Global dynamic topography observations reveal limited influence of large-scale mantle flow

Hoggard, Mark; White, Nicholas J.; Al-Attar, David

doi:10.1038/ngeo2709

Cited by 178 publications

(380 citation statements)

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“…For instance, the modeled dynamic geoid typically gives a good correlation with observations, due to a large contribution of the lower mantle (Čadek and Fleitout, 2003;5 Hager et al, 1985;Richards and Hager, 1984), but is sensitive to the choice of the mantle viscosity (Thoraval and Richards, 1997). However, the correlation between the modeled dynamic and residual topography is typically found to be weak (Heine et al, 2008;Flament et al, 2012;Steinberger and Calderwood, 2006;Steinberger, 2016;Hoggard et al, 2016). The residual topography is here defined as the observed topography corrected for the variations in the crustal and lithosphere thickness and density variations and for subsidence of the sea floor with age.…”

Section: Introductionmentioning

confidence: 99%

“…A qualitative comparison of the two observation-based residual topography fields with the modeled topography shows some (Table 1) in oceans to Steinberger (2016) (S2016) and Hoggard et al (2016 respectively. This model uses the thermal density structure derived from the ocean floor age in the upper 300 km; hence, when this contribution is removed, only the lower mantle contribution remains.…”

Section: = 23mentioning

confidence: 99%

“…Here, we compare our modeled dynamic topography to two independent observation-based residual topography fields (Hoggard et al, 2016;Steinberger, 2016). Residual topography gives a convenient way to constrain both isostatic and 5 non-isostatic contributions to the modeled dynamic topography (Crough, 1978;Gurnis et al, 2000;Wheeler and White, 2000;Becker et al, 2014;Heidbach et al, 2016;Steinberger, 2016).…”

Section: = 23mentioning

confidence: 99%

“…This is done with the assumption that if topography is perfectly compensated isostatically within the upper mantle at depths within the range of 100 -150 km, the integral of density with depth, as a function of crustal thickness and density to the Moho depth and of sea floor age will be the same everywhere for the chosen depth. The observation-based model by Hoggard et al (2016) is derived from ocean seismic surveys (in-situ) in 10 oceanic regions and free-air gravity anomaly data in continents (Figure 12a), while the residual topography model of Steinberger (2016) (Figure 12b) is derived with the CRUST 1.0 model (Laske et al, 2013). These two models are comparable in most oceanic regions, but give large mismatches in continents.…”

Section: = 23mentioning

confidence: 99%

“…As part of this work, we estimate dynamic topography and correlate our results with two different residual topography models. One is based on seismic surveys of the ocean floor used to correct for shallow contributions to topography and free-air gravity anomalies on continents (Hoggard et al, 2016). The second model is taken from Steinberger (2016) and is based on actual topography corrected for crustal thickness and density from CRUST1.0 (Laske et al, 2013).…”

Section: Introductionmentioning

confidence: 99%

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Effects of upper mantle heterogeneities on lithospheric stress field and dynamic topography

Tutu¹,

Steinberger²,

Sobolev³

et al. 2017

Preprint

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Abstract. The orientation and tectonic regime of the observed crustal/lithospheric stress field contribute to our knowledge of different deformation processes occurring within the Earth's crust and lithosphere. In this study, we analyze the influence of the thermal and density structure of the upper mantle on the lithospheric stress field and topography. We use a 3D lithosphereasthenosphere numerical model with power-law rheology, coupled to a spectral mantle flow code at 300 km depth. Our results are validated against the World Stress Map 2016 and the observation-based residual topography. We derive the upper mantle 5 thermal structure from either a heat flow model combined with a sea floor age model (TM1) or a global S-wave velocity model (TM2). We show that lateral density heterogeneities in the upper 300 km have a limited influence on the modeled horizontal stress field as opposed to the resulting dynamic topography that appears more sensitive to such heterogeneities. There is hardly any difference between the stress orientation patterns predicted with and without consideration of the heterogeneities in the upper mantle density structure across North America, Australia, and North Africa. In contrast, we find that the dynamic 10 topography is to a greater extent controlled by the upper mantle density structure. After correction for the chemical depletion of continents, the TM2 model leads to a much better fit with the observed residual topography giving a correlation of 0.51 in continents, but this correction leads to no significant improvement in the resulting lithosphere stresses. In continental regions with abundant heat flow data such as, for instant, Western Europe, TM1 results in relatively a small angular misfits of 18.30

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Section: Introductionmentioning

confidence: 99%

Section: = 23mentioning

confidence: 99%

Section: = 23mentioning

confidence: 99%

Section: = 23mentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Effects of upper mantle heterogeneities on lithospheric stress field and dynamic topography

Tutu¹,

Steinberger²,

Sobolev³

et al. 2017

Preprint

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Evolution of the northern Argentine margin during the Cenozoic controlled by bottom current dynamics and gravitational processes

Gruetzner

Uenzelmann-Neben

Franke

2016

Geochem Geophys Geosyst

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A detailed reflection seismic investigation on sediment deposition at the northern Argentine margin (37°S to 42°S) resolves major modifications in oceanographic circulation during the Cenozoic, which resulted from variations in both climatic and tectonic processes. After an extensive erosional period following the onset of glaciation of Antartica at ~34 Ma, which affected all water depth levels, a buried elongated mounded drift within the continental shelf was shaped by bottom current activity during the Miocene. This may represent the earliest deposits of the Malvinas Current that branches from the Antartic Circumpolar Current and today is part of a complex shallow water circulation system known as the Brazil-Malvinas confluence. At the same time a major terrace grew to its present form on the upper slope indicating that a precursor of Antarctic Intermediate Water was also part of the BrazilMalvinas confluence. After another major erosional phase inferred from a seismic unconformity at ~6 Ma, sheeted drifts, mounded drifts and sediment waves formed at the continental rise during the Pliocene/Pleistocene. These extensive contourite deposits are diagnostic for a steady north setting bottom flow at the depth level of todays Antarctic Bottomwater. Evidence for downslope transport mainly stems from the presence of buried turbidites and canyon related depocenters. These features can be related to Andean uplift during the Eocene and to the activation of the canyon system during the Pliocene.

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Large fluctuations of shallow seas in low-lying Southeast Asia driven by mantle flow

Zahirovic

Flament

Müller

et al. 2016

Geochem. Geophys. Geosyst.

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The Sundaland continental promontory, as the core of Southeast Asia, is one of the lowest lying continental regions, with half of the continental area presently inundated by a shallow sea. The role of mantle convection in driving long-wavelength topography and vertical motion of the lithosphere in this region has often been ignored when interpreting regional stratigraphy, including a widespread Late Cretaceous-Eocene unconformity, despite a consensus that Southeast Asia is presently situated over a large-amplitude dynamic topography low resulting from long-term post-Pangea subduction. We use forward numerical models to link mantle flow with surface tectonics and compare predicted trends of dynamic topography with eustasy and regional paleogeography to determine the influence of mantle convection on regional basin histories. A Late Cretaceous collision of Gondwana-derived terranes with Sundaland choked the active margin, leading to slab breakoff and a 10-15 Myr-long subduction hiatus. A subduction hiatus likely resulted in several hundred meters of dynamic uplift and emergence of Sundaland between 80 and 60 Ma and may explain the absence of a Late Cretaceous-Eocene sedimentary record. Renewed subduction from 60 Ma reinitiated dynamic subsidence of Sundaland, leading to submergence from 40 Ma despite falling long-term global sea levels. Our results highlight a complete ''down-up-down'' dynamic topography cycle experienced by Sundaland, with transient dynamic topography manifesting as a major regional unconformity in sedimentary basins.

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Global dynamic topography observations reveal limited influence of large-scale mantle flow

Cited by 178 publications

References 48 publications

Effects of upper mantle heterogeneities on lithospheric stress field and dynamic topography

Effects of upper mantle heterogeneities on lithospheric stress field and dynamic topography

Evolution of the northern Argentine margin during the Cenozoic controlled by bottom current dynamics and gravitational processes

Large fluctuations of shallow seas in low-lying Southeast Asia driven by mantle flow

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