Upper cretaceous to paleocene depositional sequences and sandstone petrography of southwestern Patagonia (Argentina and Chile)

Macellari, Carlos E.; Barrio, Claudio A.; Manassero, Marcelo Jorge

doi:10.1016/0895-9811(89)90031-x

Cited by 105 publications

(177 citation statements)

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“…Fig. 2 shows a simplified stratigraphic chart of the working areas based mainly on Macellari et al (1989) and Marenssi et al (2003). Furque (1973) redefined and mapped the Río Leona Formation, which originally was defined by Feruglio (1944Feruglio ( , 1949 in the La Leona River valley to contain 180 m of continental fine-grained (mainly claystones) sediments cropping out south of the city of El Calafate.…”

Section: Geologic Setting and Stratigraphymentioning

confidence: 99%

“…Most studies have focused on the Basin's tectonics, structural development, and stratigraphy but failed to detail the evolution of the sedimentary environments, with a few exceptions (Arbe and Hechem, 1984;Macellari et al, 1989;Kraemer, 2003;Marenssi et al, 2003), and no detailed sedimentological study of the paleogene deposits exists. Therefore, the aim of this article is twofold: to present a detailed description of the Río Leona Formation in the area of Viedma and Argentino Lakes to analyze the evolution of the sedimentary environments and to discuss the role of eustasy and tectonics in controlling the changes in the fluvial systems and the evolution of the Austral Basin during the Oligocene.…”

Section: Introductionmentioning

confidence: 99%

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Fluvial systems variations in the Rio Leona Formation: Tectonic and eustatic controls on the Oligocene evolution of the Austral (Magallanes) Basin, southernmost Argentina

Marenssi

Limarino

Tripaldi

et al. 2005

Journal of South American Earth Sciences

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Section: Geologic Setting and Stratigraphymentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

Fluvial systems variations in the Rio Leona Formation: Tectonic and eustatic controls on the Oligocene evolution of the Austral (Magallanes) Basin, southernmost Argentina

Marenssi

Limarino

Tripaldi

et al. 2005

Journal of South American Earth Sciences

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“…and Malvinas basins developed in front of the thrusts during the Campanian and were subsequently incorporated into the thrust sheets (Macellari et al 1989;Suarez et al 2000;Olivero and Malumián 2008;Ghiglione et al 2010). Magmatism within the batholith continued to the time of collision at ~75 Ma then stopped.…”

Section: Regional Considerationsmentioning

confidence: 99%

Arc and Slab-Failure Magmatism in Cordilleran Batholiths I – The Cretaceous Coastal Batholith of Peru and its Role in South American Orogenesis and Hemispheric Subduction Flip

Hildebrand¹,

Whalen

2014

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We examined the temporal and spatial relations of rock units within the Western Cordillera of Peru where two Cretaceous basins, the Huarmey-Cañete and the West Peruvian Trough, were considered by previous workers to represent western and eastern parts respectively of the same marginal basin. The Huarmey-Cañete Trough, which sits on Mesoproterozoic basement of the Arequipa block, was filled with up to 9 km of Tithonian to Albian tholeiitic–calc-alkaline volcanic and volcaniclastic rocks. It shoaled to subaerial eastward. At 105–101 Ma the rocks were tightly folded and intruded during and just after the deformation by a suite of 103 ± 2 Ma mafic intrusions, and later in the interval 94–82 Ma by probable subduction-related plutons of the Coastal batholith. The West Peruvian Trough, which sits on Paleozoic metamorphic basement, comprised a west-facing siliciclastic-carbonate platform and adjacent basin filled with up to 5 km of sandstone, shale, marl and thinly bedded limestone deposited continuously throughout the Cretaceous. Rocks of the West Peruvian Trough were detached from their basement, folded and thrust eastward during the Late Cretaceous–Early Tertiary. Because the facies and facing directions of the two basins are incompatible, and their development and subjacent basements also distinct, the two basins could not have developed adjacent to one another. Based on thickness, composition and magmatic style, we interpret the magmatism of the Huarmey-Cañete Trough to represent a magmatic arc that shut down at about 105 Ma when the arc collided with an unknown terrane. We relate subsequent magmatism of the early 103 ± 2 Ma syntectonic mafic intrusions and dyke swarms to slab failure. The Huarmey-Cañete-Coastal batholithic block and its Mesoproterozoic basement remained offshore until 77 ± 5 Ma when it collided with, and was emplaced upon, the partially subducted western margin of South America to form the east-vergent Marañon fold–thrust belt. A major pulse of 73–62 Ma plutonism and dyke emplacement followed terminal collision and is interpreted to have been related to slab failure of the west-dipping South American lithosphere. Magmatism, 53 Ma and younger, followed terminal collision and was generated by eastward subduction of Pacific oceanic lithosphere beneath South America. Similar spatial and temporal relations exist over the length of both Americas and represent the terminal collision of an arc-bearing ribbon continent with the Americas during the Late Cretaceous–Early Tertiary Laramide event. It thus separated long-standing westward subduction from the younger period of eastward subduction characteristic of today. We speculate that the Cordilleran Ribbon Continent formed during the Mesozoic over a major zone of downwelling between Tuzo and Jason along the boundary of Panthalassic and Pacific oceanic plates.SOMMAIRENous avons étudié les relations spatiales et temporales des unités de roches dans la portion ouest de la Cordillère du Pérou, où deux bassins crétacés, la fosse d’accumulation de Huarmey-Cañete et la fosse d’accumulation péruvienne de l’ouest, ont été perçues par des auteurs précédents comme les portions ouest et est d’un même bassin de marge. La fosse de Huarmey-Cañete, qui repose sur le socle mésoprotérozoïque du bloc d’Arequipa, a été comblée par des couches de roches volcaniques tholéitiques – calco-alcalines de l’Albien au Thithonien atteignant 9 km d’épaisseur. Vers l’est, l’ensemble a fini par former des hauts fonds. Vers 105 à 101 Ma, les roches ont été plissées fortement puis recoupées par une suite d’intrusions vers 103 ± 2 Ma, durant et juste après la déformation, et plus tard dans l’intervalle 94 – 82 Ma, probablement par des plutons de subduction du batholite côtier. Quant à la fosse d’accumulation péruvienne de l’ouest, elle repose sur un socle métamorphique paléozoïque, et elle est constituée d’une plateforme silicoclastique – carbonate à pente ouest et d’un bassin contigu comblé par des grès, des schistes, des marnes et des calcaires finement laminés atteignant 5 km d’épaisseur et qui se sont déposés en continu durant tout le Crétacé. Les roches de la fosse d’accumulation péruvienne de l’ouest ont été décollées de leur socle, plissées et charriées vers l’est durant la fin du Crétacé et le début du Tertiaire. Parce que les facies et les profondeurs de sédimentation de ces deux fosses d’accumulation dont incompatibles, et que leur développement et leur socle sont différents, ces deux fosses ne peuvent pas s’être développées côte à côte. À cause de l’épaisseur accumulée, de sa composition et du style de son magmatisme, nous pensons que la fosse d’accumulation de Huarmey-Cañete représente un arc magmatique qui s’est éteinte vers 105 Ma, lorsque l’arc est entré en collision avec un terrane inconnu. Nous pensons que le magmatisme subséquent aux premières intrusions mafiques syntectoniques et aux réseaux de dykes de 103 ± 2 Ma sont à mettre au compte d’une rupture de plaque. Le bloc Huarmey-Cañete-batholitique côtier et son socle mésoprotérozoïque sont demeurés au large jusqu’à 77 ± 5 Ma, moment où il est entré en collision et a été poussé par-dessus la marge ouest sud-américaine partiellement subduite, pour ainsi former la zone de chevauchement de vergence est de Marañon. Nous croyons que la séquence majeure de plutonisme et d’intrusion de dykes qui a succédé à la collision finale à 73–62 Ma doit être reliée à une rupture de la plaque lithosphérique sud-américaine à pendage ouest. Le magmatisme de 53 Ma et plus récent qui a succédé à la collision finale, a été généré par la subduction vers l’est de la lithosphère océanique du Pacifique sous l’Amérique du Sud. Des relations temporelles et spatiales similaires qui existent tout le long des deux Amériques représentent la collision terminale d’un ruban continental d’arcs avec les Amériques durant la phase tectonique laramienne de la fin du Crétacé–début du Tertiaire. Elle a donc séparé la subduction vers l’ouest de longue date de la période de subduction vers l’est plus jeune caractérisant la situation actuelle. Nous considérons que le ruban continental de la Cordillère s’est constitué durant le Mésozoïque au-dessus d’une zone majeure de convection descendante entre Tuzo et Jason, le long de la limite entre les plaques océaniques Panthalassique et Pacifique.

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“…Despite the similar stratigraphic framework between the portions of the Austral Basin in Última Esperanza and Tierra del Fuego (Natland et al, 1974;Biddle et al, 1986;Macellari et al, 1989;Fildani and Hessler, 2005;Olivero and Malumián, 2008;among others), there are important differences between the NW and SE Austral Basin that advise against the straightforward regional application of the sedimentologic models developed at Última Esperanza. Besides from the large distance (more than 600 km) that separates both portions of the basin, these differences include the following: (1) In the NW portion (Última Esperanza) the morphology of the cratonic high-relief margin of the predecessor back-arc basin facilitated the formation of a progradational margin during progressive filling .…”

Section: Introductionmentioning

confidence: 99%

“…Biddle et al, 1986), and the only tectonic control on the stratigraphy was exerted by the dynamics of the orogenic margin (Torres Carbonell et al, 2008a, 2009Torres Carbonell, 2010). (2) The southward progradation of the basin margin in Última Esperanza controlled the transition from deep-marine to shallow-marine sedimentation at the latest Cretaceous-early Paleogene (before w60 Ma) (Macellari et al, 1989;Fildani and Hessler, 2005;Romans et al, 2011). Differently, in Tierra del Fuego the sedimentation took place in relatively deep-water settings (at least below storm wave-base) during most of the Paleogene, with further tectonically enhanced (flexural) deepening during the Oligocene (Malumián and Olivero, 2006;Olivero and Malumián, 2008;Scarpa and Malumián, 2008).…”

Section: Introductionmentioning

confidence: 99%

Sand dispersal in the southeastern Austral Basin, Tierra del Fuego, Argentina: Outcrop insights from Eocene channeled turbidite systems

Carbonell

Olivero

2012

Journal of South American Earth Sciences

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Upper cretaceous to paleocene depositional sequences and sandstone petrography of southwestern Patagonia (Argentina and Chile)

Cited by 105 publications

References 9 publications

Fluvial systems variations in the Rio Leona Formation: Tectonic and eustatic controls on the Oligocene evolution of the Austral (Magallanes) Basin, southernmost Argentina

Fluvial systems variations in the Rio Leona Formation: Tectonic and eustatic controls on the Oligocene evolution of the Austral (Magallanes) Basin, southernmost Argentina

Arc and Slab-Failure Magmatism in Cordilleran Batholiths I – The Cretaceous Coastal Batholith of Peru and its Role in South American Orogenesis and Hemispheric Subduction Flip

Sand dispersal in the southeastern Austral Basin, Tierra del Fuego, Argentina: Outcrop insights from Eocene channeled turbidite systems

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