A plate tectonic scenario for the Iapetus and Rheic oceans

Domeier, Mathew

doi:10.1016/j.gr.2015.08.003

Cited by 162 publications

(127 citation statements)

References 125 publications

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“…Paleomagnetic results from the core and southern limb of the Central Iberian curve show an overall rotation that fits with the attitude of the southern limb of the Cantabrian Orocline (Pastor-Galán et al, 2015b;2016;. However, the timing constraints provided by these results established that no differential rotation occurred younger than ca.…”

mentioning

confidence: 53%

Late Paleozoic Iberian orocline(s) and the missing shortening in the core of Pangea. Paleomagnetism from the Iberian Range.

Pastor‐Galán¹,

Pueyo²,

Diederen³

et al. 2018

Preprint

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Supercontinents are usually interpreted to be single and rigid continental plates. How and when Pangea became a rigid supercontinent is disputed, and age estimations vary from ~330 to ~240 Ma.The Gondwana-Laurussia collision formed the Variscan-Alleghanian belt, the most prominent witness of Pangea's amalgamation. In Iberia, this orogen draws an "S" shape featured by the Once the Cenozoic rotation is restored, the change in structural trend that allegedly evidences the outer arc of the Central Iberian curve disappears. Whereas the Cenozoic rotation is incompatible with a Central Iberian curve, the Late Carboniferous rotation is fully compatible with the Cantabrian Orocline, enlarging the area affected by its counterclockwise rotations and the existence of a non-rigid Pangea until, at least, ~295 M.a.

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mentioning

confidence: 53%

Late Paleozoic Iberian orocline(s) and the missing shortening in the core of Pangea. Paleomagnetism from the Iberian Range.

Pastor‐Galán¹,

Pueyo²,

Diederen³

et al. 2018

Preprint

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“…Some paleontological, provenance, and paleomagnetic data indicate that the originally peri‐Amazonian Avalonian terranes were docked at the northern periphery of the West African craton in the Middle Cambrian (ca. 530 Ma; e.g., Barr et al, ; Domeier, ; Keppie & Keppie, ; Landing, ; Zlatkin et al, ).…”

Section: Previous Studies and Geological Settingsmentioning

confidence: 99%

“…It is widely accepted that the originally peri‐North‐African Cadomian terranes (as a part of the Hun superterrane: Stampfli et al, ; or the Galatian terranes: Stampfli et al, , or the Armorican Terrane Assemblage: Franke, ; Tait et al, ), in contrast to the Avalonian, remained proximal to Gondwana (e.g., Domeier, ; Linnemann et al, ) at least till the Late Silurian, while they were detached from Gondwana by the Paleotethys opening.…”

Section: Previous Studies and Geological Settingsmentioning

confidence: 99%

New Detrital Zircon Geochronology From the Cycladic Basement (Greece): Implications for the Paleozoic Accretion of Peri‐Gondwanan Terranes to Laurussia

2018

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Between the eastern Mediterranean basin in the South and the East European (Baltica) Craton to the north, we distinguish two fundamental pre‐Variscan geological domains: an Internal domain, which hosts Ordovician‐Devonian (450–400 Ma) igneous rocks and detrital zircon populations, and an External domain, which contains no 450‐ to 400‐Ma zircon ages. From the Balkan Peninsula to the Turkish plate, the aforementioned Internal domain includes the Serbo‐Macedonian Massif, the Istanbul and Sakarya terranes, whereas the External domain, holding a more distal position relative to Baltica, includes the Pelagonian terrane and the External Hellenides. The two domains are interpreted as two consecutive (i.e., Caledonian and Variscan) Paleozoic accretionary belts, attached to the southern margin of Baltica. The Cycladic and Pelagonian terranes are currently juxtaposed along strike of the central Hellenides in Northern Greece. The Cycladic Massif is a Cadomian‐type terrane, while the Pelagonian displays an Avalonian‐type affinity. Despite its Avalonian affinity, the Pelagonian lacks Ordovician‐Devonian (450–400‐Ma) zircon ages. In contrast, detrital zircon grains of such ages are abundant in the Cycladic Massif. In this study, the Ordovician‐Devonian detrital zircon population is recognized also in pre‐Variscan (>310‐Ma) Cycladic Basement from Ios and Naxos Islands, affiliating the Cycladic Massif with the Internal (Caledonian) domain. This indicates that the Caledonian accretion incorporated some Cadomian‐type terranes. It also suggests that the protolith of the Cycladic blueschists was deposited within the Internal domain, that is, northeast of the Pelagonian terrane. This recognition helps to reconstruct the Paleozoic and Mesozoic paleogeography of the peri‐Gondwanan terranes.

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“…The North Atlantic realm underwent episodic continental extension in the Permo-Triassic, Late Jurassic, and Early and mid-Cretaceous, with reactivation and basin formation influenced by pre-existing structures formed during the closure of the Iapetus Ocean (and part of the Rheic Ocean: e.g. Domeier 2015), and subsequent Baltica -Laurentia collision (e.g. Doré et al 1997;Skogseid et al 2000).…”

mentioning

confidence: 99%

Break-up and seafloor spreading domains in the NE Atlantic

Gaina

Nasuti

Kimbell

et al. 2017

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An updated magnetic anomaly grid of the NE Atlantic and an improved database of magnetic anomaly and fracture zone identifications allow the kinematic history of this region to be revisited. At break-up time, continental rupture occurred parallel to the Mesozoic rift axes in the south, but obliquely to the previous rifting trend in the north, probably due to the proximity of the Iceland plume at 57-54 Ma.The new oceanic lithosphere age grid is based on 30 isochrons (C) from C24n old (53.93 Ma) to C1n old (0.78 Ma), and documents ridge reorganizations in the SE Lofoten Basin, the Jan Mayen Fracture Zone region, in Iceland and offshore Faroe Islands. Updated continent -ocean boundaries, including the Jan Mayen microcontinent, and detailed kinematics of the EocenePresent Greenland-Eurasia relative motions are included in this model.Variations in the subduction regime in the NE Pacific could have caused the sudden northwards motion of Greenland and subsequent Eurekan deformation. These events caused seafloor spreading changes in the neighbouring Labrador Sea and a decrease in spreading rates in the NE Atlantic. Boundaries between major oceanic crustal domains were formed when the European Plate changed its absolute motion direction, probably caused by successive adjustments along its southern boundary.

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A plate tectonic scenario for the Iapetus and Rheic oceans

Cited by 162 publications

References 125 publications

Late Paleozoic Iberian orocline(s) and the missing shortening in the core of Pangea. Paleomagnetism from the Iberian Range.

Late Paleozoic Iberian orocline(s) and the missing shortening in the core of Pangea. Paleomagnetism from the Iberian Range.

New Detrital Zircon Geochronology From the Cycladic Basement (Greece): Implications for the Paleozoic Accretion of Peri‐Gondwanan Terranes to Laurussia

Break-up and seafloor spreading domains in the NE Atlantic

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