Advantages of a conservative velocity interpolation (CVI) scheme for particle‐in‐cell methods with application in geodynamic modeling

Wang, Hongliang; Agrusta, Roberto; Hunen, Jeroen van

doi:10.1002/2015gc005824

Cited by 60 publications

(35 citation statements)

References 34 publications

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“…Shear heating is not included (see section ). Composition is tracked by tracers that are conservatively advected (i.e., such that the divergence of the velocity field, interpolated from the element nodes, is always 0) with the flow field (Wang et al, ).…”

Section: Methodsmentioning

confidence: 99%

Modeling Slab Temperature: A Reevaluation of the Thermal Parameter

Maunder

Hunen

Bouilhol

et al. 2019

Geochem Geophys Geosyst

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We reevaluate the effects of slab age, speed, and dip on slab temperature with numerical models. The thermal parameter Φ = t v sin θ, where t is age, v is speed, and θ is angle, is traditionally used as an indicator of slab temperature. However, we find that an empirically derived quantity, in which slab temperature T ∝ log (t −a v −b ) , is more accurate at depths <120 km, with the constants a and b depending on position within the slab. Shallower than the decoupling depth (~70-80 km), a~1 and b~0, that is, temperature is dependent on slab age alone. This has important implications for the early devolatilization of slabs in the hottest (youngest) cases and for shallow slab seismicity. At subarc depths (~100 km), within the slab mantle, a~1 and b~0 again. However, for the slab crust, now a~0.5 and b~1, that is, speed has the dominant effect. This is important when considering the generation of arc magmatism, and in particular, slab melting and the generation of slab-derived melange diapirs. Moving deeper into the Earth, the original thermal parameter performs well as a temperature indicator, initially in the core of the slab (the region of interest for deep water cycling). Finally, varying the decoupling depth between 40 and 100 km has a dominant effect on slab temperatures down to 140-km depth, but only within the slab crust. Slab mantle temperature remains primarily dependent on age.

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Section: Methodsmentioning

confidence: 99%

Modeling Slab Temperature: A Reevaluation of the Thermal Parameter

Maunder

Hunen

Bouilhol

et al. 2019

Geochem Geophys Geosyst

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“…The slab-transition zone interaction is studied with 2D self-consistent subduction simulations using the finite-element code CITCOM 59 – 61 . The code solves the system of conservation of mass, momentum, and energy equations, for an incompressible fluid, at infinite Prandtl number, under the extended Boussinesq approximation 9 , without internal heating.…”

Section: Methodsmentioning

confidence: 99%

Strong plates enhance mantle mixing in early Earth

2018

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In the present-day Earth, some subducting plates (slabs) are flattening above the upper–lower mantle boundary at ~670 km depth, whereas others go through, indicating a mode between layered and whole-mantle convection. Previous models predicted that in a few hundred degree hotter early Earth, convection was likely more layered due to dominant slab stagnation. In self-consistent numerical models where slabs have a plate-like rheology, strong slabs and mobile plate boundaries favour stagnation for old and penetration for young slabs, as observed today. Here we show that such models predict slabs would have penetrated into the lower mantle more easily in a hotter Earth, when a weaker asthenosphere and decreased plate density and strength resulted in subduction almost without trench retreat. Thus, heat and material transport in the Earth’s mantle was more (rather than less) efficient in the past, which better matches the thermal evolution of the Earth.

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“…Single‐sided subduction, lithospheric models are calculated using CITCOM code (Moresi & Gumis, ; Wang et al, ). The code uses the finite element method to solve the system of conservation of mass, momentum, and energy equations for an incompressible fluid under the extended Boussinesq approximation (Christensen & Yuen , ), infinite Prandtl number, and without internal heating

\nabla \cdot \overset{u}{true} = 0,

\nabla (][, \overset{η}{true} ()(, \nabla \overset{u}{true} + \nabla {\overset{true¯}{bold-italicu}}^{T})) - \nabla \cdot \overset{P}{true} = {\overset{true¯}{normalα}}_{z} Ra \overset{T}{true} - {Ra}_{c} \sum_{normali = 1}^{n} {Rb}_{i} {\overset{true¯}{Γ}}_{i},

(][, 1 + \sum_{normali = 1}^{n} ()(, \frac{normald {\overset{true¯}{Γ}}_{i}}{normald \overset{z}{true}} {\overset{true¯}{γ_{i}}}^{2} \frac{{Rb}_{normali}}{Ra} Di true(\overset{T}{true} + {\overset{true¯}{T}}_{s})) ()(, \frac{normalδ \overset{T}{true}}{normalδ \overset{t}{true}} + \overset{u}{true} \cdot \nabla \overset{T}{true}) = \nabla^{2} \overset{T}{true} - (][, 1 + \sum_{normali = 1}^{n} ()(, \frac{normald \overset{Γ_{i}}{true}}{normald \overset{z}{true}} {\overset{true¯}{normalγ}}_{i} {Rb}_{n...}))

…”

Section: Numerical Approach and Model Setupmentioning

confidence: 99%

“…Single-sided subduction, lithospheric models are calculated using CITCOM code (Moresi & Gumis, 1996;Wang et al, 2015). The code uses the finite element method to solve the system of conservation of mass, momentum, and energy equations for an incompressible fluid under the extended Boussinesq approximation (Christensen & Yuen, 1985), infinite Prandtl number, and without internal heating ∇·u ¼ 0;…”

Section: Governing Equations and Model Setupmentioning

confidence: 99%

Topographic Fingerprint of Deep Mantle Subduction

et al. 2020

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The dynamic topography links with the mantle structures at various temporal and spatial scales. However, it is still unclear how it relates to the dynamics of subducting lithosphere when plates reach the mantle transition zone and lower mantle. Seismic tomography images show how slab morphologies vary from sinking subvertically into the lower mantle, to lying flat above the upper-lower mantle discontinuity, to thickening in the shallow lower mantle. These slab shapes have been considered to be the result of variable interaction of the slab with the upper-lower mantle discontinuity at~670 km depth. Previous studies show that periodic deep slab dynamics can explain a variety of enigmatic geological and geophysical observations such as periodic variations of the plate velocities, trench retreat and advance episodes, and the scattered distribution of slab dip angle in the upper mantle. In this study, we use two-dimensional subduction models to investigate the surface topography expression and its evolution during slab transition zone interaction. Our models show that topography does not depend on slab morphology; indeed, the dynamic topography cannot distinguish between a slab sinking straight into the lower mantle and slab stagnation at the upper-lower mantle boundary. However, topographic oscillations are related to episodes of the trench advance and retreat, which in turn are linked to the slab folding behavior at transition zone depths. Our results suggest that the surface transient signal observed by geological studies could help to detect deep subduction dynamics.

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Advantages of a conservative velocity interpolation (CVI) scheme for particle‐in‐cell methods with application in geodynamic modeling

Cited by 60 publications

References 34 publications

Modeling Slab Temperature: A Reevaluation of the Thermal Parameter

Modeling Slab Temperature: A Reevaluation of the Thermal Parameter

Strong plates enhance mantle mixing in early Earth

Topographic Fingerprint of Deep Mantle Subduction

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