Mantle Flow as a Trigger for Subduction Initiation: A Missing Element of the Wilson Cycle Concept

Baes, Marzieh; Sobolev, S. V.

doi:10.1002/2017gc006962

Cited by 39 publications

(43 citation statements)

References 42 publications

(58 reference statements)

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“…Notably, a "trench jump" after collision is predicted in some of the models (Tetreault & Buiter, 2012;Vogt & Gerya, 2014;Yang et al, 2018), which is however caused by the detachment of weak and buoyant crust of the accreting terrane, rather than initiating a new subduction zone in the neighboring oceanic plate. Another type of model focuses on the SI at passive continental margins, which only deal with two plates and a transition between them (e.g., Baes & Sobolev, 2017;Nikolaeva et al, 2011;Rey et al, 2014;Toth & Gurnis, 1998;Ulvrova et al, 2019;Zhong & Li, 2019). These models indicate that the SI at passive continental margin is not easy, which generally requires special conditions, for example, (1) a thin, weak, and very buoyant continental lithosphere (e.g., Nikolaeva et al, 2011;Marques et al, 2013Marques et al, , 2014Rey et al, 2014); (2) a prescribed weak transition zone between the continental and oceanic plates (e.g., Baes et al, 2011;Toth & Gurnis, 1998); (3) driven by downward mantle flow (e.g., Baes & Sobolev, 2017); or (4) driven by a boundary stress/force (e.g., Zhong & Li, 2019).…”

Section: Introductionmentioning

confidence: 99%

“…Another type of model focuses on the SI at passive continental margins, which only deal with two plates and a transition between them (e.g., Baes & Sobolev, 2017;Nikolaeva et al, 2011;Rey et al, 2014;Toth & Gurnis, 1998;Ulvrova et al, 2019;Zhong & Li, 2019). These models indicate that the SI at passive continental margin is not easy, which generally requires special conditions, for example, (1) a thin, weak, and very buoyant continental lithosphere (e.g., Nikolaeva et al, 2011;Marques et al, 2013Marques et al, , 2014Rey et al, 2014); (2) a prescribed weak transition zone between the continental and oceanic plates (e.g., Baes et al, 2011;Toth & Gurnis, 1998); (3) driven by downward mantle flow (e.g., Baes & Sobolev, 2017); or (4) driven by a boundary stress/force (e.g., Zhong & Li, 2019). On the other hand, the natural examples of Atlantic and Indian passive margins, neighboring to relatively old oceanic lithospheres, are generally stable and difficult for SI (Cloetingh et al, 1989;Mueller & Phillips, 1991;Niu et al, 2003;Zhong & Li, 2019).…”

Section: Introductionmentioning

confidence: 99%

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Subduction Initiation During Collision‐Induced Subduction Transference: Numerical Modeling and Implications for the Tethyan Evolution

Zhong

2020

JGR Solid Earth

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The collision‐induced subduction transference is a composite dynamic process including both the terrane collision/accretion and the subduction initiation (SI) at the neighboring passive margin. This process occurred repeatedly during the evolution of Tethyan systems, with multiple ribbon‐like continents or microcontinents drifting from Gondwana in the southern hemisphere and accreting to the Eurasian continent since Paleozoic. In the previous numerical studies, the dynamics of terrane collision and induced SI are investigated individually, which however need to be integrated to study the controlling factors and time scales of collision‐induced subduction transference. Systematic numerical models are conducted with variable properties of converging plates and different boundary conditions. The model results indicate that the forced convergence, rather than pure free subduction, is required to trigger and sustain the SI at the neighboring passive margin after terrane collision. In addition, a weak passive margin can significantly promote the occurrence of SI, by decreasing the required boundary force to reasonable value of plate tectonics. The lengths of subducted oceanic slab and accreting terrane play secondary roles in the occurrence of SI after collision. Under the favorable conditions of collision‐induced subduction transference, the time required for SI after collision is generally short within 10 Myr, which is consistent with the general geological records of Cimmerian collision and the following Neo‐Tethyan SI. In contrast, the stable Indian passive margin and absence of SI in the present Indian Ocean may be due to the low convergent force and/or the lack of proper weak zones, which remains an open question.

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Section: Introductionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

Subduction Initiation During Collision‐Induced Subduction Transference: Numerical Modeling and Implications for the Tethyan Evolution

Zhong

2020

JGR Solid Earth

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“…They argued that the Earth-like asymmetric subduction mode occurs for lids with friction angles of larger than 15 • and moderate thermal ages. Baes & Sobolev (2017) proposed mantle suction flow as a triggering factor for subduction initiation on the present-day Earth. Using 2-D numerical models, they showed that a new subduction zone can be initiated along a passive margin or fracture zone/transform fault if a suction flow exists below or near these localities.…”

Section: Introductionmentioning

confidence: 99%

Subduction initiation in mid-ocean induced by mantle suction flow

Baes

Sobolev

Quinteros

2018

Geophysical Journal International

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Pre-existing weakness zones in the lithosphere such as transform faults/fracture zones and extinct mid-oceanic ridges have been suggested to facilitate subduction initiation in an intraoceanic environment. Here, we propose that the additional forcing coming from the mantle suction flow is required to trigger the conversion of a fracture zone/transform fault into a converging plate boundary. This suction flow can be induced either from the slab remnants of former converging plate boundaries or/and from slabs of neighbouring active subduction zones. Using 2-D coupled thermo-mechanical models, we show that a sufficiently strong mantle flow is able to convert a fracture zone/transform fault into a subduction zone. However, this process is feasible only if the fracture zone/transform fault is very close to the midoceanic ridge. Our numerical model results indicate that time of subduction initiation depends on the velocity, domain size and location of mantle suction flow and age of the oceanic plate.

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“…This case exemplified the role of 3D far-field 25 tectonics during subduction infancy (Table 1), and the potential role of deep mantle flows. Upward and downward mantle flows, even far away from the initiation site, have be shown to be able to initiate subduction in 2D models (Lu et al, 2015;Baes and Sobolev, 2017). On the other hand, studies in 3D by Boutelier and Beckett (2018); Zhou et al (2018) showed that subduction initiation depends on along-strike variations in plate structure.…”

Section: Model Limitationsmentioning

confidence: 99%

Can subduction initiation at a transform fault be spontaneous?

Arcay¹,

Lallemand²,

Abecassis³

et al. 2019

Preprint

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Abstract. We propose a new exploration of the concept of spontaneous subduction, i.e., lithospheric gravitational collapse without any external forcing, at a transform fault (TF). We first seek candidates in recent subduction initiations at a TF that could fulfill the criteria of spontaneous subduction and retain 3 natural cases: Izu-Bonin-Mariana (IBM), Yap, and Matthew & Hunter. We next perform an extensive exploration of conditions allowing spontaneous gravitational sinking of the older plate in a oceanic TF using 2D thermo-mechanical simulations. Our parametric study aims at better deliminating the ranges of mechanical properties necessary to achieve the old plate sinking (OPS). The explored parameter set includes: crust and TF densities, brittle and ductile rheologies, and width of the weakened region around the TF. We focus on characterising OPS conditions in terms on (1) reasonable vs unrealistic values of mechanical parameters and (2) comparison to modern cases of subduction initiation in a TF setting. When modelled, OPS initiates following one of two distinct modes, depending mainly on the thickness of the overlying younger plate (YP). Asthenosphere may rise up to the surface above the sinking old plate provided that the YP remains motionless (verified for ages ≥ 5 Myr, mode 1). For lower YP ages (typically ≤ 2 Myr), the YP is dragged towards the OP resulting in a double-sided subduction (mode 2). When triggered, spontaneous OPS is extremely fast. The basic parameters to simulate OPS are the brittle properties of the shallow part of the lithosphere, controlling the plate resistance to bending, the distance away from the TF over which weakening is expected, and crust density. We find that all mechanical parameters have to be assigned extreme values to achieve OPS, that we consider as irrelevant. Furthermore, we point out inconsistencies between the processes and consequences of lithospheric instability as modelled in our experiments and geological observations of subduction infancy for the 3 natural candidates of subduction initiation by spontaneous OPS. We conclude that spontaneous instability of the thick OP at a TF evolving into mature subduction is an unlikely process of subduction initiation at modern Earth conditions.

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Mantle Flow as a Trigger for Subduction Initiation: A Missing Element of the Wilson Cycle Concept

Cited by 39 publications

References 42 publications

Subduction Initiation During Collision‐Induced Subduction Transference: Numerical Modeling and Implications for the Tethyan Evolution

Subduction Initiation During Collision‐Induced Subduction Transference: Numerical Modeling and Implications for the Tethyan Evolution

Subduction initiation in mid-ocean induced by mantle suction flow

Can subduction initiation at a transform fault be spontaneous?

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