El Cenozoico del alto río Teno, Cordillera Principal, Chile central: estratigrafía, plutonismo y su relación con estructuras profundas

Piquer, J; Castelli, Juan Carlos; Charrier, Reynaldo; Yáñez, Gonzalo

doi:10.4067/s0718-71062010000100002

Cited by 10 publications

(12 citation statements)

References 23 publications

(22 reference statements)

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“…2) (e.g., Zurita et al, 2000;Charrier et al, 2002Charrier et al, , 2005Charrier et al, , 2007Jara et al, 2009a). These data are consistent with thermal maturity studies (Zurita et al, 2000) and structural profiles (Fock, 2005;Farías et al, 2008;Jara et al, 2009b;Piquer et al, 2010), supporting the hypothesis that the Abanico Basin was almost clogged during the inversion stage. The greatest accumulation of both syn-rift and syn-inversion deposits has been found next to the main faults.…”

Section: The Abanico Basinsupporting

confidence: 87%

Influencia de la carga de los depósitos en la generación de fallas de atajo durante la inversión de una cuenca extensional: El caso de la cuenca de Abanico (Eoceno-Oligoceno), Andes de Chile central (33°- 35°S).

Muñoz-Sáez

Pinto²,

Charrier

et al. 2014

Andgeo

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The current paper analyzes the evolution of the Abanico Basin, in the Chilean Principal Cordillera in central Chile (33º-35ºS). According to previous studies, the basin has been affected by two main deformational episodes: the first, related to extension, and the second, to partial basin inversion. Deposits of the Abanico Formation, Eocene-Oligocene, and the Farellones Formation, Early-Middle Miocene, represent these two deformational episodes, respectively. Studies of the basin deposits and the structural features show that the basin was asymmetric and that it developed two main depocenters. The eastern depocenter is deeper and was controlled by a west-dipping fault system (El Diablo Fault System) that formed its eastern border. We propose that the geometry of the basin and the magnitude of inversion were strongly influenced by the load generated by the thick volcanic and volcaniclastic pile that accumulated in the eastern depocenter. Through analogue modeling, we interpret that the Aconcagua fold-thrust belt was triggered at ~16 Ma by a shortcut thrust rooted in the El Diablo Fault System, which during inversion was blocked because of the high load exerted by the deposits of the Abanico and Farellones formations. In addition, the stratified Mesozoic succession that formed the eastern border of the basin allowed the propagation of the shortcut thrust along the ductile Oxfordian gypsum layer. This would have determined the east vergence of the fold-thrust belt. On the western side of the basin, the absence of weak layers prevented development of a west-vergent fold-thrust belt.

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Section: The Abanico Basinsupporting

confidence: 87%

Influencia de la carga de los depósitos en la generación de fallas de atajo durante la inversión de una cuenca extensional: El caso de la cuenca de Abanico (Eoceno-Oligoceno), Andes de Chile central (33°- 35°S).

Muñoz-Sáez

Pinto²,

Charrier

et al. 2014

Andgeo

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“…In the study area, these geological domains are represented by the Mesozoic Río Damas, Baños del Flaco and Colimapu Formations and the Cenozoic Abanico Formation. This major tectonic boundary has been interpreted as the eastern border of Abanico extensional basin (Piquer et al 2010;Charrier et al 2002), developed during the Eocene to the Early Miocene (Giambiagi et al 2015). According to Piquer et al 2015, the Abanico basin was compartmentalized by previous regional-scale normal fault systems striking NW and NE.…”

Section: Regional Tectonic Features In the Area Of Descabezado Grandementioning

confidence: 98%

Mafic monogenetic vents at the Descabezado Grande volcanic field (35.5°S–70.8°W): the northernmost evidence of regional primitive volcanism in the Southern Volcanic Zone of Chile

Salas

Rabbia

Hernández

et al. 2016

Int J Earth Sci (Geol Rundsch)

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“…and some of these granitoids constitute very important porphyry Cu (-Mo) deposits (Maksaev et al, 2003;Deckart et al, 2010;Piquer et al, 2010). Geodetic models based on GPS estimations reveal that the current convergence rate between the Nazca and South American plates in this segment of the Andes is around 70 mm/a (Norabuena et al, 1999;Kendrik et al, 2003).…”

Section: Tectonic Frameworkmentioning

confidence: 99%

“…15e). Magmatic activity was intense during the Miocene and Pliocene in Chile, where widespread volcanic and plutonic rocks are exposed approximately between 33º and 35ºS (Maksaev et al, 2003;Deckart et al, 2010;Piquer et al, 2010). Fission track analysis in apatite reveal cooling ages from 21 to 3.1 Ma and suggest an important period of Andean uplift and denudation between 5.6 and 3.1 Ma (Maksaev et al, 2003).…”

Section: Relationship Between Cenozoic Magmatism and Andean Tectonicsmentioning

confidence: 99%

“…Fission track analysis in apatite reveal cooling ages from 21 to 3.1 Ma and suggest an important period of Andean uplift and denudation between 5.6 and 3.1 Ma (Maksaev et al, 2003). Piquer et al (2010) dated a granodiorite at 7.8±0.4 Ma (K-Ar in biotite) and interpreted the emplacement of intrusives rocks as being controlled by the Infiernillo-Los Cipreses fault system, a set of Late Eocene-Middle Miocene normal faults that acted as reverse faults during an episode of major tectonic contraction in the Late Miocene, which induced the ascent of the intrusive bodies. Barren Miocene granitoids located between 33º and 34ºS, with arc-like signature and crystallization ages from 14.9±0.2 Ma to 10.2±0.2 Ma (U-Pb LA-ICPMS), suggest that in this region magmatism does not reflect eastward arc front migration (Deckart et al, 2010).…”

Section: Relationship Between Cenozoic Magmatism and Andean Tectonicsmentioning

confidence: 99%

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Cenozoic structural evolution of the Argentinean Andes at 34º40’S: A close relationship between thick and thin-skinned deformation

Turienzo

Dimieri

Frisicale

et al. 2012

andgeo

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ABSTRACT. In the Argentinean side of the Andes at 34°40'S, the Cenozoic Andean orogeny produced the thick-skinned Malargüe fold-and-thrust belt and the easternmost basement uplift of the Cordillera Frontal. Integrating balanced structural cross-sections with previous studies of Cenozoic synorogenic rocks and 40 Ar/ 39 Ar ages of coeval volcanic and subvolcanic rocks, we propose a Miocene to Quaternary sequential structural evolution of this sector of the Andes. Andean deformation in the study area begun around 14.5 Ma with the growth of thick-skinned structures at the western region, formed by large basement wedges that propagated along detachment horizons within the cover generating thin-skinned structures. The development of these genetically linked thick and thin-skinned structures finished with the insertion of a third basement wedge and its associated deformation in cover rocks along the Sosneado thrust, before the extrusion of 10.8 Ma volcanic rocks. These structures imply ~10 km of shortening, representing an important Middle Miocene compressive period (2.7 mm/a). Systems of fractures measured in basement, cover and subvolcanic rocks indicate an E-W direction of compression. A supercritical Coulomb wedge attained after the Middle Miocene deformation, was responsible of new basement-involved faulting into the foreland, the west-dipping Carrizalito thrust. The absence of efficient detachment levels in the cover rocks of the eastern region difficulted the development of large basement wedges and instead important backthrusting occurred in the hangingwall of the Carrizalito thrust. Widespread subvolcanic rocks (10.5 to 5.5 Ma) exposed in this region suggest a close relationship between magmatism and antithetic faulting. With continuing compression, the Carrizalito thrust breaks through to the surface thrusting pre-Jurassic and Mesozoic sequences over Cenozoic rocks although in the southern region it remains as a blind thrust. This different configuration along the strike of the Carrizalito thrust is due to an ENE trending oblique fault. Thick-skinned structures in the eastern sector, that involve ~4 km of shortening, were covered discordantly by horizontal basalts of ~0. RESUMEN. Evolución estructural Cenozoica de los AndesArgentinos a los 34°40'S: una estrecha relación entre deformación de piel fina y piel gruesa. En los Andes Argentinos a los 34°40'S, la orogenia Andina produjo durante el Cenozoico la faja corrida y plegada de Malargüe, de piel gruesa, y hacia el este el levantamiento del basamento en la Cordillera Frontal. Integrando secciones estructurales balanceadas con estudios previos de rocas sinorogénicas terciarias y edades 40 Ar/ 39 Ar de rocas volcánicas y subvolcánicas contemporáneas, proponemos una evolución estructural secuencial desde el Mioceno al Cuaternario para este sector de los Andes. La deformación andina en el área de estudio comenzó alrededor de los 14,5 Ma con el desarrollo de estructuras de piel gruesa en la región occidental, formadas por grandes cuñas de basamento que se pro...

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El Cenozoico del alto río Teno, Cordillera Principal, Chile central: estratigrafía, plutonismo y su relación con estructuras profundas

Cited by 10 publications

References 23 publications

Influencia de la carga de los depósitos en la generación de fallas de atajo durante la inversión de una cuenca extensional: El caso de la cuenca de Abanico (Eoceno-Oligoceno), Andes de Chile central (33°- 35°S).

Influencia de la carga de los depósitos en la generación de fallas de atajo durante la inversión de una cuenca extensional: El caso de la cuenca de Abanico (Eoceno-Oligoceno), Andes de Chile central (33°- 35°S).

Mafic monogenetic vents at the Descabezado Grande volcanic field (35.5°S–70.8°W): the northernmost evidence of regional primitive volcanism in the Southern Volcanic Zone of Chile

Cenozoic structural evolution of the Argentinean Andes at 34º40’S: A close relationship between thick and thin-skinned deformation

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