A Matter of Preservation

Hawkesworth, Chris J.; Cawood, Peter A.; Kemp, Anthony I.S.; Storey, Craig; Dhuime, Bruno

doi:10.1126/science.1168549

Cited by 342 publications

(189 citation statements)

References 8 publications

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“…In such a scenario it is possibile that Earth might have had episodic mantle convection in its earlier history as previously suggested (Condie, 2001(Condie, , 1998Parman, 2007;Pearson et al, 2007;Frimmel, 2008;Ernst and Buchan, 2002). We also note that the evidence presented for episodicity is controversial; zircon peaks might reflect preservation (Hawkesworth et al, 2009), while it has been argued that the isotopic peaks may not be statistically robust (Rudge, 2008). Phase-change induced mantle avalanches could initiate superplumes/superevents (Condie, 1998).…”

Section: Earth Evolutionmentioning

confidence: 84%

Influence of the Ringwoodite-Perovskite transition on mantle convection in spherical geometry as a function of Clapeyron slope and Rayleigh number

Wolstencroft

Davies

2011

Solid Earth

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Abstract. We investigate the influence on mantle convection of the negative Clapeyron slope ringwoodite to perovskite and ferro-periclase mantle phase transition, which is correlated with the seismic discontinuity at 660 km depth. In particular, we focus on understanding the influence of the magnitude of the Clapeyron slope (as measured by the Phase Buoyancy parameter, P ) and the vigour of convection (as measured by the Rayleigh number, Ra) on mantle convection. We have undertaken 76 simulations of isoviscous mantle convection in spherical geometry, varying Ra and P . Three domains of behaviour were found: layered convection for high Ra and more negative P , whole mantle convection for low Ra and less negative P , and transitional behaviour in an intervening domain. The boundary between the layered and transitional domain was fit by a curve P = αRa β where α = −1.05, and β = −0.1, and the fit for the boundary between the transitional and whole mantle convection domain was α = −4.8, and β = −0.25. These two curves converge at Ra ≈2.5×10 4 (well below Earth mantle vigour) and P ≈ −0.38. Extrapolating to high Ra, which is likely earlier in Earth history, this work suggests a large transitional domain. It is therefore likely that convection in the Archean would have been influenced by this phase change, with Earth being at least in the transitional domain, if not the layered domain.

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Section: Earth Evolutionmentioning

confidence: 84%

Influence of the Ringwoodite-Perovskite transition on mantle convection in spherical geometry as a function of Clapeyron slope and Rayleigh number

Wolstencroft

Davies

2011

Solid Earth

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“…Total losses average 4.9 km 3 /a, based on rates of 0.4 km 3 /a of passive margin subduction in continental collision zones, 0.4 km 3 /a of dissolved chemical weathering flux, 1.1 km 3 /a of lower crustal delamination, 1.3 km 3 /a of forearc tectonic erosion and 1.7 km 3 /a of sediment subduction. At these rates the entire continental crust could be recycled into the mantle in 1.8 Ga. Clearly this has not happened because the centers of cratons have been stable and not recycled, while crust in active margins and orogens are susceptible to destruction by tectonic erosion, as well as by erosion by surface processes and subduction as sediment (Hawkesworth et al, 2009). …”

Section: Discussionmentioning

confidence: 98%

“…The modern Earth appears to be somewhat more mountainous and thus erosive compared to the Earth at 65 Ma, prior to the building of the High Andes and Tibet, as well as much of the Alpine-Himalayan belts (Patzkowsky et al, 1991;Dercourt et al, 1993). These cycles of supercontinent accretion and destruction have been recognized in thermochronology, especially zircon dating, as resulting in a rock record of uneven and biased preservation (Hawkesworth et al, 2009). Furthermore, compilations of global sediment budgets indicate that erosion rates since the initiation of Northern Hemispheric Glaciation are much elevated compared to those before ca.…”

Section: Erosional Destruction Of Cratonic Crust During the Cenozoicmentioning

confidence: 99%

Crustal redistribution, crust–mantle recycling and Phanerozoic evolution of the continental crust

Clift

Vannucchi

Morgan

2009

Earth-Science Reviews

199

151

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“…Based on our analysis of modern tectonic processes, crustal growth is greatest shortly after the supercontinent breaks up and is at a minimum as and after the supercontinent tectonically congeals. Hawkesworth et al (2009) argue that the apparent abundance of igneous rocks during times of inferred supercontinent formation reflects the fact that other tracts of juvenile crust -such as arcs and volcanic rifted margins -are destroyed. We are puzzled by this posit, because the immense size of juvenile arcs -approximately 200-300 km across and up to 30 km thick -are too great to be easily obliterated.…”

Section: Continental Crust Formation and The Supercontinent Cyclementioning

confidence: 99%

“…Crustal growth should dominate early, crustal destruction should dominate late. A significant conundrum to resolve is why the rock record seems to record that crustal growth is at a maximum when supercontinents are thought to have formed, especially for postulated Precambrian supercontinents (Condie 2004;Hawkesworth et al 2009). Based on our analysis of modern tectonic processes, crustal growth is greatest shortly after the supercontinent breaks up and is at a minimum as and after the supercontinent tectonically congeals.…”

Section: Continental Crust Formation and The Supercontinent Cyclementioning

confidence: 99%

Yin and yang of continental crust creation and destruction by plate tectonic processes

Stern

Scholl

2010

International Geology Review

202

107

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Earth's continental crust today is both created and destroyed by plate tectonic processes, a balance that is encapsulated by the traditional Chinese concept of yin-yang, whereby dualities act in concert as well as in opposition. Yin-yang conceptualizations of crustal growth and destruction are mostly related to plate tectonics; both occur mostly at subduction zones, by arc magmatic creation and by subduction removal. Crust is also created and destroyed by processes unrelated to plate tectonics, including losses by lower crust foundering and additions at hotspots. At present, creation and destruction of continental crust is either in balance (∼3.2 km 3 /year, or 3.2 AU) or more crust is being destroyed than created; the uncertainty comes from unknown deep losses of continental crust at collision zones and due to lower crustal foundering. The yinyang creation-destruction balance changes over a supercontinent cycle, with crustal growth being greatest during supercontinent break-up due to high magmatic flux at new arcs and crustal destruction being greatest during supercontinent amalgamation due to subduction of continental material and increased sediment flux due to orogenic uplift. These conclusions challenge the widely held view that continental crust volume has increased over time due to plate tectonic activity; it is just as likely that this volume has decreased.

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A Matter of Preservation

Cited by 342 publications

References 8 publications

Influence of the Ringwoodite-Perovskite transition on mantle convection in spherical geometry as a function of Clapeyron slope and Rayleigh number

Influence of the Ringwoodite-Perovskite transition on mantle convection in spherical geometry as a function of Clapeyron slope and Rayleigh number

Crustal redistribution, crust–mantle recycling and Phanerozoic evolution of the continental crust

Yin and yang of continental crust creation and destruction by plate tectonic processes

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