Stratigraphy and evolution of the Cretaceous forearc Celica-Lancones basin of southwestern Ecuador

Jaillard, Étienne; Laubacher, Gérard; Bengtson, Peter; Dhondt, Annie V.; Bulot, Luc G.

doi:10.1016/s0895-9811(99)00006-1

Cited by 44 publications

(49 citation statements)

References 13 publications

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“…Although their geometric relations with the San Juan terrane are not visible, these deposits are interpreted as postdating the accretion of the San Juan terrane to the Andean margin, which occurred therefore, in Late Campanian times (Hughes & Pilatasig 2002;Kerr et al 2002;Jaillard et al 2004;. This tectonic event is further documented on the continental margin of southern Ecuador and northern Peru, by the widespread deposition of a coarsening and shallowing upward sequence of conglomerates of Late Campanian age, unconformably overlain by transgressive marine shales of Early Maastrichtian age (Taipe et al 2004;Jaillard et al 1999; …”

Section: San Juan Terranementioning

confidence: 92%

“…The age of accretion is assumed to be the same as in central Ecuador. Jaillard et al 1999;. Location Fig.…”

Section: Fig 6: Rare Earth Element (Left) and Multi-element (Right) mentioning

confidence: 99%

“…1 Farther south, on the continental margin of northern Peru and southern Ecuador, this tectonic event is recorded by a disconformity between Early to Middle Maastrichtian marine shales and sandtones, and Paleocene sandstones (Fig. 3), associated with a well marked hiatus (Taipe et al 2004;Jaillard et al 1999;.…”

Section: Fig 6: Rare Earth Element (Left) and Multi-element (Right) mentioning

confidence: 99%

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Accreted oceanic terranes in Ecuador: southern edge of the Caribbean Plate?

Jaillard

Lapierre²,

Ordóñez

et al. 2009

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The western part of Ecuador is made from several oceanic terranes, which comprise two oceanic plateaus, of Early (c. 120 Ma) and Late Cretaceous age (c. 90 Ma), respectively. The older oceanic plateau was accreted to the Andean margin in the Late Campanian (c. 75 Ma). Fragments of the Turonian–Coniacian plateau were accreted to the Ecuadorian margin in the Late Maastrichtian (c. 68 Ma, Guaranda terrane) and Late Paleocene (c. 58 Ma, Piñón–Naranjal terrane). The Guaranda terrane received either fine-grained oceanic sediments of Coniacian–Maastrichtian age, or island arc/back-arc volcanic suites of Middle Campanian–Middle Maastrichtian age. The Piñón–Naranjal terrane recorded a comparable history, completed in the Maastrichtian–Paleocene, either by pelagic cherts, or by island arc products (Macuchi arc). The Late Cretaceous plateau of Ecuador is interpreted as part of the Caribbean oceanic plateau (COP), because their evolutions are comparable. If so, the COP was not formed by the Galápagos hotspot, but on the Farallón oceanic plate, south of Ecuador and close to the South American margin. The COP belonged to the Farallón plate, until a subduction zone separated both plates in the Middle Campanian, giving way to a well-developed Mid Campanian–Mid Maastrichtian island arc. Accretion in the Late Maastrichtian triggered a change in the subduction system, and the development of a new arc system of Late Maastrichtian–Late Paleocene age, which crosscut the South America–COP plate boundary. The last accretion occurred in the Late Paleocene.

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Section: San Juan Terranementioning

confidence: 92%

“…The age of accretion is assumed to be the same as in central Ecuador. Jaillard et al 1999;. Location Fig.…”

Section: Fig 6: Rare Earth Element (Left) and Multi-element (Right) mentioning

confidence: 99%

Section: Fig 6: Rare Earth Element (Left) and Multi-element (Right) mentioning

confidence: 99%

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Accreted oceanic terranes in Ecuador: southern edge of the Caribbean Plate?

Jaillard

Lapierre²,

Ordóñez

et al. 2009

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“…Also outcropping in northern Peru-southern Ecuador, is the Cretaceous Lancones basin (Figure 1), which comprises a broadly folded, metalliferous volcanic section ranging in age from ~105-90 Ma, just younger than most of the Huarmey basin; hosts Late Cretaceous plutons correlated with those of the Coastal batholith; and sits structurally between the Amotape and Olmos massifs (Jaillard et al 1999;Winter et al 2010). The earliest magmatism, ~105-100 Ma, was a bimodal, tholeiitic to calc-alkaline basalt-dominated sequence of pillow basalt with associated volcanic massive sulphide deposits and low Nb and Y siliceous rocks; whereas younger 99-90 Ma magmatism involved both tholeiitic and calc-alkaline basalt, andesite and more siliceous lava (Winter 2008).…”

Section: Other 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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“…Note locations of Figs. 4-6. ceous succession rests unconformably on Paleozoic-middle Cretaceous rocks of the forearc zones of southern Ecuador and northwestern Peru (Olsson, 1944;Jaillard et al, 1998Jaillard et al, , 1999.…”

Section: Geological Settingmentioning

confidence: 99%

Sedimentary record of terminal Cretaceous accretions in Ecuador: The Yunguilla Group in the Cuenca area

Jaillard

Bengtson

Ordóñez

et al. 2008

Journal of South American Earth Sciences

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A reappraisal of the ''Late Cretaceous Yunguilla Formation'' of the Cuenca area enables the definition of four distinct formations, correlatable with those of southwestern Ecuador. A mid-to late-Campanian marine transgression (Jadán Formation) is overlain by quartz-rich conglomerates of fan-delta to turbiditic fan environment (Quimas Formation) of latest Campanian-earliest Maastrichtian age, which are interpreted as evidence of the accretion of a first oceanic terrane (San Juan). Disconformable, arkosic turbidites and cherts (Tabacay Formation) of early Maastrichtian age are thought to represent the erosion of the newly accreted oceanic terrane. A major unconformity of late Maastrichtian age, caused by the accretion of a second oceanic terrane (Guaranda), is followed by the deposition of quartz-rich micaceous shelf sandstones (Saquisilí Formation) of Paleocene age. A third accretion event (late Paleocene) is recorded in coastal Ecuador. Each accretion event correlates with the uplift and erosion of the Eastern Cordillera and with a sedimentary hiatus in the eastern areas. In Ecuador, accretion of oceanic terranes contributed to the build up of the Andes through tectonic underplating of low-density material, and the eastern areas did not behave as flexural foreland basins during late Cretaceous-Paleogene times.

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Stratigraphy and evolution of the Cretaceous forearc Celica-Lancones basin of southwestern Ecuador

Cited by 44 publications

References 13 publications

Accreted oceanic terranes in Ecuador: southern edge of the Caribbean Plate?

Accreted oceanic terranes in Ecuador: southern edge of the Caribbean Plate?

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

Sedimentary record of terminal Cretaceous accretions in Ecuador: The Yunguilla Group in the Cuenca area

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