A Palaeoproterozoic diamond-bearing lithospheric mantle root beneath the Archean Sask Craton, Canada

Czas, Janina; Pearson, D.G.; Stachel, Thomas; Kjarsgaard, Bruce A.; Read, G.

doi:10.1016/j.lithos.2019.105301

Cited by 12 publications

(12 citation statements)

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“…A peak in depletion ages between 2.0 and 1.8 Ga occurs in mantle lithosphere beneath Archean and Proterozoic cratons (Box 3), indicating mantle root formation in the Paleoproterozoic [111][112][113][114] , either coincident with the assembly of some larger composite cratons e.g., Siberia, or prior to / during the formation of the Nuna supercontinent, which created some of the larger composite cratons observed today.…”

Section: )mentioning

confidence: 99%

“…Despite the association of predominantly Archean mantle underlying Archean nuclei and Proterozoic mantle underlying Proterozoic cratons (Box 3), more age decoupling exists between crust and mantle than originally proposed, e.g., 77 , with lithospheric mantle recording Archean melt extraction underlying Paleoproterozoic crust 48,115 , Paleoproterozoic mantle residues underlying Archean crust 114 , Neoarchean mantle residues underlying Meso-to Eoarchean crust 116 and Mesoproterozoic residues underlying Neoarchean crust 89 .…”

Section: )mentioning

confidence: 99%

“…A complex age structure is also evident in the mantle beneath the central Rae craton, northern Canada, where older, shallow Archean mantle is underlain by mantle that either formed, or was massively over-printed at circa 1.8 Ga 125 . Similarly, the Archean Sask craton (Canada) is underlain by mantle depleted at ~ 1.8 to 2 Ga, associated with the Trans-Hudson orogeny 114 , and the central Superior craton experienced significant lithosphere replacement during the Mesoproterozoic 126 . In contrast, the Paleoproterozoic Halls Creek orogen (West Australia composite craton) is underlain by deep lithospheric mantle of Archean age 115 , and a similar relationship exists in East 48 and West 116 Greenland, part of the Laurentia supercraton (Fig.…”

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confidence: 99%

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Deep continental roots and cratons

Pearson

Scott

Liu

et al. 2021

Nature

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129

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The formation and preservation of cratons -the oldest parts of the continents comprising over 60% of the continental landmass -remains an enduring problem. Keyto craton development is how and when the thick strong mantle roots that underlie these regions formed and evolved. Peridotite melting residues forming cratonic lithospheric roots mostly originated via relatively low-pressure melting and were subsequently transported to greater depth by thickening produced by lateral accretion and compression. The longest-lived cratons assembled during Mesoarchean and Paleoproterozoic times, creating the 150 to 250 km thick, stable mantle roots that are critical to preserving Earth's early continents and central to defining the cratons although we extend the definition of cratons to include extensive regions of long-stable Mesoproterzoic crust also underpinned by thick lithospheric roots. The production of widespread thick and strong lithosphere via the process of orogenic thickening, possibly in several cycles, was fundamental to the eventual emergence of extensive continental landmasses -the cratons.

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Section: )mentioning

confidence: 99%

Section: )mentioning

confidence: 99%

Section: )mentioning

confidence: 99%

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Deep continental roots and cratons

Pearson

Scott

Liu

et al. 2021

Nature

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129

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“…It is evident that the oxidation state is the major factor of diamond formation [233]. They may characterise the source and possible host melts [234] and processes of their formation and as well as geodynamic regimes in ancient times [235][236][237][238][239][240].…”

Section: Dependence Of Dia Compositions On the Position Within The Cratons And Terrain Typementioning

confidence: 99%

Thermobarometry of Diamond Inclusions: Evidence Mantle Evolution beneath Siberian Craton and Archean Cratons Worldwide.

Ashchepkov¹,

Logvinova²,

Spetsius³

et al. 2021

Preprint

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Thermobarometric calculations for mineral inclusions in diamonds provide a systematic comparison of PTXFO2 conditions for different cratons worldwide, using a database of 4440 mineral EPMA analyses. Beneath all cratons, the cold branch of the mantle geotherm (35-32 mWm−2) relates to the sub-Ca garnets and rarely omphacitic diamond inclusions, referring to major continental growth events in Archean. High-temperature plume-related geotherms are common in Proterozoic kimberlites such as Premier, Mesozoic – Roberts Victor etc. and are common in Slave and Siberian cratons. In mobile belts: Limpopo, Magondi, Ural Ural, Khapchan belts and in the marginal parts of cratons like Kimberly Australia pyroxenitic and eclogitic pyroxenes and garnets prevail. The pyropes in the mobile belts are more Fe- and Ca-rich, in central parts of cratons, the peridotitic associations with sub- Ca pyropes prevail. The accretionary complexes like Khapchan and Magondi belts a thick eclogite-pyroxenite lens is highly diamondiferous. Comparison by minerals shows that the PT estimates for clinopyroxenes and orthopyroxene from peridotites and eclogites are representing mainly the middle part of the sub-lithospheric mantle while garnets gives more high-pressure estimates. refer to eclogites and reflect the processes of the differentiation during migration of partial melts. This produces the trends of joint decreasing Mg’ and pressures. The PT for the chromites reflect conditions just above the lithosphere-asthenosphere boundary and mainly were formed due to interaction with the hydrous plume protokimberlite melts. Archean diamond inclusions from Wawa province Canada are represented by Ca-enrich pyropes giving low-temperature conditions. Inclusions from younger kimberlites in Superior and Slave (and Siberian and East European ) cratons show complex high-temperature geotherms due to plumes influence. Peridotite garnets beneath the Amazonian craton indicate complex layering in the lithosphere base and a pyroxene layer in the middle part of SCLM. Diamond inclusions from the Kimberley craton of Australia show the greatest variations in the temperatures and composition.

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“…Other examples of delayed crust-root coupling continue to be reported, such as the North Atlantic Craton and the Sask Craton in Canada (Wittig et al, 2010;Czas et al, 2020). The big wedge model for Archean plumes does not necessarily rule out the possibility that subducted slabs obstructed keel ascent beneath some cratons or that mantle overturn events independently generated "lifebuoy" keels after late Archean greenstone belts underwent crustal-level orogenic processes.…”

Section: Cratonization -Thermal Imprints and Keel Developmentmentioning

confidence: 99%

Komatiites From Mantle Transition Zone Plumes

Wyman

2020

Front. Earth Sci.

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During the Archean, episodic volcanism commonly included both plume-and arctype magmatism, raising the issue of a possible link between "bottom up" and "top down" geodynamic processes. Rather than plume-initiated subduction, the bestpreserved cratons demonstrate that komatiitic magmatism postdated at least some of the subduction linked volcanism. Several factors suggest that komatiite-generating plumes were sourced in the mantle transition zone. Komatiites contain 0.6 wt.% or more H 2 O, which is contrary to earlier predictions for plume ascent through the transition zone. Geodynamic reconstructions indicate that multiple subducted slabs penetrated the transition zone in the region of future plume ascent and the related trench configurations limit the size of any associated plume heads. The implied plume head sizes are inconsistent with those required for a plume to ascend from the core-mantle boundary but match those predicted for plumes sourced from the lower transition zone. Transition zone plumes have mainly been advocated for in post-Archean "big wedge" scenarios involving subducted slabs that stall at the base of the transition zone but they are also an outcome of the "basalt barrier" featured in some geodynamic models for the Archean and early Proterozoic. The latter models suggest the basaltic components of Archean subducted slabs were too buoyant to descend into the lower mantle and formed a boundary layer that isolated the upper mantle and lower mantle on the early Earth, except in times of mantle overturns. The basalt barrier was a significant thermal boundary layer that, in principle, could act as the nucleation site of upwelling plumes anywhere on the globe. The evidence discussed here, however, suggests that the mainly peridotitic mantle upwellings were enhanced by the nearby injection of closely associated slabs into the transition zone. The simplicity of the Mantle Transition Zone (MTZ) plume-forming mechanism ensured that komatiites could be generated throughout the Archean even as Earth moved toward a regime involving modernstyle subduction, globe-encompassing oceanic ridge systems and tectonic plates. The distinctive geodynamic setting of Gorgona Island produced relatively low-temperature komatiites at the only place along the margin of North and South America where it was possible to reproduce the bowl-like subduction configurations commonly associated with their Archean and Paleoproterozoic counter parts.

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A Palaeoproterozoic diamond-bearing lithospheric mantle root beneath the Archean Sask Craton, Canada

Cited by 12 publications

References 76 publications

Deep continental roots and cratons

Deep continental roots and cratons

Thermobarometry of Diamond Inclusions: Evidence Mantle Evolution beneath Siberian Craton and Archean Cratons Worldwide.

Komatiites From Mantle Transition Zone Plumes

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