Orogenic wedge advance in the northern Andes: Evidence from the Oligocene-Miocene sedimentary record of the Medina Basin, Eastern Cordillera, Colombia

Parra, Maurício; Mora, Andrés; Jaramillo, Carlos; Strecker, Manfred R.; Sobel, Edward R.; Quiroz, Luis; Rueda, Milton; Torres, Vladimir

doi:10.1130/b26257.1

Cited by 124 publications

(156 citation statements)

References 69 publications

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“…The reactivated, inherited, extensional and contractional anisotropies have produced discrete ranges that occur both along the eastern flank of the plateau as well as far to the east of the plateau margin within the otherwise undeformed foreland, as might be expected from the mechanics of reactivation of pre-existing weak structures in the crust (Mon and Salfity, 1995;. This is virtually identical to inverted extensional structures in the Eastern Cordillera of Colombia (e.g., Mora et al, 2006;Parra et al, 2009) and bears resemblance to the pattern of reactivated structures in the North American Laramide province (Marshak et al, 2000). Thus, the pre-Andean paleogeography of northwestern Argentina has left an imprint on the manner in which Cenozoic shortening is accommodated, resulting in a broad zone of deformation without a well-defined, tectonically active orogenic front and unsystematic lateral growth (e.g., Allmendinger et al, 1983;Grier et al, 1991;Mon and Hongn, 1991;Reynolds et al, 2000;Carrera et al, 2006;Ramos et al, 2006;Hongn et al, 2007;Hilley and Coutand, 2010).…”

Section: Retroarc Topography Deformation and Deposition In The Centsupporting

confidence: 51%

Structural, Geomorphic, and Depositional Characteristics of Contiguous and Broken Foreland Basins: Examples from the Eastern Flanks of the Central Andes in Bolivia and NW Argentina

Strecker

Hilley

Bookhagen

et al. 2011

Tectonics of Sedimentary Basins

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In this chapter, we contrast the elements of a typical, contiguous foreland basin system in the Bolivian Andes with the broken foreland farther south in northwestern Argentina. We illustrate differences in deposition and geomorphic shape that arise from the structural conditions to which these two systems are subjected. Generally, the principal elements of foreland-basin systems result mainly from accommodation space created by the flexural response of the crust to the topographic load of a fold-and-thrust belt. This leads to the formation of four distinct depozones: the wedge-top, foredeep, forebulge, and backbulge. In contrast, broken foreland basins are formed in areas where retroarc convergence is accommodated primarily along re-activated, high-angle structures. Rather than creating a broad area of consistently sloping mean topography, rock uplift along these structures is often disparate in space and time, leading to the formation of discrete ranges of limited along-strike extent that occur far inboard of the main topographic front of the orogen. The potentially high rock-uplift rates accommodated by steep, reactivated reverse faults favors isolation of the headwater basins of such systems from the downstream fluvial network, leading to sediment ponding behind the rising mountain ranges. In addition, the limited flexural response associated with short wavelength, laterally restricted topography may fail to create large amounts of accommodation space seen in the foredeep depozone that typifies foreland basin systems. Thus, instead of the generally continuous, laterally extensive foreland basin system associated with continental-scale crustal flexure, broken foreland basins, such as in the northwestern Argentine Andes, consist of a set of variably connected, laterally restricted depocenters. These evolve behind actively rising topography or small basins that form within the limited accommodation space created around individual uplifted mountain ranges. These types of depositional systems lack many of the elements that are typical of recent foreland basins, including well-developed foredeep, forebulge, and backbulge depositional systems. Instead of applying foreland basin models to broken foreland basin systems, it is important to view these systems in the context of their distinct structural, topographic, and geodynamic circumstances.

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Section: Retroarc Topography Deformation and Deposition In The Centsupporting

confidence: 51%

Structural, Geomorphic, and Depositional Characteristics of Contiguous and Broken Foreland Basins: Examples from the Eastern Flanks of the Central Andes in Bolivia and NW Argentina

Strecker

Hilley

Bookhagen

et al. 2011

Tectonics of Sedimentary Basins

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“…4.9 Comparison between exhumation data in a basement massif along the eastern foothills in the Colombian Eastern Cordillera (data after Mora et al 2008;Parra et al 2009b) -see location in Fig. 4.8 in the area number 2 and number 5 -and the subsidence and granulometric changes in the Neogene record of the adjacent foredeep along the eastern foothills (modifi ed after Parra et al 2009a). Exhumation is shown plotted by age versus structural position in order to derive exhumation rates based on zircon fi ssion track data and apatite fi ssion track data from the same basement massif.…”

Section: Age (Ma)mentioning

confidence: 99%

“…Notice the Chiribiquete, Araracuara and Macarena ranges and the position of the Orinoco-Amazon drainage divide. All these elements are defi ned by the Vaupés Swell low-elevation arch.The numbers indicate the location of different recent geological studies in the Eastern Cordillera: 1.Gómez et al (2003Gómez et al ( , 2005; 2 Parra et al (2009aParra et al ( , 2009bBayona et al (2008)…”

mentioning

confidence: 99%

Tectonic History of the Andes and Sub‐Andean Zones: Implications for the Development of the Amazon Drainage Basin

Mora

Baby

Roddaz

et al. 2009

Amazonia: Landscape and Species Evolution

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118

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“…Due to this renewed interest, many informal reports contain valuable regional data. Some recent studies have proposed regional basin analysis in Peru (Hermoza 2004;Hermoza et al 2005aHermoza et al , 2005b, in Ecuador (Christophoul et al 2002a) and in Colombia (Bayona et al 2007;Parra et al 2009) but lack stratigraphic homogenization. As a result, political frontiers have prevented an earlier synthesis of the Tertiary evolution of the Amazonian foreland basin.…”

Section: The Amazonian Foreland Basin System 63mentioning

confidence: 99%

Cenozoic Sedimentary Evolution of the Amazonian Foreland Basin System

Roddaz

Hermoza

Mora

et al. 2009

Amazonia: Landscape and Species Evolution

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In this chapter we present a synthesis of the Cenozoic evolution of the Amazonian foreland basin system, based on a review of the estimated ages, lithology and sedimentary structures, palaeontological content, and inferred depositional environments of sedimentary units in the basin. In addition, we have calculated maximum sedimentation rates for the Cenozoic formations of the northern Peruvian foreland basin and integrated these with existing data on sedimentation rates, subsidence analysis, migration of depocentre and depositional environments. Based on this information we propose a model for the Cenozoic evolution of the Amazonian foreland. The sedimentary architecture of this foreland basin indicates that Cenozoic evolution was marked by several periods, which were roughly synchronous and of similar effect, along the entire Amazonian foreland basin system. Tectonic loading of the Andes of Colombia, Ecuador, Peru and northern Bolivia, and development of the Amazonian foreland, was initiated during Late Cretaceous-Paleocene times and followed by an unloading stage during the Early-Middle Eocene period. The Middle-Late Eocene marine transgression and the increase in sedimentation rates, associated with westward migration of the depocentre, were all indicative of a renewed phase of tectonic loading of the Peruvian Western Cordillera and the Ecuadorian and Colombian Eastern Cordillera. Subsequent Oligo-Miocene increase in sedimentation rates and further migration of the depocentres towards the present-day sub-Andean zone, are all indicative for a thrust-induced uplift and loading of the Eastern Cordilleras of Peru, Bolivia and Colombia. This Oligo-Miocene loading stage maintained high subsidence rates that favoured the sedimentation of aggradational fl oodplain and coastal plain and tidally infl uenced deposits. Nevertheless, the processes that controlled the Early-Middle Miocene marine ingressions remain to be determined. Late Miocene ongoing thrust tectonic loading of the Eastern Cordillera, initial structuring of the sub-Andean zone and the onset of the main phase of Andean surface uplift induced fl exural subsidence in the foredeep depozones of the entire Amazonian foreland basin. This process also drove the Late Miocene marine transgressions that characterized the fi lled stage of the Ecuadorian, Peruvian and Bolivian Amazonian foreland basin system. Valley incisions and full relief development in the hinterland during the Late Miocene-Pliocene provided increased sediment supply and overfi lled the Amazonian foreland basin system. Finally, the fl at-slab subduction of the Nazca ridge induced Pliocene (~4 Ma) uplift of the Fitzcarrald Arch and subdivided the Amazonian foreland basin into the northern and southern Amazonian foreland basins.

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Orogenic wedge advance in the northern Andes: Evidence from the Oligocene-Miocene sedimentary record of the Medina Basin, Eastern Cordillera, Colombia

Cited by 124 publications

References 69 publications

Structural, Geomorphic, and Depositional Characteristics of Contiguous and Broken Foreland Basins: Examples from the Eastern Flanks of the Central Andes in Bolivia and NW Argentina

Structural, Geomorphic, and Depositional Characteristics of Contiguous and Broken Foreland Basins: Examples from the Eastern Flanks of the Central Andes in Bolivia and NW Argentina

Tectonic History of the Andes and Sub‐Andean Zones: Implications for the Development of the Amazon Drainage Basin

Cenozoic Sedimentary Evolution of the Amazonian Foreland Basin System

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