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EL HETTANGIENSE-SINEMURIENSE ( JURÁSICO INFERIOR) EN EL SECTOR MONTALBÁN-OLIETE (TERUEL): ANALISIS DE FACIES Y EVOLUCI~N TECTOSEDIMENTARIA
Abstract
Resumen: En este trabajo se realiza el estudio sedimentológico y tectónico de los materiales de edad Hettangiense-Sinemuriense en un sector de la Rama Aragonesa de la Cordillera Ibérica, situado entre Montalbán y Oliete. La variedad de facies encontradas, yesos y lutitas, brechas de colapso-disolución con clastos evaporíticos, brechas de colapso-disolución con clastos dolomíticos, brechas sedimentarias dolomíticas y poligénicas, dolom'as masivas oquerosas y dolomías tableadas, corresponde a tres subambientes de plataforma interna, desde sebja costeras a medios marinos someros. La presencia de facies de evaporitas o de facies de brechas de colapso-disolución en la Fm. Cortes de Tajuña estaría en función de la lejanía o proximidad con los medios marinos abiertos. Se ha determinado la posición de una serie de fallas normales activas durante el Hettangiense-Sinemuriense que condicionaron la morfología y la distribución de espesores y facies en la cuenca. En las zonas próximas a los escapes de falla y más subsidentes de la cuenca, aparecen megabrechas de clastos angulosos. Palabras clave: brechas, relación tectónica-sedimentación, Cordillera Ibérica, Jurásico Inferior. Abstract: The results of a sedimentological and tectonic analysis of the Hettangian-Sinemurian of the northern Iberian Chain (Montalbán-Oliete area, Teruel province) are presented in this work. The variety of the distinguished facies: evaporites and lutites, evaporitic collapse breccia, dolomitic collapse breccia, erosive breccia (dolomitic and poligenic), massive dolomites, larninated dolomites, are related to deposition in three different environments of a inner platform ranging from shallow sabkha to subtidal environments. The presence of evaporites or collapse breccias in Cortes de Tajuña formation depends on the distance from open sea environments. A set of normal Lower Jurassic faults has been mapped. Thickness and facies distribution were controlled by the tilting of blocks due to normal faulting. In the closest areas to the fault, megabreccia facies are found.
... El esquema litoestratigráfico propuesto en este trabajo otorga el rango de formación a cada una de las unidades litoestratigráficas definidas en el apartado anterior y diferenciadas tanto litológicamente como en edad, ya que representan episodios claramente distintos en la evolución sedimentaria de la plataforma carbonatada somera del Jurásico Inferior de Mallorca. En este apartado se analiza su correlación con la estratigrafía definida en otras áreas tanto del margen ibérico del Tethys, como su conexión con el margen subboreal al norte del Macizo Ibérico: Cuenca de Asturias y Cuenca Vasco-Cantábrica (Suárez-Vega, 1974;Valenzuela et al., 1986;Braga et al., 1988;Pujalte et al., 1988;Robles et al., 1989Robles et al., , 2004Quesada et al., 1991Quesada et al., , 1993Quesada et al., , 2005Aurell et al., 2002Aurell et al., , 2003, Pirineos (Fauré, 2002), Cordillera Ibérica y Costero-Catalana (Comas-Rengifo et al., 1998Bordonaba & Aurell, 2001;Aurell et al., 2003;Gómez et al., 2003;Gómez & Goy, 2004 y Cordillera Bética (García-Hernández et al., 1979a, b, 1986Vera, 1988;Andreo et al., 1991;Ruiz-Ortiz et al., 2004); así como en relación a otras áreas tethysianas próximas: plataformas de Trento y Friuli al Sur de los Alpes (Masetti et al., , 2016Preto et al., 2017), plataforma Umbria-Marche de los Apeninos centrales, Sicilia (Di Stefano et al., 2002;Basilone 2009;Marino & Santantonio, 2010;Jenkyns, 2020) y Alto Atlas en Marruecos (Crevello, 1991;Kenter & Campbell, 1991). En todas ellas se describen formaciones litoestratigráficas similares a las definidas para el Jurásico Inferior de Mallorca (Figs. 4 y 5) y más concretamente, para el intervalo Sinemuriense−Pliensbachiense inferior, objetivo principal del presente trabajo (Fig. 2). ...
... Bordonaba & Aurell, 2001, 2002a, cuyo límite inferior, en el corte tipo de Almonacid de la Cuba, se sitúa en el Sinemuriense superior (parte superior de biozonaRaricostatum, 198,9 Ma.;Gómez et al., 2003;Gómez & Goy, 2005;Bádenas et al., 2010;Sequero et al., 2017).En las Zonas Externas, Prebético y Subbético, de la Cordillera Bética, las facies perimareales sinemurienses equivalentes a la Formación Es Barraca, que se presentan dolomitizadas, constituyen el Miembro inferior de la Formación Gavilán(Van Veen, 1969). En el Subbético Interno, donde está mejor preservado de la dolomitización (norte de Vélez Rubio), esta unidad (Miembro M1, segúnNieto et al. 1992 y Rey, 1997 contiene Lituosepta recoarensis y en la parte superior L. compressa, biozonas que indicarían una edad Sinemuriense superior−base del Pliensbachiense para el techo de esta unidad(Andreo et al., 1991;Rey, 1993;Nieto et al. 2004; BouDaguer-Fadel & Bosence, 2007).En el tránsito al dominio Boreal en el norte de la Península Ibérica (margen subboreal,Fig. ...
Los nuevos resultados obtenidos en estudios recientes del Sinemuriense-Pliensbachiense inferior (Formación Sóller) en la isla de Mallorca, aconsejan modificar su esquema litoestratigráfico. La nueva propuesta litoestratigráfica para este intervalo elimina la Formación Sóller y eleva sus tres miembros, anteriormente definidos como miembros Es Barraca, Sa Moleta y Es Racó, a la categoría de formación. Esta redefinición se apoya en los nuevos datos estratigráficos, sedimentológicos y bioestratigráficos obtenidos a partir del estudio detallado de la Formación Es Barraca (término recuperado en este artículo), que indican que los miembros de la hasta ahora Formación Sóller no son equivalentes laterales entre sí y representan distintas etapas en la evolución de la cuenca, estando separadas por discontinuidades de carácter regional. La primera unidad (Formación Es Barraca) representa la evolución durante el Sinemuriense de una plataforma carbonatada somera, similar a las plataformas epicontinentales desarrolladas durante el Lías inferior en el ámbito del Tethys más occidental. La segunda y la tercera (Formación Sa Moleta y Formación Es Racó; Pliensbachiense inferior) son unidades disconformes con la anterior, muestran litologías y asociaciones de facies diferenciadas y presentan una distribución y espesores irregulares a favor de surcos intraplataforma.
... Similarly, other NE-SW faults were active across the basin, such as those forming the grabens and halfgrabens described near Blesa (see Figs. 6,7). It is interesting to note that other normal faults that had been active in the study area during a previous latest Triassicearliest Jurassic extensional stage (see Bordonaba and Aurell 2001) underwent no significant reactivation in this latest Jurassic-earliest Cretaceous rifting stage. This is the case with the W-E-trending fault system located near Oliete, which had controlled significant variations in thickness in previous rifting stages (i.e. the Hettangian breccias and evaporites; see Bordonaba and Aurell 2001). ...
... It is interesting to note that other normal faults that had been active in the study area during a previous latest Triassicearliest Jurassic extensional stage (see Bordonaba and Aurell 2001) underwent no significant reactivation in this latest Jurassic-earliest Cretaceous rifting stage. This is the case with the W-E-trending fault system located near Oliete, which had controlled significant variations in thickness in previous rifting stages (i.e. the Hettangian breccias and evaporites; see Bordonaba and Aurell 2001). ...
A review of the onset of the synrift sedimentation and synsedimentary extensional tectonics of the Oliete sub-basin (north- western Maestrazgo basin, East Spain) is presented here based on new data acquired after extensive sedimentological, struc- tural and palaeontological analysis of the Barremian Blesa Fm. The lower boundary of the Blesa Fm is a prominent basal synrift unconformity overlying Jurassic units. This formation has been divided into three genetic stratigraphic sequences bounded by sub-basin-wide unconformities. The lower Blesa sequence (LBS) is characterized by distal alluvial to palustrine marls/clays grading upward to palustrine–lacustrine limestones. The LBS is bounded on top by a planar to irregular trans- gressive, hardened ferruginous surface, locally encrusted by oysters. Above this discontinuity, the middle Blesa sequence consists of oyster-rich limestones and marls deposited in a shallow restricted bay, which grade to distal alluvial and palus- trine–lacustrine marls/clays and limestones towards the marginal areas of the basin. The boundary between the middle and upper Blesa sequence (UBS) is a regressive surface outlined by the local presence of an erosive conglomeratic bed. The UBS generally starts with red clays deposited in distal alluvial fan environments, which grade upwards to palustrine and lacustrine carbonates and marls/clays. The local presence of heterolithic alternations of clay with ne-to-medium sandstone and of cross-bedded sandstones indicates the local occurrence of siliciclastic coastal environments in the UBS. The upper bound- ary of the Blesa Fm is marked by widespread transgression, giving rise to the bioclastic limestones of the Alacón Fm. In the present paper, the stratigraphic position and palaeoenvironmental context of the abundant vertebrate remains found across the de ned sequences within the Blesa Formation is reviewed. The results obtained are relevant for a further understanding of the tectosedimentary evolution of the studied basin. Successive stages of evolution are distinguished, including the initial uplift, breakup and erosion of the earlier Jurassic carbonate platform that took place during the Tithonian–Hauterivian; the onset of synrift sedimentation during the early Barremian, which was highly controlled by extensional faulting and di eren- tial block subsidence; the homogenization of the basin subsidence accompanied by the incursion of marine waters (sourced from southeastern areas) during the middle part of the Barremian; and the signi cant fall in base level, of possible climatic origin and also involving signi cant siliciclastic input in the northern areas of the Oliete sub-basin around the middle part of the late Barremian.
... Thouarsense -Aalanensis zones (Gómez and Goy, 2000). Selected references: Goy et al. (1976), Gómez (1979), Morillo and Meléndez (1979), Fernández-López and Suárez-Vega (1980), Schaff (1986), Braga et al. (1985Braga et al. ( , 1988, Comas-Rengifo and Yébenes (1988), Comas-Rengifo et al. (1988a,b, 1998, Valenzuela et al. (1989), Robles et al. (1989), Goy and Ureta (1990), San Román and Aurell (1992), Quesada and Robles (1995), Borrego et al. (1996), Quesada et al. (1997), Fernández-López et al. (1998a), Gómez andGoy (1998, 2000), Bordonaba et al. (2000), Rosales et al. (2001), Bordonaba and Aurell (2001). Pliensbachian in the northern and central IB has been located above these sequences, in the lowermost Upper Pliensbachian (lower Stokesi Zone). ...
A correlation and sequence stratigraphy study of Jurassic successions has been carried out in the main sedimentary basins of northeast Iberia, i.e., Asturias, Basque-Cantabrian, and Iberian basins, based on the identification of transgressive–regressive cycles. The development and palaeogeographic evolution of the epicontinental carbonate platforms of northeast Iberia were largely controlled by major tectonic activity at three main intervals, at the beginning of the Jurassic, in the Lower–Middle Jurassic transition, and during the uppermost Jurassic, respectively. During Early Jurassic times, northeast Iberia was the site of a single and large carbonate ramp opened to the north. This carbonate ramp suffered a progressive drowning, evolving from an inner to hemipelagic ramp systems, with the local development of suboxic environments in the deepest areas located to the north. During the Middle Jurassic, different open carbonate platforms were formed including the development of swells in intermediate areas. During the Upper Jurassic, the outer ramp areas were progressively moving to the east Iberian Basin, and the ammonite faunas showing a markedly Tethyan affinity thereafter.
... Comparison of the surface data from the Iberian Range, the subsurface data from the Tajo and Ebro Cenozoic basins, and the available biostratigraphic data support the conclusion that the breccias of the Cortes de Tajuña Formation are the near-surface dissolved equivalent of the evaporites of the Lecera Formation (CastilloHerrador, 1974; Morillo Velarde and Meléndez Hevia, 1979; Gómez, 1979, 1991 Ortí, 1987 Ortí, , 1990 Jurado, 1990; Pérez-López et al., 1996; Gómez and Goy, 1997a Gómez and Goy, , 1998 Gómez and Goy, , 1999 Gómez and Goy, , 2004 Ortí and Salvany, 2004). Other authors suggest that these deposits are sedimentary talus breccias related to synsedimentary faulting (San Aurell et al., 1992 Aurell et al., , 2002 Aurell et al., , 2003 Campos et al., 1996; Bordonaba et al., 1999; Bordonaba and Aurell, 2001), associated with a supposed angular and erosional unconformity at the T–J boundary, though some of these authors (Bordonaba and Aurell, 2002) also propose a dissolution–collapse origin. ...
More than 20 successions containing the Triassic–Jurassic (T–J) boundary were studied in five of the major geological units of Spain. The data are from outcrop, cored boreholes, and interpreted well-logs. A consistent − 3.4‰ δ13Corg isotope excursion, starting in the Rhaetian and continuing in the Hettangian, was recorded in Asturias. Climate changes in the T–J transition show a warming episode in the early Hettangian. Other climate changes are indicated by an increase in hygrophytic miospores above the T–J boundary; this reflects a more humid episode at the beginning of the Hettangian. The Messejana Dyke in southeastern Iberia is part of the Central Atlantic Magmatic Province (CAMP). CO2 outgassing related to extensive magmatic activity in the CAMP is thought to be one of the possible factors responsible for the end-Triassic mass extinction. No major sea-level changes or unconformities were recorded at the T–J boundary. Only in the Asturias area was there a well-defined shallow carbonate platform during the T–J transition. The other areas of eastern and northern Spain were occupied by coastal playas and sabkhas that developed in arid climatic conditions. The biotic crisis around the T–J boundary is reflected in the palynomorph record. In Asturias, seven species do not persist beyond the late Rhaetian, and only six appeared in the Triassic–Jurassic transition. However, 22 taxa appeared in the early Hettangian.
... Cortes de Tajuña y Cuevas Labradas es, por lo general, gradual, ya que ambas unidades se encuentran en relación de cambio lateral de facies. En torno al límite Sinemuriense-Pliensbachiense existe una discontinuidad sedimentaria ligada a un evento transgresivo, que implica el depósito de facies relativamente profundas (rampa media) en la parte septentrional de la plataforma (Gómez y Goy, 1997; Bordonaba y Aurell, 2001). Dicha discontinuidad permite separar dos términos litológicos bien diferenciados dentro de la Fm. ...
En este trabajo se realiza el análisis sedimentológico de los materiales del inicio del ciclo Jurásico (Rethiense p.p.-Sinemuriense), pertenecientes a las Fms. Cortes de Tajuña, Lécera y Cuevas Labradas (parte inferior) en un sector de la Cordillera Ibérica central, situado en la Sierra de Arcos. Las facies se han agrupado en tres grandes tipos: yesos-anhidritas con intercalación de dolomías, brechas (con clastos evaporíticos y con clastos dolomíticos) y dolomías masivas oquerosas, correspondientes a los subambientes de sebja costera y llanura intermareal, desarrollados en una plataforma interna. Las brechas de disolución tienen un origen sinsedimentario y diagenético temprano y provienen de la disolución de nódulos y niveles de evaporitas intercalados en las dolomías. Las evaporitas son muy potentes en las zonas más subsidentes y se interdigitan lateralmente con brechas de disolución, lo que muestra un cambio gradual en el ambiente de sedimentación. La presencia de facies de evaporitas o de facies de brechas es función de la existencia de áreas supramareales, con aguas sobresaturadas. La variación de potencia observada dentro de la Fm. Cortes de Tajuña es un rasgo original del depósito y está controlada por la subsidencia diferencial y no por la disolución tardía de los niveles evaporíticos.
A sedimentological analysis has been carried out in the uppermost Raethian-Sinemurian, Cortes de Tajuña, Lécera and Cuevas Labradas (lower part) Fms., in the outcrops of the Sierra de Arcos (central Iberian Chain, NE Spain). Three facies have been distinguished: gypsum-anhydrite with dolomitic intercalations, breccias (with evaporitic and dolomitic clasts) and massive dolomites. These facies were deposited in inner platform areas, ranging from shallow sabkha to intertidal flat environments. Breccias were originated by dissolution during the early stages of the diagenesis. The presence of evaporites reflects the development of supratidal areas, oversaturated in salts. Thick evaporites successions change laterally to breccias, showing a gradual environmental transition. Overall thickness variation in the uppermost Raethian-Hettangian units was controlled by local basin subsidence due to normal faulting, rather than late burial dissolution of evaporitic levels.
En este trabajo se realiza el análisis sedimentológico de los materiales del inicio del ciclo Jurásico (Rethiense p.p.-Sinemuriense), pertenecientes a las Fms. Cortes de Tajuña, Lécera y Cuevas Labradas (parte inferior) en un sector de la Cordillera Ibérica central, situado en la Sierra de Arcos. Las facies se han agrupado en tres grandes tipos: yesos-anhidritas con intercalación de dolomías, brechas (con clastos evaporíticos y con clastos dolomíticos) y dolomías masivas oquerosas, correspondientes a los subambientes de sebja costera y llanura intermareal, desarrollados en una plataforma interna. Las brechas de disolución tienen un origen sinsedimentario y diagenético temprano y provienen de la disolución de nódulos y niveles de evaporitas intercalados en las dolomías. Las evaporitas son muy potentes en las zonas más subsidentes y se interdigitan lateralmente con brechas de disolución, lo que muestra un cambio gradual en el ambiente de sedimentación. La presencia de facies de evaporitas o de facies de brechas es función de la existencia de áreas supramareales, con aguas sobresaturadas. La variación de potencia observada dentro de la Fm. Cortes de Tajuña es un rasgo original del depósito y está controlada por la subsidencia diferencial y no por la disolución tardía de los niveles evaporíticos.
Field work carried out on the Lower Jurassic (i.e., Hettangian-lower Pliensbachian) of the north Iberian basin (Sierra del Moncayo, Spain), including the mapping of unconformities and sedimentary units as well as the facies analysis, has allowed us to recognize two episodes in the sedimentary evolution of the basin. A lower one, Hettangian in age, includes sediments deposited during the period of extensional tectonic activity, which involved the formation of half-graben basins by normal listric faults. Sedimentary breccias and rudites, located mainly at the edges of the half-grabens are derived from the erosion of blocks uplifted during the Triassic. In the depocenter of the half-grabens which show most subsidence these breccias pass into thick dolomitic and evaporitic successions, deposited in sabkha environments, under negligible marine influence. The later episode, Sinemurian and lower Pliensbachian in age, consists of shallow marine carbonate units deposited in a low-angle ramp setting.
The presence of a thinned crust beneath the Valencia trough has been recognized for a long time. However, to date no attempt to link this thinning, inferred from geophysical data, with the superficial structures has been made. A quantification of the Neogene extensional processes in the crustal evolution of the Valencia trough is presented. As a consequence of the complexity of the Betic-Balearic domain, the analysis has been done for the Catalan-Valencian domain (northwestern areas of the trough). Crustal and superficial data in this area show that Neogene extension was accommodated by a listric normal fault system detached in a deep upper crustal level (13–15 km) in the marginal zone of the domain. Quantitative analysis of the Neogene structure shows the incoherence between the upper crustal thinning inferred from the geometric analysis of the superficial structures (β factor 1.4–1.5) and from geophysical data (1.8). Although the latter value agrees with that deduced from the analysis of Neogene subsidence, this incoherence suggests that the present thinned crust would be partially inherited from the Mesozoic extension. In this way, Mesozoic subsidence analysts and the recognized Mesozoic structure show that the Mesozoic extension was almost as important as the Neogene one.
[ES] El paquete dolomítico infracretácico del sector central de los Catalánides está formado, en su base, por una brecha calcárea y dolomítica atribuible al Lías, que erosiona el zócalo triásico y posee un techo calcáreo de edad portlandiense. Entre las brechas basales y los tramos dolomíticos superiores se ha observado también otra discordancia erosiva. Los cortes realizados demuestran la presencia de un relieve en el zócalo triásico-liásico, muy visible en las localidades estudiadas. [FR] La série infracrétacée du secteur central des Catalanides est formée par un niveau basal, erosif sur le socle triasique, constitué par une breche calcaire et dolomitique, atribuée au Lias et un niveau supérieur calcaire d'iige portlandien. Parmi les breches inférieures et les niveaux supérieurs m a observé une autre discordance erosive. Les coupes montrent l'existence d'un relief au contact triasique-liasique tres visible dans la région étudiée. Peer reviewed
The presence of "primary porosity" in ancient reef or bank sequences is generally assumed. Evaporite solution porosity in exposed Devonian reef-bank complexes of western Canada, however, is important. Detailed investigations are likely to show that such solution porosity is more general in the laterally equivalent subsurface petroleum reservoirs than the literature suggests. Much of the so-called primary porosity in reef reservoirs may be evaporite solution porosity.
