Structural and microstructural analysis of the Retortillo Syncline (Variscan belt, Central Iberia). Implications for the Central Iberian Orocline

Silva, Ícaro Días da; Barreiro, Juan Gómez; Catalán, José R. Martı́nez; Ayarza, P.; Pohl, J.; Martínez, Enrique Merino

doi:10.1016/j.tecto.2017.07.015

Cited by 19 publications

(9 citation statements)

References 48 publications

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“…The latter, on which this paper is focused, is characterized by geographical landscapes exhibiting an Appalachian geomorphological style composed of narrow synclines topped by the 'Purple Series' and the Armorican Quartzite, and broad antiforms exhibiting Ediacaran-Cambrian successions in their cores. The overall Variscan structure of the Central Iberian Zone is the overprinting result of three distinct deformation events plus a somewhat later activity related to the subvertical shear zones or to faults (Díez Balda et al, 1990;Díez Fernández & Pereira, 2016;Dias da Silva et al, 2017).…”

Section: Structural Style Of the Central Iberian Zonementioning

confidence: 99%

Updated stratigraphic framework and biota of the Ediacaran and Terreneuvian in the Alcudia-Toledo Mountains of the Central Iberian Zone, Spain

et al. 2019

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Se presenta en este trabajo una revisión actualizada de la estratigrafía del Ediacárico-Terranóvico del valle de Alcudia y los montes de Toledo, Zona Centroibérica. Se subdivide el Supergrupo infrayacente ediacárico del Alcudiense Inferior-Domo Extremeño en los Grupos del Guadiana (Formaciones de La Coronada y Sta. Ma de Zújar) y de Campanario (Formaciones de Botija, Monroy y Orellana). El supergrupo contiene varios acritarcos sin utilidad bioestratigráfica, así como dubiofósiles, pero su edad se ha establecido claramente a partir de zircones detríticos. Este litosoma siliciclástico aparece recubierto mediante contacto disconforme con el Grupo mixto de Ibor (Formaciones de Castañar, Villarta y Arrocampo) o la Formación siliciclástica del Cíjara. El contenido fósil del Grupo de Ibor incluye sabellidítidos, vendoténidos, macrofitas, bioacumulaciones y arrecifes con Cloudina, Sinotubulites, Protolagena y estromatolitos y trombolitos, así como una amplia variedad de icnofósiles; la Formación del Cíjara ha librado microfósiles bacterianos como Bavlinella y Palaeogomphosphaeria, y pistas fósiles simples (Gordia, Helminthoidichnites y treptícnidos). El límite Ediacárico-Cámbrico, a partir de icnofósiles, se sitúa en la parte basal de la Formación de Arrocampo y en la parte terminal de la del Cíjara. El valle del Alcudia ofrece algunas peculiaridades, lo que se refleja por el mantenimiento de una subdivisión litoestratigráfica propia: el Grupo de Ibor se divide en las Formaciones de Tamujar, Hinojosas (caracterizada por su contenido en icnofósiles, que incluye treptícnidos, Monomorphichnus, Psammichnites y Taphrelminthopsis) y Cabezarrubias (con Bergaueria y Planolites). Otra discontinuidad mayor se reconoce a techo del Grupo de Ibor y de la Formación del Cíjara, recubiertos respectivamente por la Formación de San Lorenzo y unas capas de megabrechas muy características. Las megabrechas, interpretadas como depósitos de talud y conocidas como las capas de Fuentes, Membrillar y Navalpino, se sitúan a base de la Formación del Pusa, de composición heterolítica y de edad Terranóvico a Serie cámbrica 2. Se subdivide el Pusa en tres miembros, destacando el intermedio por el registro de yacimientos de interés económico de fosfato (Capa de Fontanarejo). La Formación del Pusa contiene el fósil de cuerpo blando Beltanelliformis así como numerosos icnofósiles (Monomorphicnus y Treptichnus; miembro inferior), espículas de esponja asociadas con trombolitos (miembro intermedio) y Scenella, trilobites, arqueociatos e icnofósiles (Dactyloidites, Psammichnites, Rusophycus y Teichichnus; miembro superior). En ausencia de megabrechas, el Grupo de Ibor aparece directamente recubierto por las Formaciones de San Lorenzo y Fuentepizarra, esta última caracterizada por su contenido en calizas fosfáticas ricas en microfósiles, como Anabarella, que caracterizan la transición Fortuniense-Piso Cámbrico 2.

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Section: Structural Style Of the Central Iberian Zonementioning

confidence: 99%

Updated stratigraphic framework and biota of the Ediacaran and Terreneuvian in the Alcudia-Toledo Mountains of the Central Iberian Zone, Spain

et al. 2019

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“…the Tamames-Marofa-Sátão synform) are C3 structures, possibly nucleated within existing C1-C2 structures (e.g. Dias da Silva et al, 2017;Jacques et al, 2018b). The remarkable continuity along the Central Iberian Zone of these folds ( Fig.…”

Section: Structural Geology and Geochronologymentioning

confidence: 93%

The enigmatic curvature of Central Iberia and its puzzling kinematics

Pastor‐Galán¹,

Gutiérrez-Alonso²,

Weil³

2020

Preprint

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The collision between Gondwana and Laurussia that formed the latest supercontinent, Pangea, occurred during Devonian to Early Permian times and resulted in large-scale orogeny that today transects Europe, northwest Africa and eastern North America. This orogen is characterized by an 'S' shape corrugated geometry in Iberia. The northern curve of the corrugation is the well known and studied Cantabrian (or Ibero-Armorican) Orocline and is convex to the east and towards the hinterland. Largely ignored for decades, the geometry and kinematics of the southern curvature, known as the Central Iberian curve, are still ambiguous and hotly debated. Despite the paucity of data, the enigmatic Central Iberian curvature has

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“…310-297Ma) (Van der Voo et al, 1997;Weil et al, 2013;Fernández-Lozano et al, 2016;Pastor-Galán et al, 2015b. Furthermore, detailed structural analyses infer that the geometry of many large-scale fold structures in the Iberian massif have been strongly reshaped by late-Variscan D3 deformation (Macaya, 1983;Martínez Catalán, 2012;Díez Fernández and Pereira, 2016;Dias da Silva et al, 2017;Pereira et al, 2017). To elucidate the above discrepancy, further studies tackling the geometry and kinematics of both Variscan fold generations are necessary.…”

Section: Introductionmentioning

confidence: 99%

“…1) (Julivert and Marcos, 1973;Bastida et al, 2010;Pastor-Galán et al, 2012). Within the Central Iberian Zone (CIZ), however, detailed accounts of F1-F3 superimposed folding are limited and have focused on narrow synforms containing Ordovician formations (Dias da Silva et al, 2017;.…”

Section: Introductionmentioning

confidence: 99%

Superimposed folding and W-Sn vein-type mineralisation in the Central Iberian Zone associated with late-Variscan oroclinal buckling: A structural analysis from the Regoufe area (Portugal)

2018

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The Cantabrian orocline is a major orocline that bends the Variscan belt of Western Europe. Despite a wealth of studies, its timing and relationship with the late-Variscan folding stages in the Iberian Massif are still debated. This study provides an integrated structural analysis of the Variscan fold generations and associated W-Sn bearing vein systems within the southern Central Iberian Zone (Regoufe, Portugal), giving insight into their kinematic relationship with oroclinal buckling. Two superimposed fold generations with mutually parallel, steep to vertical fold axes have been identified. Isoclinal F1 folds with E-W striking axial planes formed during coaxial shortening and are spatially localised. F3 folds with NW-SE axial planes are associated with late-Variscan transpressional deformation and constrain the structural outline of the major folds. Temporal and kinematic considerations indicate that vertical-axis, asymmetric F3 folding corresponds with the expected deformation style within the southern limb of the Cantabrian orocline. The Regoufe area is characterised by two types of W-Sn vein-type mineralisation. Granite-hosted hydrothermal quartz veins show a concentric distribution and are associated with the stress regime during granite emplacement. The vein system within the metasedimentary host rock, however, is emplaced along a regional, subhorizontal cross-fold joint system. This cross-fold joint system developed orthogonal to the subvertical F3 fold axes, and is interpreted to be coeval with oroclinal buckling. These results impact the understanding of (i) the relative significance and geometry of the main deformation stages in the Iberian massif, reconciling the timing and kinematics of F3 regional folding with oroclinal buckling, and (ii) the kinematic relationship between late-to postorogenic deformation and W-Sn veintype mineralisation.

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Structural and microstructural analysis of the Retortillo Syncline (Variscan belt, Central Iberia). Implications for the Central Iberian Orocline

Cited by 19 publications

References 48 publications

Updated stratigraphic framework and biota of the Ediacaran and Terreneuvian in the Alcudia-Toledo Mountains of the Central Iberian Zone, Spain

Updated stratigraphic framework and biota of the Ediacaran and Terreneuvian in the Alcudia-Toledo Mountains of the Central Iberian Zone, Spain

The enigmatic curvature of Central Iberia and its puzzling kinematics

Superimposed folding and W-Sn vein-type mineralisation in the Central Iberian Zone associated with late-Variscan oroclinal buckling: A structural analysis from the Regoufe area (Portugal)

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