Non-hotspot formation of volcanic chains: control of tectonic and flexural stresses on magma transport

Hieronymus, Christoph F.; Bercovici, David

doi:10.1016/s0012-821x(00)00227-2

Cited by 67 publications

(70 citation statements)

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“…An extended discussion on the origin of the magmatic provinces in West Africa, and in the Air-CL line is provided in Ngako et al (2006) and only summarized in this section. Following Hieronymus & Bercovici (2000) model, the spreading ridge of the proto Atlantic Ocean during Barremian offers a tentative explanation for the SW-NE Nigeria-BT-CL parallel trends which is susceptible to take into account the whole geometry and structure of the intraplate magmatism in West and Central-Africa. This model predicts island chains aligned with a deviatorically tensile tectonic stress perpendicular to the ridge; the thin elastic lithosphere near the ridge is subjected to strong deviatorically tensile stress field perpendicular to the ridge axis.…”

Section: Continental Breaking and Possible Links With Magmatic Chainsmentioning

confidence: 99%

“…This initial perturbation may be provided by a change in the tectonic stress field due to plate motion reorganization (which is amplified locally by an inhomogeneity in the lithosphere), the formation of a small sublithospheric melting anomaly or a change in convection. Hieronymus & Bercovici (2000) have finally shown that multiple lines of volcanoes can result from interaction of flexural, membrane and tectonic stresses. Indeed: i) due to tensile membrane stresses, several volcanoes typically form in the space between any two volcanoes of the initial chain; ii) membrane stresses perpendicular to the axis of the ridge also interact with the flexural stresses to generate volcanism away from the axis.…”

Section: Continental Breaking and Possible Links With Magmatic Chainsmentioning

confidence: 99%

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Plates Amalgamation and Plate Destruction, the Western Gondwana History

Ngako¹,

Njonfang²

2011

Tectonics

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Tectonics 4This study involves modern structural analysis and concepts (phase chronology, strain analysis, deformation and kinematics), petrology (metamorphic parageneses and phase equilibrium, relation with deformation, geothermobarometry), geochemistry (major and trace elements) and geochronology. Data from regional literature including geophysical data are also abundantly used for synthesis and re-interpretation. The most important achievements include: 1. A new tectonic model for the Pan-African/Brasiliano belts; this model includes many original aspects and developments with regards to the collisional setting, tectonics, metamorphic and magmatic processes. In particular, a three-plate model is proposed, and the role of the asthenosphere on crustal melting and reactivation during collision is emphasized. 2. Evidence of a tectonic indent in the central Nigeria-Cameroon domain, inferred from the regional strain field; indentation in central-west Africa strongly suggests that the East Saharan Block (ESB) evolved originally as a rigid prong prior to crustal melting, batholiths emplacement and subsequent dismantling of the prong during the late PanAfrican evolution. 3. Clear distinction between Pan-African and Post Pan-African tectonic and magmatic processes which raises the question on the relevance of integrating Phanerozoic lithospheric structures inferred from geophysical data (gravity, seismic tomography, etc.) in the interpretation and reconstruction of the Pan-African tectonic evolution. Future research would be focused on the Central Cameroon Shear Zone (CCSZ) kinematics and the characterization of vestiges of the dismantled SFCC/ESB cratons and hypothetic pre-tectonic boundaries.

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Section: Continental Breaking and Possible Links With Magmatic Chainsmentioning

confidence: 99%

Section: Continental Breaking and Possible Links With Magmatic Chainsmentioning

confidence: 99%

Plates Amalgamation and Plate Destruction, the Western Gondwana History

Ngako¹,

Njonfang²

2011

Tectonics

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“…An alternative view is that hotspot volcanism represents shear-stress driven upwelling within the lithosphere (e.g. Hieronymus & Bercovici 2000;Ballmer et al 2013) due to hotspotridge interaction (Kopp et al 2003;O'Connor et al 2015) and due to changes in slab-pull forces induced by plate-re-organization (Wessel & Kroenke 2007), intraplate volcanism as a by-product of plate tectonics itself (e.g. Anderson 2000;Foulger & Natland 2003), or hotspot volcanism as precursor for a break-apart of the Pacific Plate (Clouard & Gerbault 2008).…”

Section: Introductionmentioning

confidence: 99%

The Manihiki Plateau—a key to missing hotspot tracks?

Pietsch

Uenzelmann-Neben

2016

Geophys. J. Int.

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“…Courtillot et al, 2003;Campbell, 2001, Richards et al, 1989. The melt source is the hot buoyant plume.Other models propose that age progressive seamount chains may be the result of tensional stresses, tectonic cracking of the oceanic plate, or horizontal dike propagation extending pre-existing features (e.g., Favela and Anderson, 1999; Natland and Winterer, 2005;Fairhead and Wilson, 2005;Hieronymus and Bercovici, 2000). The development of a chain results from the propagation of the crack or dike in response to the stress field across the plate.…”

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confidence: 99%

Ridge-crossing seamount chains: A nonthermal approach

Beutel¹,

Anderson²

2007

Special Paper 430: Plates, Plumes and Planetary Processes

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Ridge-crossing seamount chains; a non-thermal approachIn this paper we examine whether it is viable to form an age-progressive ridge crossing seamount chain using a non-plume mechanism. Non-thermal melt sources considered include fertile mantle blobs and sub-solidus mantle while lithospheric stresses generated at the ridge and at ridge-transform intersections are tapped to bring the mantle to the surface. Finite element models, analog models, and an analysis of the Tristan de Cunha chain all show that ridge-crossing seamount chains may be created using these mechanisms. Essentially, as a ridge migrates or reorganizes excess magmatism may appear to switch sides of the ridge as areas of extensional stress at the ridge-transform intersection migrate with the ridge.. INTRODUCTIONHypotheses for ridge-crossing seamount chains have focused on the interaction of mantle plumes with migrating ridge segments (DePaolo & Manga, 2003;Sleep 2002b).These hypotheses call for a stationary plume of hot mantle material that rises to the base of the lithosphere and creates a chain of age-progressive seamounts in the middle of the plate. As a migrating ridge approaches the plume, buoyant mantle material rises along the base of the lithosphere like a helium balloon along a cathedral ceiling to the ridge and age progressive chains of seamounts are created on both sides of the ridge from a single hotspot source. Eventually the ridge moves away from the plume and seamount production switches across the ridge to the other plate, ceases to generate seamounts on 2 the ridge, and continues to generate seamounts on the new plate only (e.g., DePaolo & Manga, 2003;Sleep 2002b;Ribe et al., 1996;Kincaid et al., 1996;Small, 1995). This scenario results in the formation of an asymmetrical V-shaped array of seamounts such as the Tristan de Cunha chain in the South Atlantic (Figure 1).Because current non-thermal models of seamount formation are unable to explain this geometry, (e.g. propagating cracks are presumed to be unable to cross ridges, and asthenospheric heterogeneities are presumed to be moving rapidly), ridge-crossing seamount chains have been cited as evidence for plumes of material that remain relatively stationary in comparison to the plates. However, if the mantle is lithologically heterogeneous and contains areas with different melting points on a scale from km to 100's of km and/or if ridge-transform intersections are involved, then non-thermal ridgecrossing seamount chains are not only viable, but also likely. In this paper we propose a mechanism for the development of ridge-crossing seamount chains that does not invoke deep mantle plumes yet still accounts for the four primary elements necessary for a viable hypothesis for the origin of seamount chains ranging in size from 2 or 3 seamounts to seamount chains spanning a 100 Ma. The primary elements included in this mechanism are; a source of melt, a means of bringing melt to the surface, an asymmetrical ridgecrossing seamount chain, and an explanation for the age progressive nature o...

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Non-hotspot formation of volcanic chains: control of tectonic and flexural stresses on magma transport

Cited by 67 publications

References 48 publications

Plates Amalgamation and Plate Destruction, the Western Gondwana History

Plates Amalgamation and Plate Destruction, the Western Gondwana History

The Manihiki Plateau—a key to missing hotspot tracks?

Ridge-crossing seamount chains: A nonthermal approach

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