calculations. Earth Planet. Sci. Lett. 531 , 116009 (2020).

Buffett, B. et al. Evidence for MAC waves at the top of Earth’s core and implications for variations in length of day. Geophys. J. Int. 204 , 1789–1800 (2016).

Umemoto, K. & Hirose, K. Liquid iron–hydrogen alloys at outer core conditions by first-principles calculations. Geophys. Res. Lett. 42 , 7513–7520 (2015).

Fu, S. et al. Hydrogen and silicon effects on hexagonal close packed Fe alloys at high pressures: implications for the composition of Earth’s inner core. J. Geophys. Res. Solid Earth 128 , e2022JB026016 (2023).

Kaneshima, S. & Helffrich, G. Vp structure of the outermost core derived from analysing large-scale array data of SmKS waves. Geophys. J. Int. 193 , 1537–1555 (2013).

Tang, V. et al. Seismological evidence for a non-monotonic velocity gradient in the topmost outer core. Sci. Rep. 5 , 8613 (2015).

Mittal, T. et al. Precipitation of multiple light elements to power Earth’s early dynamo. Earth Planet. Sci. Lett. 532 , 116030 (2020).

Nakagawa, T. On the thermo-chemical origin of the stratified region at the top of the Earth’s core. Phys. Earth Planet. Inter. 276 , 172–181 (2018).

Mound, J. et al. Regional stratification at the top of Earth’s core due to core–mantle boundary heat flux variations. Nat. Geosci. 12 , 575–580 (2019).

Yokoo, S. et al. Stratification in planetary cores by liquid immiscibility in Fe–S–H. Nat. Commun. 13 , 644 (2022).

Ono, S. Experimental constraints on the temperature profile in the lower mantle. Phys. Earth Planet. Inter. 170 , 267–273 (2008).

Morard, G. et al. Melting of Fe–Ni–Si and Fe–Ni–S alloys at megabar pressures: implications for the core–mantle boundary temperature. Phys. Chem. Miner. 38 , 767–776 (2011).

Nomura, R. et al. Low core–mantle boundary temperature inferred from the solidus of pyrolite. Science 343 , 522–525 (2014).

McKelvy, M. J. et al. Exploration of the role of heat activation in enhancing serpentine carbon sequestration reactions. Environ. Sci. Technol. 38 , 6897–6903 (2004).

Deschamps, F. et al. Geochemistry of subduction zone serpentinites: a review. Lithos 178 , 96–127 (2013).

Prakapenka, V. B. et al. Advanced flat top laser heating system for high pressure research at GSECARS: application to the melting behavior of germanium. High Press. Res. 28 , 225–235 (2008).

Liermann, H.-P. et al. The Extreme Conditions Beamline P02.2 and the Extreme Conditions Science Infrastructure at PETRA III. J. Synchrotron Rad. 22 , 908–924 (2015).

Konôpková, Z. et al. Laser heating system at the Extreme Conditions Beamline, P02.2, PETRA III. J. Synchrotron Rad. 28 , 1747–1757 (2021).

Boehler, R. High-pressure experiments and the phase diagram of lower mantle and core materials. Rev. Geophys. 38 , 221–245 (2000).

Shen, G. et al. Laser heated diamond cell system at the Advanced Photon Source for in situ X-ray measurements at high pressure and temperature. Rev. Sci. Instrum. 72 , 1273–1282 (2001).

Benedetti, L. R. & Loubeyre, P. Temperature gradients, wavelength-dependent emissivity, and accuracy of high and very-high temperatures measured in the laser-heated diamond cell. High Press. Res. 24 , 423–445 (2004).

Prescher, C. & Prakapenka, V. B. DIOPTAS: a program for reduction of two-dimensional X-ray diffraction data and data exploration. High Press. Res. 35 , 223–230 (2015).

Dorogokupets, P. I. & Dewaele, A. Equations of state of MgO, Au, Pt, NaCl-B1, and NaCl-B2: internally consistent high-temperature pressure scales. High Press. Res. 27 , 431–446 (2007).

Shim, S.-H. PeakPo - a Python software for X-ray diffraction analysis at high pressure and high temperature. Zenodo https://doi.org/10.5281/zenodo.810200 (2017).

Gessmann, C. K. et al. Oxygen fugacity dependence of Ni, Co, Mn, Cr, V, and Si partitioning between liquid metal and magnesiowüstite at 9–18 GPa and 2200 °C. Geochim. Cosmochim. Acta 63 , 1853–1863 (1999).

Walter, M. J. et al. The stability of hydrous silicates in Earth’s lower mantle: experimental constraints from the systems MgO–SiO 2 –H 2 O and MgO–Al 2 O 3 –SiO 2 –H 2 O. Chem. Geol. 418 , 16–29 (2015).

Righter, K. et al. Redox processes in early Earth accretion and in terrestrial bodies. Elements 16 , 161–166 (2020).

Vogel, A. K. et al. The dependence of metal–silicate partitioning of moderately volatile elements on oxygen fugacity and Si contents of Fe metal: implications for their valence states in silicate liquids. Geochim. Cosmochim. Acta 237 , 275–293 (2018).

Robie, R. A. et al. Thermodynamic properties of minerals and related substances at 298.15 K and 1 bar (10 5 Pascals) pressure and at higher temperatures. U. S. Geol. Surv. Bull. 1452 , 298–310 (1978).

Dewaele, A. et al. Quasihydrostatic equation of state of iron above 2 Mbar. Phys. Rev. Lett. 97 , 215504 (2006).

Dobson, D. P. et al. The equation of state of CsCl-structured FeSi to 40 GPa: implications for silicon in the Earth’s core. Geophys. Res. Lett. 30 , 2002GL016228 (2003).

Sata, N. et al. Compression of FeSi, Fe 3 C, Fe 0.95 O, and FeS under the core pressures and implication for light element in the Earth’s core. J. Geophys. Res. 115 , B09204 (2010).

Geballe, Z. M. & Jeanloz, R. Solid phases of FeSi to 47 GPa and 2800 K: new data. Am. Mineral. 99 , 720–723 (2014).

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Acknowledgements

Y.L., T.K. and J.L. were supported by the Leader Researcher programme (NRF-2018R1A3B1052042) of the Korean Ministry of Science and ICT (MSICT). S.-H.S. and T.K. were supported by NSF grants EAR1338810, EAR2019565 and AST2108129. They were also supported by National Aeronautics and Space Administration (NASA) grant 80NSSC18K0353. S.-H.S. also benefited from collaborations and information exchange within the Nexus for Exoplanet System Science (NExSS) research coordination network sponsored by NASA’s Science Mission Directorate. This research used resources of the Advanced Photon Source, a US Department of Energy (DOE) Office of Science User Facility operated for the DOE Office of Science by Argonne National Laboratory under contract no. DE-AC02-06CH11357. We acknowledge the support of GSECARS (Sector 13), which is supported by the National Science Foundation—Earth Sciences (EAR-1634415), and the Department of Energy, Geosciences (DE-FG02-94ER14466). Parts of this research were carried out at the P02.2 beamline at PETRA III, and we acknowledge Deutsches Elektronen-Synchrotron (DESY, Hamburg, Germany), a member of the Helmholtz Association HGF, for the provision of experimental facilities. We also acknowledge the scientific exchange and support of the Center for Molecular Water Science (CMWS) at DESY. We acknowledge resources and support from the Goldwater Environmental Laboratory, part of the Chemical and Environmental Core Facilities at Arizona State University (ASU). We also thank A. Chizmeshya at ASU for providing the synthetic lizardite.

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Department of Earth System Sciences, Yonsei University, Seoul, South Korea

Taehyun Kim, Jeongmin Lee & Yongjae Lee

School of Earth and Space Exploration, Arizona State University, Tempe, AZ, USA

Taehyun Kim, Joseph G. O’Rourke & Sang-Heon Shim

Center for Advanced Radiation Sources, University of Chicago, Argonne, IL, USA

Stella Chariton & Vitali Prakapenka

Deutsches Elektronen-Synchrotron (DESY), Hamburg, Germany

Rachel J. Husband, Nico Giordano & Hanns-Peter Liermann

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Contributions

T.K., J.L. and S.-H.S. performed the experiments, and T.K. analysed the X-ray diffraction, SEM, TEM and EDS data. S.C., V.P., R.J.H., N.G. and H.-P.L. supported synchrotron beamline setups and operations. J.G.O. performed the calculations. Y.L. and S.-H.S. supervised the research, discussed the results with T.K. and worked on the manuscript with all authors.

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Correspondence to Sang-Heon Shim or Yongjae Lee .

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The authors declare no competing interests.

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Nature Geoscience thanks Riko Iizuka-Oku and the other, anonymous, reviewer(s) for their contribution to the peer review of this work. Primary Handling Editors: Alison Hunt and Louise Hawkins, in collaboration with the Nature Geoscience team.

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Extended data

Extended data fig. 1 x-ray diffraction patterns showing the reaction products from a, fesi in a h 2 o medium (setup 1), b, fe-9wt%si sandwiched between hydrous silicate layers (setup 5), and c, fe-9wt%si sandwiched between hydrous aluminous silicate layers (setup 6)..

X-ray diffraction patterns were collected (a) at 32 GPa and 1282 K (A30A_14), and (b) after temperature quenching from 3040 K at 62 GPa (A15H_18), and (c) at 111 GPa and 3550 K (A15I_29). The X-ray energy was 30 keV for (a) and 37 keV for (b) and (c). The vertical colour bars indicate the positions of the diffraction peaks from the identified phases. The background feature indicated by a double-sided grey arrow in low two-theta region in patterns (b) and (c) is from laser carbon mirrors.

Extended Data Fig. 2 In situ X-ray diffraction patterns measured during laser heating (a, 60 GPa and 3601 K (A30B_36), b, 137 GPa and 3700 K (A15G_28), and c, 68 GPa and 4100 K (A15H_26)) and after temperature quenching (44 GPa and 300 K (a), 123 GPa and 300 K (b), and 50 GPa and 300 K (c)).

In the high-temperature patterns, the broad diffuse X-ray scattering mainly from FeH x melt is highlighted by grey-shaded area. The diffraction peaks of fcc FeH x (with Miller indices) were observed only after temperature quench to 300 K.

Extended Data Fig. 3 The volume per Fe atom of the reaction product, FeH x , after heating at 300 K.

Solid and open symbols indicate temperature (T) conditions were higher than melting T of FeH x or lower than melting T of FeH x , respectively. The volume of bcc Fe at 1 bar, measured from FeSi + H 2 O setup after heating and pressure released 1 bar, is shown as a red cross. Previous results are shown as separate curves or points (FeH and FeH 2 (300 K) 35 ; FeH (300 K) 36 for higher pressure; bcc Fe 77 (black cross at 1 bar); hcp Fe 78 (black crosses at high pressures)). ΔT(m) is a temperature difference between the measured T during heating and the melting temperature of fcc FeH 37 .

Extended Data Fig. 4 The volumes of B2 FeSi at high pressure and 300 K from this study and previous studies 79 , 80 , 81 .

Solid and open symbols indicate temperature conditions were higher than melting T of FeH 37 or lower than melting T of FeH, respectively.

Extended Data Fig. 5 XRD pattern and SEM analysis of the recovered sample from laser heating of Fe-9wt%Si sandwiched between two Mg(OH) 2 layers.

a, In situ X-ray diffraction pattern, and b, c, chemical analysis obtained from experiments at 65 GPa and 300 K after heated at 1800 K at 74 GPa (P30A_18). The experimental setup was a Fe-9wt%Si foil sandwiched between Mg(OH) 2 layers. The scale bars are 7 µm.

Extended Data Fig. 6 SEM analysis of the recovered sample from laser heating of FeSi sandwiched between two Mg(OH) 2 layers.

a, A cross-sectional view of the recovered sample after heating at 2810 K and 129 GPa (A15G_18). The two-dimensional elemental distribution maps of b, Fe (red) and Si (cyan), and c, Fe (red) and Mg (green).

Extended Data Fig. 7 SEM-EDS analysis of the recovered sample from laser heating to 4100 K at 68 GPa of Fe-9wt%Si sandwiched between two Lizardite+MgSiO 3 layers (setup 5).

a, An SEM image of the cross-section of the recovered hot spot (A15H_26). b, The porous texture at the centre of metallic melt (the black box in a) indicates hydrogen escaped from the metallic melt upon decompression to 1 bar. c, An SEM image of the boundary between the metallic melt and silicate melt. The bottom row shows elemental distribution maps for Fe, Si and Mg obtained for the yellow box in (a). The SiO 2 grain was produced by the reaction between Si from the Fe-Si alloy and water from silicate at the boundary between metallic melt and silicate melt.

Extended Data Fig. 8 SEM images of the recovered samples from FeSi + H 2 O.

a, The centre of the heated spot after quenching from 1282 K at 32 GPa (A30A_14). b, The centre of the heated spot after quenching from 1202 K at 28 GPa (A30A_09). Elemental distributions of c, Fe, and d, Si of the area in (b). When H 2 O medium was used, the recovered samples showed complete conversion of FeSi alloy to SiO 2 and FeH, which also agrees with in situ X-ray diffraction result (Extended Data Fig. 1a ). The cracks in (a) are caused by decompression. The scale bars are 1 µm.

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Kim, T., O’Rourke, J.G., Lee, J. et al. A hydrogen-enriched layer in the topmost outer core sourced from deeply subducted water. Nat. Geosci. 16 , 1208–1214 (2023). https://doi.org/10.1038/s41561-023-01324-x

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Received : 09 March 2023

Accepted : 11 October 2023

Published : 13 November 2023

Issue Date : December 2023

DOI : https://doi.org/10.1038/s41561-023-01324-x