The Hadean–Archaean transition at 4 Ga: From magma trapping in the mantle to volcanic resurfacing of the Earth

Nédélec, Anne; Monnereau, M.; Toplis, Michael J.

doi:10.1111/ter.12266

Cited by 9 publications

(6 citation statements)

References 43 publications

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“…Investigations of the 4.37-4.02 Ga Jack Hills detrital zircon crystals (JHZ), which are the oldest remnants of primordial felsic magmas on Earth, support the existence of a felsic crust during the earliest stages of the Hadean eon (Cavosie et al, 2006;Harrison, 2009;Burnham and Berry, 2017). Either reworking into younger crust or recycling of the Hadean crust into the mantle have been proposed to explain the lack of remnants of the earliest felsic crust on Earth (O'Neil and Carlson, 2017;Nédélec et al, 2017). However, studies of the Jack Hills zircon crystals allow to infer the presence of an igneous protolith that had experienced low-tomoderate temperature alteration by aqueous fluids, thereby ruling out a sedimentary source (Burnham and Berry, 2017;Whitehouse et al, 2017), although alternative opinions still exist (Harrison, 2009;Bell et al, 2018).…”

Section: Implications For the Early Earthmentioning

confidence: 99%

Hydrated Peridotite – Basaltic Melt Interaction Part I: Planetary Felsic Crust Formation at Shallow Depth

et al. 2021

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Current theories suggest that the first continental crust on Earth, and possibly on other terrestrial planets, may have been produced early in their history by direct melting of hydrated peridotite. However, the conditions, mechanisms and necessary ingredients for this crustal formation remain elusive. To fill this gap, we conducted time-series experiments to investigate the reaction of serpentinite with variable proportions (from 0 to 87 wt%) of basaltic melt at temperatures of 1,250–1,300°C and pressures of 0.2–1.0 GPa (corresponding to lithostatic depths of ∼5–30 km). The experiments at 0.2 GPa reveal the formation of forsterite-rich olivine (Fo90–94) and chromite coexisting with silica-rich liquids (57–71 wt% SiO2). These melts share geochemical similarities with tonalite-trondhjemite-granodiorite rocks (TTG) identified in modern terrestrial oceanic mantle settings. By contrast, liquids formed at pressures of 1.0 GPa are poorer in silica (∼50 wt% SiO2). Our results suggest a new mechanism for the formation of the embryonic continental crust via aqueous fluid-assisted partial melting of peridotite at relatively low pressures (∼0.2 GPa). We hypothesize that such a mechanism of felsic crust formation may have been widespread on the early Earth and, possibly on Mars as well, before the onset of modern plate tectonics and just after solidification of the first ultramafic-mafic magma ocean and alteration of this primitive protocrust by seawater at depths of less than 10 km.

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Section: Implications For the Early Earthmentioning

confidence: 99%

Hydrated Peridotite – Basaltic Melt Interaction Part I: Planetary Felsic Crust Formation at Shallow Depth

et al. 2021

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“…O'Neill and Roberts (2018) refer to stagnant, sluggish, plutonic squishy, or heat pipe variants, whereas Fischer and Gerya (2016) refer to plume-lid tectonics. "Sagduction"-the vertical sinking of weak lithosphere-is another vigorous non-plate tectonic-style (Nédélec et al, 2017). In 2015 we finished taking a first look at all of the large (= semi-spherical) bodies in the Solar System using a variety of spacecraft (Stern et al, 2018).…”

Section: Plate Tectonics and Single-lid Tectonicsmentioning

confidence: 99%

The Mesoproterozoic Single-Lid Tectonic Episode: Prelude to Modern Plate Tectonics

Stern¹

2020

GSAT

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The hypothesis that the Mesoproterozoic (1600-1000 Ma) tectonic regime was a protracted single-lid episode is explored. Singlelid tectonic regimes contrast with plate tectonics because the silicate planet or moon is encased in a single lithospheric shell, not a global plate mosaic. Single-lid tectonics dominate among the Solar System's active silicate bodies, and these show a wide range of magmatic and tectonic styles, including heat pipe (Io), vigorous (Venus), and sluggish (Mars). Both positive and negative evidence is used to evaluate the viability of the Mesoproterozoic single-lid hypothesis. Four lines of positive evidence are: (1) elevated thermal regime; (2, 3) abundance of unusual dry magmas such as A-type granites and anorthosites; and (4) paucity of new passive continental margins. Negative evidence is the lack of rock and mineral assemblages formed by plate-tectonic processes such as ophiolites, blueschists, and ultra high-pressure terranes. Younger platetectonic-related and Mesoproterozoic mineralization styles contrast greatly. Paleomagnetic evidence is equivocal but is permissive that Mesoproterozoic apparent polar wander paths of continental blocks did not differ significantly. These tests compel the conclusion that the Mesoproterozoic single-lid hypothesis is viable.

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“…One geophysical difference between early Earth and now, is the likelihood that whereas the mantle was substantially hotter in the Hadean [ 34 , 135 ], the oceanic crust was stagnant prior to the onset of plate tectonics produced by volcanic over-, inter- and under-plating, fed from super plumes. Hence, at certain locations, the thermal gradient in dormant sections would have been much lower on early Earth [ 35 , 37 ].…”

Section: Four Minerals To Set the Stage For Life’s Emergencementioning

confidence: 99%

Six ‘Must-Have’ Minerals for Life’s Emergence: Olivine, Pyrrhotite, Bridgmanite, Serpentine, Fougerite and Mackinawite

Russell

Ponce

2020

Life

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Life cannot emerge on a planet or moon without the appropriate electrochemical disequilibria and the minerals that mediate energy-dissipative processes. Here, it is argued that four minerals, olivine ([Mg>Fe]2SiO4), bridgmanite ([Mg,Fe]SiO3), serpentine ([Mg,Fe,]2-3Si2O5[OH)]4), and pyrrhotite (Fe(1−x)S), are an essential requirement in planetary bodies to produce such disequilibria and, thereby, life. Yet only two minerals, fougerite ([Fe2+6xFe3+6(x−1)O12H2(7−3x)]2+·[(CO2−)·3H2O]2−) and mackinawite (Fe[Ni]S), are vital—comprising precipitate membranes—as initial “free energy” conductors and converters of such disequilibria, i.e., as the initiators of a CO2-reducing metabolism. The fact that wet and rocky bodies in the solar system much smaller than Earth or Venus do not reach the internal pressure (≥23 GPa) requirements in their mantles sufficient for producing bridgmanite and, therefore, are too reduced to stabilize and emit CO2—the staple of life—may explain the apparent absence or negligible concentrations of that gas on these bodies, and thereby serves as a constraint in the search for extraterrestrial life. The astrobiological challenge then is to search for worlds that (i) are large enough to generate internal pressures such as to produce bridgmanite or (ii) boast electron acceptors, including imported CO2, from extraterrestrial sources in their hydrospheres.

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The Hadean–Archaean transition at 4 Ga: From magma trapping in the mantle to volcanic resurfacing of the Earth

Cited by 9 publications

References 43 publications

Hydrated Peridotite – Basaltic Melt Interaction Part I: Planetary Felsic Crust Formation at Shallow Depth

Hydrated Peridotite – Basaltic Melt Interaction Part I: Planetary Felsic Crust Formation at Shallow Depth

The Mesoproterozoic Single-Lid Tectonic Episode: Prelude to Modern Plate Tectonics

Six ‘Must-Have’ Minerals for Life’s Emergence: Olivine, Pyrrhotite, Bridgmanite, Serpentine, Fougerite and Mackinawite

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