The exchange of volatile species—water, carbon dioxide, nitrogen and halogens—between the mantle and the surface of the Earth has been a key driver of environmental changes throughout Earth’s history. Degassing of the mantle requires partial melting and is therefore linked to mantle convection, whose regime and vigour in the Earth’s distant past remain poorly constrained1,2. Here we present direct geochemical constraints on the flux of volatiles from the mantle. Atmospheric xenon has a monoisotopic excess of 129Xe, produced by the decay of extinct 129I. This excess was mainly acquired during Earth’s formation and early evolution3, but mantle degassing has also contributed 129Xe to the atmosphere through geological time. Atmospheric xenon trapped in samples from the Archaean eon shows a slight depletion of 129Xe relative to the modern composition4,5, which tends to disappear in more recent samples5,6. To reconcile this deficit in the Archaean atmosphere by mantle degassing would require the degassing rate of Earth at the end of the Archaean to be at least one order of magnitude higher than today. We demonstrate that such an intense activity could not have occurred within a plate tectonics regime. The most likely scenario is a relatively short (about 300 million years) burst of mantle activity at the end of the Archaean (around 2.5 billion years ago). This lends credence to models advocating a magmatic origin for drastic environmental changes during the Neoarchaean era, such as the Great Oxidation Event.
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The sample description and Xe data are available at https://zenodo.org/record/3378722#.Xa6cMi3pNvE.
The Matlab code for modelling the degassing rate of Xe from the mantle is available at https://zenodo.org/record/3381874#.Xa6cey3pNvE.
Labrosse, S. & Jaupart, C. Thermal evolution of the Earth: secular changes and fluctuations of plate characteristics. Earth Planet. Sci. Lett. 260, 465–481 (2007).
Stüeken, E. E., Kipp, M. A., Scwieterman, E. W., Johnson, B. & Buick, R. Modeling pN2 through geological time: implications for planetary climates and atmospheric biosignatures. Astrobiology 16, 949–963 (2016).
Marty, B. et al. Xenon isotopes in 67P/Churyumov-Gerasimenko show that comets contributed to Earth’s atmosphere. Science 356, 1069–1072 (2017).
Bekaert, D. V. et al. Archean kerogen as a new tracer of atmospheric evolution: implications for dating the widespread nature of early life. Sci. Adv. 4, eaar2091 (2018).
Avice, G. et al. Evolution of atmospheric xenon and other noble gases inferred from Archean to Paleoproterozoic rocks. Geochim. Cosmochim. Acta 232, 82–100 (2018).
Meshik, A. P., Hohenberg, C. M., Pravdivtseva, O. V. & Kapusta, Y. S. Weak decay of Ba-130 and Ba-132: geochemical measurements. Phys. Rev. C 64, 035205 (2001).
Ozima, M. & Podosek, F. A. Noble Gas Geochemistry (Cambridge Univ. Press, 2002).
Avice, G., Marty, B. & Burgess, R. The origin and degassing history of the Earth’s atmosphere revealed by Archean xenon. Nat. Commun. 8, 15455 (2017).
Pujol, M., Marty, B. & Burgess, R. Chondritic-like xenon trapped in Archean rocks: a possible signature of the ancient atmosphere. Earth Planet. Sci. Lett. 308, 298–306 (2011).
Mukhopadhyay, S. Early differentiation and volatile accretion recorded in deep-mantle neon and xenon. Nature 486, 101–104 (2012).
Péron, S. & Moreira, M. Onset of volatile recycling into the mantle determined by xenon anomalies. Geochem. Persp. Lett. 9, 21–25 (2018).
Marty, B., Zimmermann, L., Pujol, M., Burgess, R. & Philippot, P. Nitrogen isotopic composition and density of the Archean atmosphere. Science 342, 101–104 (2013).
Zahnle, K. J., Gacesa, M. & Catling, D. C. Strange messenger: a new history of hydrogen on Earth, as told by xenon. Geochim. Cosmochim. Acta 244, 56–85 (2019).
Pujol, M., Marty, B., Burgess, R., Turner, G. & Philippot, P. Argon isotopic composition of Archaean atmosphere probes early Earth geodynamics. Nature 498, 87–90 (2013).
Bianchi, D. et al. Low helium flux from the mantle inferred from simulations of oceanic helium isotope data. Earth Planet. Sci. Lett. 297, 379–386 (2010).
Allard, P. Global emissions of helium-3 by subaerial volcanism. Geophys. Res. Lett. 19, 1478–1481 (1992).
Parai, R. & Mukhopadhyay, S. Xenon isotopic constraints on the history of volatile recycling into the mantle. Nature 560, 223–227 (2018): correction. 563, E28 (2018).
Herzberg, C., Condie, K. & Korenaga, J. Thermal history of the Earth and its petrological expression. Earth Planet. Sci. Lett. 292, 79–88 (2010).
Heber, V. S., Brooker, R. A., Kelley, S. P. & Wood, B. J. Crystal-melt partitioning of noble gases (helium, neon, argon, krypton, and xenon) for olivine and clinopyroxene. Geochim. Cosmochim. Acta 71, 1041–1061 (2007).
Porcelli, D. & Elliott, T. The evolution of He isotopes in the convective mantle and the preservation of high 3He/4He ratios. Earth Planet. Sci. Lett. 269, 175–185 (2008).
Sleep, N. H. in Treatise on Geophysics 9 (ed. Stevenson, D.) 145–170 (Elsevier, 2007).
Korenaga, J. Thermal evolution with a hydrating mantle and the initiation of plate tectonics in the early Earth. Earth Planet. Sci. Lett. 116, 1–20 (2011).
Tang, M., Chen, K. & Rudnick, R. L. Archean upper crust transition from mafic to felsic marks the onset of plate tectonics. Science 351, 372–375 (2016).
Blake, T. S., Buick, R., Brown, S. J. A. & Barley, M. E. Geochronology of a Late Archaean flood basalt province in the Pilbara Craton, Australia: constraints on basin evolution, volcanic and sedimentary accumulation, and continental drift rates. Precambr. Res. 133, 143–173 (2004).
Sleep, N. H. & Windley, B. F. Archean plate tectonics: constraints and inferences. J. Geol. 90, 363–379 (1982).
Percival, J. A., Stern, R. A. & Skulski, T. Crustal growth through successive arc magmatism: reconnaissance U–Pb SHRIMP data from the northeastern Superior Province, Canada. Precambr. Res. 109, 203–238 (2001).
Ciborowski, T. J. R. & Kerr, A. C. Did mantle plume magmatism help trigger the Great Oxidation Event? Lithos 246–247, 128–133 (2016).
Holland, H. D. Volcanic gases, black smokers, and the Great Oxidation Event. Geochim. Cosmochim. Acta 66, 3811–3826 (2002).
Canil, D. Vanadium in peridotites, mantle redox and tectonic environments: Archean to present. Earth Planet. Sci. Lett. 195, 75–90 (2002).
Gaillard, F., Scaillet, B. & Arndt, N. T. Atmospheric oxygenation caused by a change in volcanic degassing pressure. Nature 478, 229–232 (2011).
Marty, B. & Tolstikhin, I. N. CO2 fluxes from mid-ocean ridges, arcs and plumes. Chem. Geol. 145, 233–248 (1998).
Kasting, J. F. Faint young Sun redux. Nature 464, 687–689 (2010).
Rubin, M. et al. Krypton isotopes and noble gas abundances in the coma of comet 67P/Churyumov-Gerasimenko. Sci. Adv. 4, eaar6297 (2018).
Reimold, W. U. & Gibson, R. L. Geology and evolution of the Vredefort impact structure, South Africa. J. Afr. Earth Sci. 23, 125–162 (1996).
Tolstikhin, I. N. & Marty, B. The evolution of terrestrial volatiles: a view from helium, neon, argon and nitrogen isotope modelling. Chem. Geol. 147, 27–52 (1998).
Halliday, A. N. The origins of volatiles in the terrestrial planets. Geochim. Cosmochim. Acta 105, 146–171 (2013).
Gonnermann, H. M. & Mukhopadhyay, S. Preserving noble gases in a convective mantle. Nature 459, 560–563 (2009).
Holland, G. & Ballentine, C. J. Seawater subduction controls the heavy noble gas composition of the mantle. Nature 441, 186–191 (2006).
Ballentine, C. J., Marty, B., Sherwood Lollar, B. & Cassidy, M. Neon isotopes constrain convection and volatile origin in the Earth’s mantle. Nature 433, 33–38 (2005).
Moreira, M. & Charnoz, S. The origin of the neon isotopes in chondrites and on the Earth. Earth Planet. Sci. Lett. 433, 249–256 (2016).
Williams, C. D. & Mukhopadhyay, S. Capture of nebular gases during Earth’s accretion is preserved in deep-mantle neon. Nature 565, 78–81 (2019).
Marty, B. The origins and concentrations of water, carbon, nitrogen and noble gases on Earth. Earth Planet. Sci. Lett. 313–314, 56–66 (2012).
Caffee, M. W. et al. Primordial noble gases from Earth’s mantle: identification of a primitive volatile component. Science 285, 2115–2118 (1999).
Korenaga, J. in Archean Geodynamics and Environments (eds Benn, K., Mareschal, J. C. & Condie, K. C.) 7–32 (Geophys. Monogr. Ser. 164, AGU, 2006).
Jaupart, C. & Mareschal, J.-C. in Treatise on Geophysics 6 (ed. Stevenson, D.) 217–251 (Elsevier, 2007).
Herzberg, C. & Asimow, P. D. PRIMELT3 MEGA.XLSM software for primary magma calculation: peridotite primary magma MgO contents from the liquidus to the solidus. Geochem. Geophys. Geosyst. 16, 563–578 (2015).
This study was supported by the European Research Council (Photonis Advanced Grant no. 695618). We thank G. Avice for discussions, and the Fondation des Treilles for providing a congenial environment in which to discuss these concepts with colleagues.
The authors declare no competing interests.
Publisher’s note Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
Peer review information Nature thanks Greg Holland and the other, anonymous, reviewer(s) for their contribution to the peer review of this work.
Extended data figures and tables
Grey and blue data points5,8 define the evolution (red curve) of atmospheric Xe mass-dependent fractionation (MDF)4. The left-hand y axis shows the isotopic fractionation of atmospheric Xe (δXeair) in units of ‰ per atomic mass unit (u). The right-hand y axis represents multiples of the Xe inventory of the modern atmosphere, ATMXe. Error bars, ±2σ. The purple point on the left-hand side (ATM) is the modern atmospheric composition, the red dot on the right-hand side (U-Xe) is the primordial composition of atmospheric xenon3, the grey-shaded area shows the data range from ref. 5 and references therein, and the dotted horizontal line gives the MDF value; the ATMXe values correspond to a mean age of 3 Ga.
Open circle data points are from ref. 38, and the pink filled circle shows the isotopic composition of air (error bars, 1σ). The boxed area at lower left is shown magnified in the inset. There is a correlation between the excess 129Xe and 128Xe (thick line, dotted thin lines define the error envelope, 95% CI) that can be used to extrapolate the primordial 129Xe/130Xe of the mantle source for an AVCC-like 128Xe/130Xe (dashed black line).
Extended Data Fig. 3 Modelled evolution of the atmospheric 40Ar/36Ar ratio as a function of time following a mantle degassing event between 2.6 Ga and 2.2 Ga.
The values are scaled to 129XeDEF, and are shown with different contributions of mantle 40Ar: 0% (‘Monotonic’), 5% and 10%. Atmospheric 40Ar/36Ar ratios are normalized to the present-day value of 298.6, and the evolution curves were adjusted in order to yield the modern value. The Archaean atmosphere’s value is from ref. 14. The yellow dot marks the end of catastrophic degassing and the start of continuous degassing, following ref. 14.
Extended Data Fig. 4 Schematic representation of the method used to calculate the contribution of mantle-derived 129Xe to the atmospheric budget of 129Xe from step i − 1 to step i.
The format is the same as in Fig. 1, where the y axis corresponds to δXeair (only indicative here).The ‘mantle’ arrow indicates that the 129Xe/130Xe of the mantle end-member is high, and would plot off-graph in this space. Δ129Xe values at each step of the simulation are reported on the left of the corresponding data points. The dashed line corresponds to the MDF line, with the shaded blue area representing the corresponding error envelope.
Shown is recycling of atmospheric Xe into the mantle (blue lines, left-hand y axis)17 compared to the time evolution of atmospheric Xe isotopic composition4 (δXeair, right-hand y axis). The pink arrow shows the direction of atmospheric Xe isotopic evolution, from U-Xe (the progenitor of atmospheric Xe) to present. This illustrates the fact that regassing of atmospheric Xe into the mantle would have become efficient only after atmospheric Xe had reached a modern-like isotopic composition, that is, within the last 1.5 Gyr. Adapted from ref. 17.
Extended Data Fig. 6 Maximum flux of Xe (represented by 130Xe) degassed from the mantle as a function of the mantle 129Xe/130Xe ratio.
Computations reported in Fig. 2 of the main text have been carried out using a fixed mantle 129Xe/130Xe of 14. Here we show that lowering this ratio (for example, via subduction of atmospheric Xe) down to modern mantle-like 129Xe/130Xe ≈ 7–8 would result in even greater Xe fluxes from the Archaean mantle (see black arrow). Given that the onset of atmospheric Xe recycling into the mantle is not well known, possible 130Xe flux values from the Archaean mantle are within the range 10–150 mol yr−1 (orange curve), well above the modern flux value (0.85 ± 0.35 mol yr−1, horizontal dashed line; Extended Data Table 2).
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Marty, B., Bekaert, D.V., Broadley, M.W. et al. Geochemical evidence for high volatile fluxes from the mantle at the end of the Archaean. Nature 575, 485–488 (2019) doi:10.1038/s41586-019-1745-7