Episodic out-of-sequence deformation promoted by Cenozoic fault reactivation in NW Argentina

Payrola, Patricio; Papa, Cecilia del; Aramayo, Alejandro; Pingel, Heiko; Hongn, Fernando; Sobel, Edward R.; Zeilinger, Gerold; Strecker, Manfred R.; Zapata, S.; Cottle, John M.; Paz, Natalia Salado; Glodny, Johannes

doi:10.1016/j.tecto.2019.228276

Cited by 22 publications

(37 citation statements)

References 72 publications

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“…On the other hand, the broken foreland, as characterized by thick-skinned deformation, cannot be fully explained by flat slabs 47 or the model proposed by this study, because some deformation was as early as 55 Ma 36 , predating flat-slab subduction and the arrival of JFR. This deformation has been proposed to be related to pre-existing structures in the basement 39 , 49 and facilitated by tectonic compression that could be induced by slab–lower mantle interaction 36 . We suggest this deformation does not necessarily represent the start of the major Andean shortening.…”

Section: Discussionmentioning

confidence: 99%

Southward expanding plate coupling due to variation in sediment subduction as a cause of Andean growth

Liu

Gurnis

2021

Nat Commun

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Growth of the Andes has been attributed to Cenozoic subduction. Although climatic and tectonic processes have been proposed to be first-order mechanisms, their interaction and respective contributions remain largely unclear. Here, we apply three-dimensional, fully-dynamic subduction models to investigate the effect of trench-axial sediment transport and subduction on Andean growth, a mechanism that involves both climatic and tectonic processes. We find that the thickness of trench-fill sediments, a proxy of plate coupling (with less sediments causing stronger coupling), exerts an important influence on the pattern of crustal shortening along the Andes. The southward migrating Juan Fernandez Ridge acts as a barrier to the northward flowing trench sediments, thus expanding the zone of plate coupling southward through time. Consequently, the predicted history of Andean shortening is consistent with observations. Southward expanding crustal shortening matches the kinematic history of inferred compression. These results demonstrate the importance of climate-tectonic interaction on mountain building.

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Section: Discussionmentioning

confidence: 99%

Southward expanding plate coupling due to variation in sediment subduction as a cause of Andean growth

Liu

Gurnis

2021

Nat Commun

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“…in the Aguilar Range, Insel et al., 2012) and from the Eastern Cordillera (i.e. in the Sierra de Santa Rosa de Tastil, Cachi Range, Cerro Durazno, Sierra de Chango Real, and Filos del Pelado; Andriessen & Reutter, 1994; Coutand et al., 2006; Deeken et al., 2006; Payrola et al., 2020; Pearson et al., 2013; Villagrán, 2020) – see Figure 11. Similar exhumation ages have been reported from the Eastern Cordillera of Bolivia (e.g.…”

Section: Discussionmentioning

confidence: 99%

“…Documented Paleogene tectono‐sedimentary features (white dots) and Paleogene thermochronological ages (black dots) are shown. Do: Domeyko Range (Maksaev & Zentilli, 1999; Mpodozis et al., 2005); Li: Cordón de Lila Range (Andriessen & Reutter, 1994); Uy: Uyuni area (Horton, Hampton, & Waanders, 2001; Lamb & Hoke, 1997); Tu: Tupiza area (Ege et al., 2007; Horton, 2005; Tawackoli et al., 1996); Ri: Rinconada area (López Steinmetz & Montero‐López, 2019); Ag: Aguilar area (Boll & Hernández, 1986; Insel et al., 2012; Monaldi, Salfity, Vitulli, & Ortiz, 1993); Co: Cobres area (Deeken et al., 2006); SA: Sierra Alta Range (Coutand et al., 2001; Montero‐López et al., 2018); Po: Pozuelos Range (DeCelles et al., 2007); Ma: Macón Range (Jordan & Mpodozis, 2006); Cp: Copalayo Range (Carrapa & DeCelles, 2008); Ta: Tastil Range (Villagrán, 2020); Pa: Pascha Range (Andriessen & Reutter, 1994; Montero‐López, Aramayo, & Ballato, 2017; Villagrán, 2020); La: Lampasillos Range (Hongn et al., 2007; Pearson et al., 2013; Villagrán, 2020); Ca: Cachi Range (Carrapa et al., 2014; Hongn et al., 2007; Pearson et al., 2012); Tt: Tin Tin Range (Hongn et al, 2011; del Papa et al., 2013); FP: Filos del Pelado Range (Payrola et al., 2020); Lu: Luracatao Range (Deeken et al., 2006; Payrola Bosio et al, 2009; Aramayo et al., 2017); CD: Cerro Durazno Range (Coutand et al., 2006; Deeken et al., 2006); SQ: Sierra de Quilmes Range (Aramayo et al., 2017; Mortimer et al., 2007); CR: Chango Real Range (Coutand et al., 2001); Cl : Calalaste Range (Carrapa et al., 2005; Kraemer et al., 1999). Black line shows the western limit of Cretaceous rift activity.…”

Section: Discussionmentioning

confidence: 99%

“…Data from this study, together with information gleaned from other investigations in north‐western Argentina and southern Bolivia (e.g. Lamb & Hoke, 1997; Adelman, 2001; Coutand et al., 2001; Carrapa et al., 2005; Elger et al., 2005; Ege et al., 2007; Hongn et al., 2007; del Papa et al., 2013; Aramayo et al., 2017; Anderson et al., 2018; Montero‐López et al., 2018; López Steinmtez et al, 2020; Payrola et al., 2020), consistently supports the existence of rather isolated but widespread elevated Paleogene topography in the area of the present‐day Puna‐Eastern Cordillera transition zone, as well as in the present‐day Puna (Figure 11). However, little is known about exactly when this region first became a highland area with the plateau characteristics that define todays.…”

Section: Discussionmentioning

confidence: 99%

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Development of an incipient Paleogene topography between the present‐day Eastern Andean Plateau (Puna) and the Eastern Cordillera, southern Central Andes, NW Argentina

et al. 2020

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The structural and topographic evolution of orogenic plateaus is an important research topic because of its impact on atmospheric circulation patterns, the amount and distribution of rainfall, and resulting changes in surface processes. The Puna region in the northwestern Argentina (between 13°S and 27°S) is part of the Andean Plateau, which is the world's second largest orogenic plateau. In order to investigate the deformational events responsible for the initial growth of this part of the Andean plateau, we carried out structural and stratigraphic investigations within the presentday transition zone between the northern Puna and the adjacent Eastern Cordillera to the east. This transition zone is characterized by ubiquitous exposures of continental middle Eocene redbeds of the Casa Grande Formation. Our structural mapping, together with a sedimentological analysis of these units and their relationships with the adjacent mountain ranges, has revealed growth structures and unconformities that are indicative of syntectonic deposition. These findings support the notion that tectonic shortening in this part of the Central Andes was already active during the middle Paleogene, and that early Cenozoic deformation in the region that now constitutes the Puna occurred in a spatially irregular manner. The patterns of Paleogene deformation and uplift along the eastern margin of the present-day plateau correspond to an approximately north-south oriented swath of reactivated basement heterogeneities (i.e. zones of mechanical weakness) stemming from regional Paleozoic mountain building that may have led to local concentration of deformation belts.

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“…To the east, Payrola, del Papa, et al. (2020) also report internal unconformities in the PPFm. Combined, these observations imply a rather continuous deformation history during the sedimentation of the LFM and PPFm.…”

Section: Regional Structures Related To Mio‐pliocene Deformationmentioning

confidence: 96%

Stratigraphic response to fragmentation of the Miocene Andean foreland basin, NW Argentina

et al. 2021

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Foreland basins are sensitive recorders of spatiotemporal variations in tectonic and climatic forcing associated with an approaching orogenic front. Thus, analysis of foreland deposits and their associated deformation patterns and provenance signals allows assessment of tectonic and sedimentary processes during orogeny, providing clues to past environmental conditions. The Calchaquí region in the southern part of the northwest Argentinian Eastern Cordillera (ca. 25-26°S lat) structurally evolved from a contiguous Paleogene foreland of the Andes into a broken foreland and finally an intermontane basin landscape. This history is recorded in the sedimentary sequences of the Mio-Pliocene Angastaco and Palo Pintado Formations. We combine sedimentological methods, U-Pb zircon and K-Ar glass geochronology, clay mineralogy, and geochemical weathering indices with apatite fission track and (U-Th-Sm)/ He thermochronology, structural data, and fault modelling to document the stratigraphic response to the fluvial and tectonic processes that followed the formation of the broken foreland. Our observations suggest that fluvial systems in the Calchaquí region repeatedly changed their location and geometry. These fluvial systems were associated with pro-and retrograding gravel wedges that most likely formed in response to the structural growth of the Aguas de Castilla and Altos de Viñaco ranges that bound the basin to the east. A compartmentalisation of the foreland with restricted fluvial networks must have occurred by ca. 9 Ma. Our results demonstrate that the reconstruction of stratigraphic architectures constitutes a powerful means to better understand intrabasin tectonics and surface uplift in foreland basins.

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Episodic out-of-sequence deformation promoted by Cenozoic fault reactivation in NW Argentina

Cited by 22 publications

References 72 publications

Southward expanding plate coupling due to variation in sediment subduction as a cause of Andean growth

Southward expanding plate coupling due to variation in sediment subduction as a cause of Andean growth

Development of an incipient Paleogene topography between the present‐day Eastern Andean Plateau (Puna) and the Eastern Cordillera, southern Central Andes, NW Argentina

Stratigraphic response to fragmentation of the Miocene Andean foreland basin, NW Argentina

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