Guyana: the Lost Hadean crust of South America?

Nadeau, Sylvain; Chen, Wei; Reece, Jimmy; Lachhman, Deokumar; Ault, Randy; Faraco, Maria Telma Lins; Fraga, Lêda Maria Barreto; Reis, Nelson Joaquim; Betiollo, Leandro Menezes

doi:10.5327/z2317-48892013000400002

Cited by 34 publications

(16 citation statements)

References 6 publications

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“…Schobbenhaus et al 2004, Cordani & Teixeira 2007, Cordani et al 2010, Bettencourt et al 2010. The oldest portion (Hadean-Archean) of the Amazonian Craton (Central Amazonian Province) consists of granite-greenstone terrains and high-grade metamorphic rocks exposed in the Brazil-Central and Guiana shields (Tassinari & Macambira 2004, Nadeau et al 2013. The MaroniItacaiúnas Belt separates these landmasses, and it is dated around 2250-2050 Ma (Ledru et al 1994).…”

Section: The Amazonian Cratonmentioning

confidence: 99%

Paleomagnetism of the Amazonian Craton and its role in paleocontinents

et al. 2016

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In the last decade, the participation of the Amazonian Craton on Precambrian supercontinents has been clarified thanks to a wealth of new paleomagnetic data. Paleo to Mesoproterozoic paleomagnetic data favored that the Amazonian Craton joined the Columbia supercontinent at 1780 Ma ago, in a scenario that resembled the South AMerica and BAltica (SAMBA) configuration. Then, the mismatch of paleomagnetic poles within the Craton implied that either dextral transcurrent movements occurred between Guiana and Brazil-Central Shield after 1400 Ma or internal rotation movements of the Amazonia-West African block took place between 1780 and 1400 Ma. The presently available late-Mesoproterozoic paleomagnetic data are compatible with two different scenarios for the Amazonian Craton in the Rodinia supercontinent. The first one involves an oblique collision of the Amazonian Craton with Laurentia at 1200 Ma ago, starting at the present-day Texas location, followed by transcurrent movements, until the final collision of the Amazonian Craton with Baltica at ca. 1000 Ma. The second one requires drifting of the Amazonian Craton and Baltica away from the other components of Columbia after 1260 Ma, followed by clockwise rotation and collision of these blocks with Laurentia along Grenvillian Belt at 1000 Ma. Finally, although the time Amazonian Craton collided with the Central African block is yet very disputed, the few late Neoproterozoic/Cambrian paleomagnetic poles available for the Amazonian Craton, Laurentia and other West Gondwana blocks suggest that the Clymene Ocean separating these blocks has only closed at late Ediacaran to Cambrian times, after the Amazonian Craton rifted apart from Laurentia at ca. 570 Ma.

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Section: The Amazonian Cratonmentioning

confidence: 99%

Paleomagnetism of the Amazonian Craton and its role in paleocontinents

et al. 2016

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“…Narryer quartzite by Froude et al (1983) and subsequently in greater abundance by Compston and Pidgeon (1986) in a quartz pebble metaconglomerate at the Jack Hills -both in the Narryer Gneiss Complex of the Yilgarn Craton, western Australia. Zircons with Hadean (> 4 Ga) 207 Pb/ 206 Pb ages have subsequently been reported from most other continents including North America (Bowring and Williams, 1999;Mojzsis and Harrison, 2002;Iizuka et al, 2006), South America (Nadeau et al, 2013;Paquette et al, 2015), Eurasia (Wang et al, 2007;Duo et al, 2007;Xu et al, 2012;Xing et al, 2014), India (Miller et al, 2018), and Africa (Byerly et al, 2018), suggesting a widely distributed occurrence of zirconbearing crust by at least the late Hadean. Nonetheless, both the antiquity (Valley et al, 2014) and quantity (Holden et al, 2009) of Hadean zircon from the Jack Hills far exceed that yet analyzed from any other locality; as such, the Jack Hills zircon record predominates our understanding of the Hadean eon on Earth.…”

Section: Introductionmentioning

confidence: 96%

Stepwise chemical abrasion–isotope dilution–thermal ionization mass spectrometry with trace element analysis of microfractured Hadean zircon

Keller

Boehnke²,

Schoene

et al. 2019

Geochronology

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Abstract. The Hadean Jack Hills zircons represent the oldest known terrestrial material, providing a unique and truly direct record of Hadean Earth history. This zircon population has been extensively studied via high-spatial-resolution high-throughput in situ isotopic and elemental analysis techniques, such as secondary ionization mass spectrometry (SIMS), but not by comparatively destructive, high-temporal-precision (<0.05 % two-sigma) thermal ionization mass spectrometry (TIMS). In order to better understand the lead loss and alteration history of terrestrial Hadean zircons, we conduct stepwise chemical abrasion–isotope dilution–thermal ionization mass spectrometry with trace element analysis (CA-ID-TIMS-TEA) on manually microfractured Hadean Jack Hills zircon fragments previously dated by SIMS. We conducted three successive HF leaching steps on each individual zircon fragment, followed by column chromatography to isolate U–Pb and trace element fractions. Following isotopic and elemental analysis, the result is an independent age and trace element composition for each leachate of each zircon fragment. We observe ∼50 Myr of age heterogeneity in concordant residues from a single zircon grain, along with a protracted history of post-Hadean Pb loss with at least two modes circa ∼0 and 2–4 Ga. Meanwhile, stepwise leachate trace element chemistry reveals enrichments of light rare earth elements, uranium, thorium, and radiogenic lead in early leached domains relative to the zircon residue. In addition to confirming the efficacy of the LREE-I alteration index and providing new insight into the mechanism of chemical abrasion, the interpretation and reconciliation of these results suggest that Pb loss is largely driven by low-temperature aqueous recrystallization and that regional thermal events may act to halt – not initiate – Pb loss from metamict domains in the Hadean Jack Hills zircons.

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“…These mafic-dominated supracrustal belts are thought to represent segments of the ancient oceanic crust and their isotopic characters provide information about the Hadean and Eoarchean mantle (Furnes et al, 2009;O'Neil et al, 2012). Evidence is also accumulating about the existence of continental crust in Hadean times (4.0-4.5 Ga) from study of zircon grains in Archean sediments and xenocrystic zircon grains in granitic gneisses (Compston and Pidgeon, 1986;Nelson et al, 2000;Wilde et al, 2001;Wyche et al, 2004;Iizuka et al, 2006;Duo et al, 2007;Harrison, 2009;Nadeau et al, 2013). In recent years more refined isotopic studies of Pb, Sm, Nd, Lu, Hf, and particularly of short lived isotopes and oxygen isotopes have provided new information on the processes of crustal growth during the Hadean time and on the physical and chemical conditions existing on the surface of the early Earth (Bowring and Housh, 1995;Moorbath and Whitehouse, 1996;Kemp et al, 2010).…”

Section: Introductory Remarksmentioning

confidence: 99%

The Architecture and Evolution of the Singhbhum Craton

Mukhopadhyay

Matin

2020

Episodes

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The Singhbhum Craton is built up by successive pulses of discrete granitic magmatism at ~3.52 Ga, Ga that produced tonalitetrondhjemite-granodiorite (TTG)-type suites and were followed by younger pulses at 3. Ga producing voluminous granitic-granodioritic magma. There is enough evidence to indicate that continental crust building activity started in the Hadean time and continued through Eoarchean. But the rocks of this period were fully recycled to generate the Paleoarchean and younger crust. The different pulses of granitic magmatism during the Paleoarchean were interspersed with the formation of supracrustal rocks which are now preserved as supracrustal belts peripheral to the craton or as internal screens within the craton. Halfnium isotopic record suggests that the Hadean and Eoarchean granitoids were sourced in an enriched reservoir, probably some form of early mafic protocrust. From ~3.6-3.5 Ga a shift in the isotopic composition of Hf is noticed, marked by upward excursion of ε Hf(t) plots towards suprachondritic values, signifying that the early mantle reservoir was serially modified by contamination by a juvenile melt derived from a depleted source. This probably signals a change in the geodynamic scenario, major depletion of the mantle and generation of voluminous TTG melts. There are contending hypotheses of plume-driven and subduction-driven mechanisms of continental crust formation. In the Singhbhum Craton during Hadean and Eoarchean times episodic mantle plumes probably operated in a stagnant lid tectonic setting. Repeated plume activities and the formation of oceanic plateaus might have triggered the onset of subduction which at the initial stages might have been of short duration. The transition from plume-driven tectonics to subduction-driven tectonics might have taken place at about 3.5 Ga. The supracrustal belts of the Older Metamorphic Group (OMG) and the Iron Ore Group (IOG) are thought to have formed in supra-subduction settings. Widespread metamorphism and deformation affected the craton during 3.34-3.26 Ga. By 3.1 Ga the Singhbhum Craton had stabilized and emerged as a landmass. Paleosols developed on the surface; rift basins were formed which were receptacles of siliciclastic sediments and mafic volcanics; anorogenic K-feldspar bearing granites were emplaced. Swarms of mafic dykes of Paleo-to Meso-Proterozoic age intruded the craton marking a tensional regime that was probably related to the initial stage of basin formation in the North Singhbhum Mobile Belt.

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Guyana: the Lost Hadean crust of South America?

Cited by 34 publications

References 6 publications

Paleomagnetism of the Amazonian Craton and its role in paleocontinents

Paleomagnetism of the Amazonian Craton and its role in paleocontinents

Stepwise chemical abrasion–isotope dilution–thermal ionization mass spectrometry with trace element analysis of microfractured Hadean zircon

The Architecture and Evolution of the Singhbhum Craton

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