Subandean thrust and fold belt of northwestern Argentina: Geometry and timing of the Andean evolution

Echavarría, Leandro E.; Hernández, Roberto M.; Allmendinger, Richard W.; Reynolds, James H.

doi:10.1306/01200300196

Cited by 160 publications

(274 citation statements)

References 32 publications

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“…Andean hinterland basins vary from 100 to 50,000 km 2 and contain principally nonmarine successions >2-12 km thick with accumulation rates commonly >200 m/Myr (Horton et al, 2001;Garzione et al, 2008). These thicknesses and rates match those reported for Andean foreland, wedgetop, and piggyback basins (Reynolds et al, 1990;Jordan, 1995;Echavarria et al, 2003;Horton, 2005).…”

Section: Basin Overviewsupporting

confidence: 72%

Cenozoic Evolution of Hinterland Basins in the Andes and Tibet

Horton

2011

Tectonics of Sedimentary Basins

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Sedimentary basins have been generated in hinterland regions of the Andean and Himalayan-Tibetan orogens during Cenozoic plate convergence. These hinterland basins record nonmarine sediment accumulation (commonly in high-elevation, lowrelief, internally drained, arid/semiarid settings) during protracted deformation and surface uplift of continental crust. In South America, Andean hinterland basins are produced between the western magmatic arc and craton-directed fold-thrust belt to the east. In the India-Asia collision zone, hinterland basins develop as elements of the growing Tibetan plateau between the Himalayan thrust belt and Asian plate interior to the north. Hinterland sedimentary basins in the Andes and Tibet are distinguished from foreland basins adjacent to their respective fold-thrust belts by structural position, elevation, and stratigraphic evolution. Sediment accommodation in these hinterland basins is created by flexure, fault-induced subsidence, and topographic ponding, with common examples of remnant foreland basins succeeded by younger hinterland basins.

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Section: Basin Overviewsupporting

confidence: 72%

Cenozoic Evolution of Hinterland Basins in the Andes and Tibet

Horton

2011

Tectonics of Sedimentary Basins

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“…The shortening rates increase to the north, with its maximums further north in the Subandean System (Kley et al 1999;Echavarria et al 2003;Uba et al 2009). The sector with bigger shortening in the study region is located at both margins of the Cumbres Calchaquíes (Fig.…”

Section: Discussionmentioning

confidence: 98%

Basin fragmentation controlled by tectonic inversion and basement uplift in Sierras Pampeanas and Santa Bárbara System, northwest Argentina

Iaffa

Sàbat

Muñoz

et al. 2013

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The study area is located within the Central Andes, a complex region composed of different structural styles. The region is characterized by highly elevated basement cored ranges, which abruptly break the foreland plain. These ranges were uplifted mainly by deep detached high-angle faults or by the inversion of former extensional faults of the Cretaceous rift. Palaeozoic orogenies generated crustal scale discontinuities in the basement, some of them reactivated during the Andean orogeny. Sedimentary sequences and layers architecture in the basins bordering ranges recorded the tectonic evolution of the region. Basement, syn–rift, post-rift and three foreland stages were interpreted in the seismic sections according to the arrangement of the horizons and the main outcropping geological units in bordering ranges. Based on seismic data sets and field data, here we document a particular style of activation of basement faults. Thick-skinned structures that are not always related to the tectonic inversion but to the reactivation of older basement anisotropies represent a paradox since they were not active during the rifting stage. A flat slab subduction and a subsequent angle recovery conditioned the structural evolution of the area.

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“…For example, in the Santa Barbara system the foreland deposits have a thickness of approximately 3000 m (Cristallini et al, 1997;Bossi et al, 2001). In the transition to the Subandean ranges, sedimentary thickness increases (Reynolds et al, 2001) and reaches more than 7000 m in the Argentine and southern Bolivian sectors of the Subandean fold-and-thrust belt (Echavarria et al, 2003;Uba et al, 2006). The hydrologic connectivity of basins within this broken foreland has varied over geologic time.…”

Section: Retroarc Topography Deformation and Deposition In The Centmentioning

confidence: 99%

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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Subandean thrust and fold belt of northwestern Argentina: Geometry and timing of the Andean evolution

Cited by 160 publications

References 32 publications

Cenozoic Evolution of Hinterland Basins in the Andes and Tibet

Cenozoic Evolution of Hinterland Basins in the Andes and Tibet

Basin fragmentation controlled by tectonic inversion and basement uplift in Sierras Pampeanas and Santa Bárbara System, northwest 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

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