Uplift sequence of the Andes at 30°S: Insights from sedimentology and U/Pb dating of synorogenic deposits

Suriano, Julieta; Mardónez, Diego; Mahoney, J. Brian; Mescua, José; Giambiagi, Laura; Kimbrough, David L.; Lossada, Ana Clara

doi:10.1016/j.jsames.2017.01.004

Cited by 34 publications

(28 citation statements)

References 42 publications

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“…By the early to middle Miocene, the magmatic arc was established over the El Indio Belt (Figure b) and was accompanied by tectonic inversion of the Oligocene extensional faults and the development of new structures concentrated within this region (Giambiagi et al, ; Martin, Clavero, & Mpodozis, ; Rodríguez, ; Winocur et al, ). Finally, during middle to late Miocene magmatic activity diminished as the Nazca plate shallowed, and the deformation front migrated eastward, sequentially exhuming the Colangüil range (Fosdick et al, ) and the Precordillera (Suriano et al, ) on the eastern slope of the Andes. Since ~5 Ma active shortening has been located in the easternmost Precordillera and Pampean broken foreland, as a consequence of the established flat slab setting (Ramos et al, ; Siame, Bellier, & Sebrier, ).…”

Section: Tectonic Settingmentioning

confidence: 99%

“…The mechanisms invoked to explain the observed trends include variations in subduction dynamics and age and geometry of the slab (Jordan et al, 1983;Ramos, 2010;Ramos et al, 2004;Yáñez & Cembrano, 2004), inherited rheological heterogeneities of the South American plate (Mpodozis & Ramos, 1989;Ramos et al, 2004;Sobolev and Babeyko, 2005), lithospheric strength variations (Oncken et al, 2006;Tassara & Yanez, 2003), and an enhanced climate erosion feedback (Lamb & Davis, 2003), yet it still remains unclear which mechanism has the greatest influence. While the Miocene is considered the main phase of Andean orogeny at these latitudes (e.g., Allmendinger et al, 1990;Allmendinger & Judge, 2014;Fosdick, Carrapa, & Ortíz, 2015;Jordan et al, 1983;Suriano et al, 2017), several lines of evidence point toward the importance of Paleogene compressive events affecting different sectors of the range. These often overlooked Paleogene events resulted in the initial thickening of the crust and development of high topography, as well as accounting for some of the observed variations in total horizontal shortening.…”

Section: Introductionmentioning

confidence: 99%

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Thermochronologic Evidence for Late Eocene Andean Mountain Building at 30°S

et al. 2017

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The Andes between 28° and 30°S represent a transition between the Puna‐Altiplano Plateau and the Frontal/Principal Cordillera fold‐and‐thrust belts to the south. While significant early Cenozoic deformation documented in the Andean Plateau, deciphering the early episodes of deformation during Andean mountain building in the transition area is largely unstudied. Apatite fission track (AFT) and (U‐Th‐Sm)/He (AHe) thermochronology from a vertical and a horizontal transect reveal the exhumation history of the High Andes at 30°S, an area at the heart of this major transition. Interpretation of the age‐elevation profile, combined with inverse thermal modeling, indicates that the onset of rapid cooling was underway by ~35 Ma, followed by a significant decrease in cooling rate at ~30–25 Ma. AFT thermal models also reveal a second episode of rapid cooling in the early Miocene (~18 Ma) related to rock exhumation to its present position. Low exhumation between the rapid cooling events allowed for the development of a partial annealing zone. We interpret the observed Eocene rapid exhumation as the product of a previously unrecognized compressive event in this part of the Andes that reflects a southern extension of Eocene orogenesis recognized in the Puna/Altiplano. Renewed early‐Miocene exhumation indicates that the late Cenozoic compressional stresses responsible for the main phase of uplift of the South Central Andes also impacted the core of the range in this transitional sector. The major episode of Eocene exhumation suggests the creation of significant topographic relief in the High Andes earlier than previously thought.

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Section: Tectonic Settingmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

Thermochronologic Evidence for Late Eocene Andean Mountain Building at 30°S

et al. 2017

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“…Tectonics 10.1002/2017TC004608 Fosdick et al, 2015;Japas et al, 2016;Levina et al, 2014;Mardonez et al, 2015;Suriano et al, 2017), and few studies describe structures other than those accommodating Miocene-Holocene contraction along the arc and backarc regions. In yet another interpretation, Charchaflié et al (2007) describe normal faults in the northern sector of the belt, in the Veladero area (29.3°S), generated during the 15 to 10 Ma period, apparently controlling the emplacement of ore deposits.…”

Section: Citationmentioning

confidence: 99%

“…On the other hand, Bissig et al () argue that gold deposition occurred several million years after this shortening phase. Indeed, by the time of ore deposition in the metallogenic belt, crustal shortening was focused eastward, in the Argentine Precordillera fold‐and‐thrust belt (Allmendinger & Judge, ; Fosdick et al, ; Japas et al, ; Levina et al, ; Mardonez et al, ; Suriano et al, ), and few studies describe structures other than those accommodating Miocene‐Holocene contraction along the arc and backarc regions. In yet another interpretation, Charchaflié et al () describe normal faults in the northern sector of the belt, in the Veladero area (29.3°S), generated during the 15 to 10 Ma period, apparently controlling the emplacement of ore deposits.…”

Section: Introductionmentioning

confidence: 99%

Cenozoic Shift From Compression to Strike‐Slip Stress Regime in the High Andes at 30°S, During the Shallowing of the Slab: Implications for the El Indio/Tambo Mineral District

Giambiagi

Álvarez²,

Creixell³

et al. 2017

Tectonics

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In the High Andes of central Chile, above the flat‐slab segment, analysis of more than 1,000 fault slip data from Miocene outcrops provides evidence for a change of the regional tectonic regime from compressional to strike slip. This shift in tectonic regime occurred during the waning stages of arc volcanism between 14 and 11 Ma, as a result of the shallowing of the Nazca plate, in conjunction with the migration of deformation to the Precordillera. During the early to middle Miocene, a compressive regime with horizontal σ1 axis (N86°E) was responsible for reverse slip along NNE to N‐striking faults. During the late Miocene, a shift to strike‐slip tectonics took place due to an increase in the absolute magnitude of the vertical stress component as the crust thickened and the gravitational potential energy increase. We argue that instead of the previously accepted highly compressional setting in the arc region during the slab flattening, the change to a strike‐slip regime was the main control on mineralization. Mineralization was controlled by the promotion of fluid expulsion from the magma chambers along active, subvertical strike‐slip fault systems with a high slip tendency, and focusing of fluids in localized areas undergoing extension. Under this strike‐slip regime, the El Indio, Tambo, and La Despensa fault systems formed as dextral strike‐slip systems. The tips and jogsites along these faults experienced local extensional stress fields, forming the El Indio and Tambo mineral districts.

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“…The Iglesia basin formed adjacent to the Argentine Precordillera ( Figure 1), a fold-and-thrust belt that was uplifted during the late Miocene (Suriano et al, 2017), with particularly high shortening rates from 12-9 Ma (Allmendinger & Judge, 2014;Jordan et al, 1993). Shifts in sediment sources and changes in facies, recorded in the foredeep, (e.g.…”

Section: Analogue Setting: the Iglesia Basin (Argentina)mentioning

confidence: 99%

Regional landscape response to thrust belt dynamics: The Iglesia basin, Argentina

et al. 2018

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Intermontane basins are often the result of regionally variable uplift in tectonic settings. Wedge‐top basins, a type of intermontane basin, form along thrust faults within a fold and thrust belt, and provide an ideal environment to study the regional fluvial and surface response to local variations in rock uplift. This study simulates the formation and evolution of an intermontane basin using a landscape evolution model. The modelling results demonstrate that large trunk streams maintain connectivity during basin formation for two reasons: (1) their stream power is enhanced by the capture of smaller streams, enabling them to incise through the uplifting downstream region, and (2) they acquire increased sediment yield to completely infill the upstream accommodation space rather than forming an endorhic basin. During active deformation of the fold‐and‐thrust belt, both channel slope and erosion rates are reduced upstream of the intermontane basin and these changes propagate as a wave of low erosion into the uplands. For a uniform background uplift rate in a landscape previously at steady state, this reduced rate of erosion results in a net surface uplift upstream of the basin. Following the eventual breach of the basin's bounding structural barrier, a wave of high erosion propagates through the basin and increases the channel slope. This onset of increased erosion can be delayed by up to several million years relative to the onset of downstream uplift. Observed paleoerosion rates in paired wedge‐top and foreland basin sequences, and present‐day stream profiles in the Argentine Precordillera support our modelling results. Our results may be extrapolated to other foreland systems, and are potentially identifed using low‐temperature thermochronometers in addition to paleoerosion rates.

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Uplift sequence of the Andes at 30°S: Insights from sedimentology and U/Pb dating of synorogenic deposits

Cited by 34 publications

References 42 publications

Thermochronologic Evidence for Late Eocene Andean Mountain Building at 30°S

Thermochronologic Evidence for Late Eocene Andean Mountain Building at 30°S

Cenozoic Shift From Compression to Strike‐Slip Stress Regime in the High Andes at 30°S, During the Shallowing of the Slab: Implications for the El Indio/Tambo Mineral District

Regional landscape response to thrust belt dynamics: The Iglesia basin, Argentina

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