Mesozoic Pelagic Phosphate Stromatolites from the Penibetic (Betic Cordillera, Southern Spain)

Martín‐Algarra, Agustín; Vera, Jesús

doi:10.1007/978-94-011-1124-9_14

Cited by 18 publications

(11 citation statements)

References 38 publications

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“…8d). These kinds of encrustations are called endostromatolites (Monty 1984;Martín-Algarra and Vera 1994;Sánchez-Navas 1995, 2000;Burkhalter 1995). They can also be partially Wlled with coarser-grained sediments including ferruginous macro-oncoids (Fig.…”

Section: Reclot Unitmentioning

confidence: 97%

“…These sedimentary discontinuities are represented in several domains, for instance the Iberian Range (Aurell et al 1994(Aurell et al , 1999Ramajo and Aurell 1997;Ramajo et al 2002;Meléndez et al 2005), the Côte D'Or (Courville and Collin 1997), Chaignay (ScouXaire et al 1997), the western Subalpine Basin (Dromart 1989), the southeastern Paris Basin (Lorin et al 2004;Collin et al 2005), the Jura region of Switzerland (Gygi 1981;Huber et al 1987), Swabia (Gygi and Persoz 1987), and the Maghreb (Soussi and MЈrabet 1991;Kadiri 2002;Reolid et al 2011). In the Betic External Zone, which represents the South Iberian Paleomargin during the Mesozoic, major stratigraphic gaps and discontinuity surfaces occur in the Bathonian-Oxfordian interval (Sequeiros 1974(Sequeiros , 1979Seyfried 1978;García-Hernández et al 1980Sandoval 1979Sandoval , 1983Molina 1987;Marques et al 1991;Martín-Algarra and Vera 1994;Vera and Martín-Algarra 1994;Martín-Algarra and Sánchez-Navas 2000;O'Dogherty et al 2000;Vera 2001;.…”

Section: Introductionmentioning

confidence: 97%

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Evolution of pelagic swells from hardground analysis (Bathonian–Oxfordian, Eastern External Subbetic, southern Spain)

Nieto

Reolid

Molina

et al. 2011

Facies

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The Middle Bathonian to Middle Oxfordian interval in the Eastern External Subbetic (Betic Cordillera, SE Spain) is characterized by Ammonitico Rosso facies including various stratigraphic breaks. Five hardgroundbounded units are recognized in relation to hiatuses in the ammonite record at the following stratigraphic boundaries: Hg1 (Lower-Middle Bathonian), Hg2 (Middle-Upper Bathonian), Hg3 (Lower-Middle Callovian), Hg4 (MiddleUpper Callovian), and Hg5 (Callovian-Oxfordian). Interesting features of these hardgrounds include their microfacies, ferruginous crusts and macro-oncoids, taphonomy of macroinvertebrates, trace fossils, neptunian dykes, and the hiatuses associated with each of them. The main hardgrounds (Hg1, Hg2, and Hg5) contain trace fossils of the Cruziana and Trypanites ichnofacies as well as abundant fossil macroinvertebrates with taphonomic features evidencing corrasion, early diagenesis, and reworking, indicating substrate evolution from softground to hardground. Neptunian dykes aVected the trace fossils and ammonoid moulds, and their walls and the hardground surfaces were colonized by ferruginous microbial crusts. These features are characteristic of the External Subbetic pelagic swells, where the absence of sedimentation, sediment bypassing and erosion, and early diagenesis during relative sea-level falls produced hardgrounds. The neptunian dykes are indicative of tectonic activity in the areas of pelagic swells.Ferruginous crusts and macro-oncoids developed only on hardground surfaces and neptunian dykes walls prior to deposition of condensed bioclastic beds, which are interpreted as the Wrst deposits after hardground development and are related to the onset of transgression. The varying ranges of the gaps as well as lateral facies changes are related to diVerent local paleobathymetry controlled by the activity of listric faults.

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Section: Reclot Unitmentioning

confidence: 97%

Section: Introductionmentioning

confidence: 97%

Evolution of pelagic swells from hardground analysis (Bathonian–Oxfordian, Eastern External Subbetic, southern Spain)

Nieto

Reolid

Molina

et al. 2011

Facies

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“…En el Subbético Interno, en el sector oriental de la cordillera, Aguado et al (1991) y Rey (1993 han reconocido bloques levantados por fallas normales fosilizados por esta formación y con abundantes depósitos conglomeráticos rodeándolos, intercalados en la propia formación. Finalmente, en el Penibético, Martín-A1garra (1987) y Martín-Algarra y Vera (1989Vera ( , 1994 en sus reconstrucciones paleogeográficas locales muestran cómo la Formación Capas Rojas fosiliza un gran bloque basculado, rellenando también diques neptúnicos. Todos estos datos indican inequívocamente que el fondo de la cuenca en el que se depositó la formación presentaba desniveles, en especial escalones debidos a fallas, y más localmente elevaciones debidas a relieves volcánicos submarinos.…”

Section: Significado Paleogeográficounclassified

“…B. Idem para el Eoceno inferior coincidente con el final de la sedimentación de la citada formación en amplios sectores de la cuenca. C. Vera (1989Vera ( , 1994.…”

Section: Significado Paleogeográficounclassified

“…En el sector noroccidental del Penibético la Formación Capas Rojas se dispone discordantemente sobre los materiales de la Formación Torcal (Jurásico superior) o de la Formación Endrinal (Jurásico inferior-medio) fosilizando una superficie de paleokarst originada durante el Cretácico inferior (Martín-Algarra, 1987; Martín-Algarra y Vera, 1989Vera, , 1994Martín-Algarra et al, 1992).…”

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Untitled

Vera¹,

Molina²

1999

Estud. geol.

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RESUMENSe analizan las características (litofacies, biofacies, edad, potencia, etc.) de la Fonnación Capas Rojas (Cretácico superior-Eoceno) que aflora extensamente en el Subbético, dentro de las Zonas Externas de la Cordillera Bética. Esta fonnación presenta una gran uniformidad de facies en amplios sectores de la cordillera y tiene su equivalente, en facies y en edad, en la Fonnación Scaglia Rossa de los Apeninos del centro de Italia y de los Alpes meridionales y en fonnaciones igualmente análogas en otros dominios alpinos mediterráneos. A partir de los datos sedimentológicos y paleoecológicos disponibles, especialmente del contenido en macrofósiles (rudistas aislados y equínidos) y del análi-sis de las icnofacies, se concluye que su depósito tuvo lugar en un medio marino hemipelágico de una profundidad moderada (pocos centenares de metros) durante un intervalo de tiempo muy prolongado (40-50 Ma) con una tasa de sedimentación muy reducida (pocos milímetros por mil años). Del análisis de la evolución del margen continental en el que se depositó, y de los equivalentes de otros dominios alpinos, se deduce que el inicio de su depósito marcó el final de la diferenciación en surcos y umbrales de estos már-genes pasivos en las etapas avanzadas del ritting, de manera que esta formación, en amplios sectores de la cuenca, cubrió áreas previamente escalonadas por fallas y lentamente las niveló. ABSTRACTThe characteristics (lithofacies, biofacies, age, thickness, vertical and lateral relations, etc,) and significance of the Capas Rojas Fonnation (Upper Cretaceous-Eocene) are analysed. This fonnation crops out widely in the Subbetic (External Zones of the Betic Cordillera). The Capas Rojas Formation presents a great uniformity in the wide sectors of this cordillera and has its equivalent in facies and age, in the Scaglia Rossa Fonnation of the Apennines and southern Alps and also in equally analogous fonnations in other Alpine Mediterranean domains. From the available sedimentological and paleoecological data, mainly from the macrofossils (isolated rudists and echinoids) content and from the ichnofacies analysis, it is concluded that its deposition took place in a hemipelagic marine environment with a moderate depth (a few hundreds of metres) during a long interval of time (40-50 Ma) with a very low sedimentation rate (a few millimetres per thousand years). From the analysis of the evolution of the continental margin in which was deposited, and of their equivalents in other Alpine domains, is deduced that the beginning of its deposition recorded the end of the differentiation in troughs and swells of these passive margins in the advanced stages of the rifting, so that this unit, in wide sector of the basin covered areas with an irregular topography in the bottom, mainly controlled by faults and slowly levelled them.

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