Analogue modeling of lithospheric-scale orocline buckling: Constraints on the evolution of the Iberian-Armorican Arc

Pastor‐Galán, Daniel; Gutiérrez-Alonso, Gabriel; Zulauf, Gernold; Zanella, Friedhelm E.

doi:10.1130/b30640.1

Cited by 57 publications

(33 citation statements)

References 126 publications

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“…Illite crystallinity and conodont color alteration indexes are consistent with diagenetic conditions to very low grade metamorphism (e.g., García‐López et al, ; Pastor‐Galán et al, ). The Cantabrian Zone is mostly preserved in NW Iberia in the core of the Cantabrian Orocline (Figure 1a; Pastor‐Galan, Gutierrez‐Alonso, Zulauf, et al, ), but it also crops out in areas of the Aragonese Branch of the Iberian Range in East Iberia (Figure 1b; Calvín‐Ballester & Casas‐Sainz, ; Carls, , ), where we performed our study (Figures 1b and ).…”

Section: Tectonic and Geological Settingsmentioning

confidence: 95%

Late Paleozoic Iberian Orocline(s) and the Missing Shortening in the Core of Pangea. Paleomagnetism From the Iberian Range

et al. 2018

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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 Cantabrian Orocline and the Central Iberian curve. The curvature of Central Iberia is particularly evident in Galicia-Trás-os-Montes and in a change of trend that it draws in the Aragonese Branch of the Iberian Range. Recent research showed that both curvatures are not coeval and that the Central Iberian curve had to form prior to ca. 318 Ma (i.e., not a secondary orocline). We report paleomagnetic and structural results from Paleozoic rocks in the Santa Cruz syncline (Aragonese Branch of the Iberian Range) that indicate two main vertical axis rotations events: (1) a Cenozoic (Alpine) clockwise rotation of >20°and (2) a late Carboniferous counterclockwise rotation of 70°. 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 nonrigid Pangea until, at least,~295 Ma.Plain Language Summary Supercontinents like Pangea are thought to be rigid and stable in its interiors. It is not clear, however, when the supercontinents achieve its final rigid and sturdy form. There is a debate on when Pangea became a rigid supercontinent; some people argue that it happened as soon as 330 million years ago and others as recently as 240. The Iberian peninsula witnessed all this process, and today, we still can see the relic of the mountain range formed at that time with an "S" shape. Recent research showed that both north and south curvatures did not form coevally and that the southern curve formed before 318 Ma. We report paleomagnetic and structural results from Paleozoic rocks in the Aragonese Branch of the Iberian Range that indicate that the change in trend that allegedly evidences the southern curve of this "S" shape is a much later effect of Alpine tectonics. Altogether, the results show that Pangea was not rigid until at least 290 million years ago.

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Section: Tectonic and Geological Settingsmentioning

confidence: 95%

Late Paleozoic Iberian Orocline(s) and the Missing Shortening in the Core of Pangea. Paleomagnetism From the Iberian Range

et al. 2018

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“…Another debate concerns the relationships between the Amorican and Iberian branches of the Variscan system. The most popular interpretation is that the Variscan orogen formed an orocline (Pastor-Galan et al, 2012), which is supported by the lack of Variscan overprint on the Newfoundland margin. The drilling of Culm-type sediments, characteristic for the Variscan foreland, at ODP Site 1069 along the deep Iberia margin supports this interpretation (for location see Fig.…”

Section: The Role Of Variscan Inheritance In Structuring the Alpine Tmentioning

confidence: 98%

The role of inheritance in structuring hyperextended rift systems: Some considerations based on observations and numerical modeling

Manatschal

Lavier²,

Chenin³

2015

Gondwana Research

166

112

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International audienceA long-standing question in Earth Sciences is related to the importance of inheritance in controlling tectonic processes. In contrast to physical processes that are generally applicable, assessing the role of inheritance suffers from two major problems: firstly, it is difficult to appraise without having insights into the history of a geological system; and secondly all inherited features are not reactivated during subsequent deformation phases. Therefore, the aim of this paper is to give some conceptual framework about how inheritance may control the architecture and evolution of hyperextended rift systems.In this paper, we use the term inheritance to refer to the difference between an “ideal” layer-cake type lithosphere and a “real” lithosphere containing heterogeneities. The underlying philosophy of this work is that the evolution of hyperextended rift systems reflects the interplay between their inheritance (innate/“genetic code”) and the physical processes at play (acquired/external factors). Thus, by observing the architecture and evolution of hyperextended rift systems and integrating the physical processes, one may get hints on what may have been the original inheritance of a system.We first define 3 types of inheritance, namely structural, compositional and thermal inheritance and develop a simple and robust terminology able to describe and link observations made at different scales using geological, geophysical and modeling approaches. To this, we add a definition of rift-induced processes, i.e. processes leading to compositional changes during rifting (e.g. serpentinization or decompression melting). Using this approach, we focus on 3 well-studied rift systems that are the Alpine Tethys, Pyrenean–Bay of Biscay and Iberia–Newfoundland rift systems. However, as all these examples are magma-poor, hyperextended rift systems that evolved over a Variscan lithosphere the concepts developed in this paper cannot be applied universally. For the studied examples we can show that:1) the inherited structures did not significantly control the location of breakup2) the inherited thermal state may control the mode and architecture of rift systems, in particular the architecture of the necking zone3) the architecture of the necking zone may be influenced by the distribution and importance of ductile layers during decoupled deformation and is consequently controlled by the thermal structure and/or the inherited composition of the crust4) conversely, the deformation in hyperextended domains is strongly controlled by weak hydrated minerals (e.g. clay, serpentinite) that result from the breakdown of feldspar and olivine due to fluid and reaction assisted deformation5) inherited structures, in particular weaknesses, are important in controlling strain localization on a local scale and during early stages of rifting6) inherited mantle composition and rift-related mantle processes may control the rheology of the mantle, the magmatic budget, the thermal structure and the localization of final rifting.Thes...

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“…The origin of curved orogenic belts (oroclines) is a contentious issue that has attracted much attention in recent literature [e.g., Johnston et al, 2013;Rosenbaum, 2014]. A large volume of publications, particularly those that deal with Paleozoic oroclines in Variscan Europe and central Asia, assume that oroclinal bending has involved buckling of the whole lithosphere in response to orogen-parallel compression [Xiao et al, 2010;Gutiérrez-Alonso et al, 2012;Pastor-Galán et al, 2012;Weil et al, 2013]. In contrast, other models suggest that the origin of many oroclines was intimately linked to trench retreat and associated back-arc extension [Royden, 1993;Lonergan and White, 1997;Rosenbaum and Lister, 2004;Schellart and Lister, 2004;Morra et al, 2006;Rosenbaum, 2014].…”

Section: Introductionmentioning

confidence: 99%

Orocline‐driven transtensional basins: Insights from the Lower Permian Manning Basin (eastern Australia)

et al. 2016

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The New England Orogen in eastern Australia exhibits an oroclinal structure, but its geometry and geodynamic evolution are controversial. Here we present new data from the southernmost part of the oroclinal structure, the Manning Orocline, which supposedly developed in the Early Permian, contemporaneously and/or shortly after the deposition of the Lower Permian Manning Basin. New U‐Pb detrital zircon data provide a maximum depositional age of ~288 Ma. Structural evidence from rocks of the Manning Basin indicates that both bedding and preoroclinal fold axial planes are approximately oriented parallel to the trace of the Manning Orocline. Brittle deformation was dominated by sinistral strike‐slip faulting, particularly along a major fault zone (Peel‐Manning Fault System), which is marked by the occurrence of a serpentinitic mélange, and separates tectonostratigraphic units of the New England Orogen. Our revised geological map shows that the Manning Basin is bounded by faults and serpentinites, thus indicating that basin formation was intimately linked to deformation along the Peel‐Manning Fault System. The Manning Basin is thus interpreted to be a transtensional pull‐apart basin associated with the Peel‐Manning Fault System. Age constraints and structural relationships indicate that basin formation likely occurred during the incipient stage of oroclinal bending, with block rotations and fragmentation of the transtensional pull‐apart system occurring subsequently. The intimate link between oroclinal bending and basin formation in the New England oroclines indicates that back‐arc extension, accompanied by transtensional deformation, could have played an important role in the early stage of orocline development.

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Analogue modeling of lithospheric-scale orocline buckling: Constraints on the evolution of the Iberian-Armorican Arc

Cited by 57 publications

References 126 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

The role of inheritance in structuring hyperextended rift systems: Some considerations based on observations and numerical modeling

Orocline‐driven transtensional basins: Insights from the Lower Permian Manning Basin (eastern Australia)

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