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Saillard Et Al., 2008.Pdf Earth and Planetary Science Letters 277 (2009) 50–63 Contents lists available at ScienceDirect Earth and Planetary Science Letters journal homepage: www.elsevier.com/locate/epsl Non-steady long-term uplift rates and Pleistocene marine terrace development along the Andean margin of Chile (31°S) inferred from 10Be dating M. Saillard a,⁎, S.R. Hall b, L. Audin a,c, D.L. Farber b,d, G. Hérail a,c, J. Martinod a, V. Regard a, R.C. Finkel d,e, F. Bondoux a,b a Université de Toulouse; UPS (SVT-OMP); LMTG; 14 Av, Edouard Belin, F-31400 Toulouse, France b University of California, Santa Cruz, Department of Earth Sciences, Santa Cruz, CA 95060, USA c IRD; LMTG; F-31400 Toulouse, France d Lawrence Livermore National Laboratory, LLNL, Livermore, CA 94550, USA e University of California, Berkeley, Department of Earth and Planetary Sciences, Berkeley, CA 94720, USA a r t i c l e i n f o a b s t r a c t Article history: Pleistocene uplift of the Chilean coast is recorded by the formation of wave-cut platforms resulting from Received 21 January 2008 marine erosion during sea-level highstands. In the Altos de Talinay area (~31°S), we have identified a Received in revised form 18 September 2008 sequence of 5 wave-cut platforms. Using in situ produced 10Be exposure ages we show that these platforms Accepted 26 September 2008 were formed during interglacial periods at 6, 122, 232, 321 and 690 ka. These ages correspond to marine Available online 22 November 2008 isotopic stages (MIS) or substages (MISS) 1, 5e, 7e, 9c and 17. Shoreline angle elevations used in conjunction Editor: C.P. Jaupart with our chronology of wave-cut platform formation, illustrate that surface uplift rates vary from 103± 69 mm/ka between 122 and 6 ka, to 1158±416 mm/ka between 321 and 232 ka. The absence of preserved Keywords: platforms related to the MIS 11, 13 and 15 highstands likely reflects slow uplift rates during these times. We Beryllium-10 suggest that since 700 ka, the Altos de Talinay area was predominantly uplifted during 2 short periods marine terrace following MIS 17 and MISS 9c. This episodic uplift of the Chilean coast in the Pleistocene may result from Pleistocene subduction related processes, such as pulses of tectonic accretion at the base of the forearc wedge. uplift rate © 2008 Elsevier B.V. All rights reserved. Central Andes underplating 1. Introduction the average long-term rate over a time period of ~0.4–1 Ma (Bloom et al., 1974; Bull, 1985; Lajoie, 1986; Burbank and Anderson, 2001; A former assumption used in the analysis of tectonic deformation Marquardt et al., 2004). In this paper, we study and date a sequence of over geodetic (10 yr) and geologic (106 yr) time scales is that the rate five marine terraces to constrain the variability of the coastal Andean of deformation should remain constant over these time scales. In uplift rate. Considering that each marine terrace has a time resolution order to resolve this question and provide new constraints for related to one sea-level highstand, our data integrate uplift rate over integrating studies of geodetic, seismologic and geochronologic data, 100 kyr time steps, the periodicity of marine terrace formation. More our study focuses on uplift rate calculations over various time ranges. rapid uplift rate variations that may have occurred during this time This should lead to a unique estimation of long-term rates of step will not be represented on the morphological scale and thus are deformation (Chéry and Vernant, 2006) while, at the same time, not considered. provide an estimation of variability over shorter time scales. This Marine terraces are an important class of geologic markers that are premise is currently being tested (cf. Friedrich et al., 2003; produced through complex interactions between sea-level fluctua- Allmendinger et al., 2005). However when calculating slip- or uplift- tions and uplift along an active margin (Bradley and Griggs, 1976; rates in order to define active tectonics, it was necessary in most of Merritts and Bull, 1989; Anderson et al., 1999; Muhs et al., 1990; Lajoie previous studies to assume that the short-term rate inferred from the et al., 1991) that can in theory, provide important constraints on the displacement of a geologic marker (b100 ka), may be a robust signal of rates of coastal uplift (Chappell, 1983; Lajoie, 1986; Burbank and Anderson, 2001). Along the Andean forearc, sequences of marine terraces record changes in sea-level together with the uplift history of ⁎ Corresponding author. Tel.: +33 5 61 33 26 62; fax: +33 5 61 33 25 60. the coastal area (DeVries, 1988; Hsu, 1992; Goy et al., 1992; Macharé E-mail addresses: [email protected] (M. Saillard), [email protected] and Ortlieb,1992; Ortlieb et al., 1992, 1996; Ota et al., 1995; Zazo, 1999; (S.R. Hall), [email protected] (L. Audin), [email protected] (D.L. Farber), Zazo et al., 1994; Cantalamessa and DiCelma, 2004; Marquardt et al., [email protected] (G. Hérail), [email protected] (J. Martinod), [email protected] (V. Regard), [email protected] (R.C. Finkel), 2004; Pedoja, 2003; Pedoja et al., 2006; Quezada et al., 2007). [email protected] (F. Bondoux). However, at many locations (e.g., Papua New Guinea, USA, Peru, Chile, 0012-821X/$ – see front matter © 2008 Elsevier B.V. All rights reserved. doi:10.1016/j.epsl.2008.09.039 M. Saillard et al. / Earth and Planetary Science Letters 277 (2009) 50–63 51 Ecuador) where marine terraces have been studied, steady uplift is The study area is located above the Pacific shoreline, at the foot of often assumed and chronostratigraphical correlation of the terraces to the Chilean Coastal Cordillera along a ~100 km-long stretch of coast sea-level highstands is used to assign ages due to restricted access to from Tongoy (30.25°S) to south of Bahía El Teniente (31°S; Coquimbo datable material (Muhs et al., 1990; Hsu, 1992; Macharé and Ortlieb, region, Chile; Fig. 1). Due to the subduction of the Nazca Plate beneath 1992; Goy et al., 1992; Ota et al., 1995; Burbank and Anderson, 2001; the South American plate at a rate of ~82 mm/a (DeMets et al., 1994), Cantalamessa and Di Celma, 2004; Pedoja et al., 2006). In this study, this segment of the Chilean coast is seismically active and the area we focus on the Altos de Talinay area of Chile (~30°–31°S). The general experiences a recurrent major interplate event approximately every morphology of the area has been previously described (Paskoff, 1966, 100 yrs (1647, Mw =8.5; 1730, Mw= 8.7; 1880, Mw= 7.7; 1943, 1970; Chávez, 1967; Herm, 1969; Ota et al., 1995; Benado, 2000; Mw=8.3; Beck et al., 1998; Heinze, 2003). Moreover, this region Heinze, 2003). This area shows a well developed sequence of five shows a high degree of seismic coupling between the subducting wave-cut platforms (WCPs) directly abraded into the bedrock. Nazca and the overriding South America plates (Lemoine et al., 2001; Fig. 1. Geodynamic setting of the study area (black box) on bathymetric and topographic digital elevation model of Eastern Pacific Ocean and South America. Velocities are calculated from NNR-NUVEL-1A plate motion model of DeMets et al. (1994). White line with triangles corresponds to the Peru–Chile trench. White line between two dashes mark flat slab subduction zone. Black triangles are active volcanoes. Black stars with numbers correspond to previously study marine terrace locations. 1: Ecuador – north of the Talarac Arc (Cantalamessa and DiCelma, 2004; Pedoja, 2003; Pedoja et al., 2006). 2: Northern Peru – south of the Talarac Arc (DeVries,1988; Pedoja, 2003; Pedoja et al., 2006). 3: Southern Peru – above the Nazca Ridge and Chala Bay (Hsu,1992; Goy et al.,1992; Macharé and Ortlieb,1992; Zazo,1999; Saillard, 2008). 4: Southern Peru – Ilo (Ortlieb et al.,1992; Zazo et al.,1994; Saillard, 2008). 5: Chile – Mejillones area (Ortlieb et al., 1996; Zazo, 1999). 6: Chile – Caldera (Marquardt et al., 2004; Quezada et al., 2007). 7: Chile – Altos de Talinay area (Ota et al., 1995; Saillard, 2008). 52 M. Saillard et al. / Earth and Planetary Science Letters 277 (2009) 50–63 Pardo et al., 2002; Gardi et al., 2006). This suggests that the upper 33°S, the morphology of the margin along this segment of the Andean plate morphology may display evidence of the ongoing subduction Cordillera does not show a Central Depression nor an active volcanic processes related to the position of the seismogenic zone (i.e. marine arc. This particular morphological sequence is developed above a terraces or/and active tectonics; Audin et al., 2008). segment of flat subduction – between 30°S and 33°S – which is In the Coquimbo region, the Coastal Cordillera progressively passes bordered to the north and south by normal dipping subduction zones to the Precordillera and finally the high Cordillera of the Andes. In (Gutscher et al., 2000; Yañez et al., 2001; Fig. 1). Yañez et al. (2001) contrast to the morphology north of La Serena (~29.9°S) or south of suggest that the flat slab segment of the Nazca plate in this area is Fig 2. Map of the study area showing the morphostructural units (modified from Heinze, 2003), the distribution of marine terraces, major faults and rivers. The black boxes outline the location of Fig. 4A and B. PAF: Puerto Aldea Fault. White concentric circles in the Tongoy Paleobay Depression are Losa deposits (see paragraph 2). ‘Cenozoic basin’ corresponds to Tongoy–Limari basin with Cenozoic marine and continental sediments.
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