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Abrupt Change in the Dip of the Subducting Plate Beneath North Chile E

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Abrupt Change in the Dip of the Subducting Plate Beneath North Chile E LETTERS PUBLISHED ONLINE: 8 APRIL 2012 | DOI: 10.1038/NGEO1447 Abrupt change in the dip of the subducting plate beneath north Chile E. Contreras-Reyes1*, J. Jara1,2, I. Grevemeyer3, S. Ruiz1* and D. Carrizo1,2 No large tsunamigenic earthquake has occurred in north Chile thrust interface during the past ∼130 years4,9. An earthquake with since 1877 and the region has been largely recognized as a similar characteristics occurred in 1967 (Mw 7.4), which ruptured mature seismic gap1–9. At the southern end of the seismic gap, at 46–48 km depth just north of the 2007 event8. Both the 1967 and the 2007 Mw 7.7 Tocopilla earthquake ruptured the deeper 2007 events should be considered as precursors of an expected larger seismogenic interface, whereas the coupled upper interface tsunamigenic earthquake that could partially or completely rupture remained unbroken4,6,7. Seismological studies onshore show the ∼550-km-long seismic gap in north Chile. a gently varying dip of 20◦ to 30◦ of the downgoing Nazca The Tocopilla epicentre underlies a spectacular coastal scarp, a plate3,6, which extends from the trench down to depths of major trench-parallel morphological feature of the leading edge of 40–50 km. Here, we study the lithospheric structure of the the forearc, which extends >1,000 km along the northern Chilean subduction zone of north Chile at about 22◦ S, using wide- coast with an average height of 1,000 m. This coastal scarp forms angle seismic refraction and reflection data from land and part of the Coastal Cordillera; a trench-parallel morphological sea, complemented by hypocentre data recorded during the province formed mainly by an extinct, exhumed and uplifted 2007 Tocopilla aftershocks7. Our data document an abrupt Mesozoic palaeomagmatic arc. Some authors have suggested that increase in the dip of the subducting plate, from less than underplating at the base of the continental crust caused by 10◦ to about 22◦, at a depth of approximately 20 km. The subduction erosion may be responsible for the tectonic evolution distribution of the 2007 aftershocks indicates that the change of the leading edge of the forearc11–17. in dip acted as a barrier for the propagation of the 2007 Neotectonic studies reveal that the coastal scarp is a young earthquake towards the trench, which, in turn, indicates that and active feature formed during the past three to six million the subduction megathrust is not only segmented along the years12,15,18. However, there are controversial hypotheses explaining trench, but also in the direction of the dip. We propose that its origin and there is no consensus at present. Hypotheses include large-magnitude tsunamigenic earthquakes must cross the that the coastal scarp was formed by crustal extensional faulting barrier and rupture the entire seismogenic zone. and coastal uplift15, that this feature is not tectonic related but The Chilean subduction zone is an extremely active convergent is the result of marine erosion related to coastal subsidence16, or margin producing large earthquakes (Mw > 8) about every ten years that it has a tectonic-erosive origin associated with coastal active and capable of generating at least one tsunamigenic megathrust faulting and fault scarp retreat owing to marine erosion17. Owing earthquake per century. These earthquakes occur in the seismogenic to the large scale and the trench-parallel geometry of the coastal contact between the subducting oceanic Nazca and overriding scarp, it is likely that this major feature must be related to the continental South American plates. In particular, north Chile zone of coupling between the oceanic Nazca and continental South (19◦–23◦ S) has been identified as a mature seismic gap not American plates12,15. However, the genesis of the coastal scarp still having experienced a tsunamigenic megathrust earthquake since remains under debate due mainly to the lack of marine data. the Iquique event in 1877 (Mw 8.8; refs 1–9). The rupture zone To better understand the seismogenic contact zone and its of this historic event is bounded in the north and south by the link with the overriding crustal deformation, we studied the 1868 (Mw 8.8; ref. 2) and 1995 (Mw 8.1; ref. 3) earthquake upper lithospheric structure of the subduction zone of north rupture areas, respectively (Fig. 1a). An important portion of the Chile at ∼22◦ S using amphibious wide-angle refraction and southern Peru 1868 earthquake rupture area broke in 2001 with reflection data. This data set is complemented by accurate the Arequipa megathrust earthquake (Mw 8.4; ref. 10) releasing hypocentre data of the 2007 Tocopilla aftershocks recorded by a considerable amount of slip accumulated during >130 years. a local network installed in the region7 (Fig. 1). The wide- In contrast, only a few events with 7 < Mw < 8 have occurred in angle seismic data were acquired in 1995 during the Crustal north Chile since 1877, and they were not large enough to release Investigations on- and offshore Nazca/Central Andes (CINCA) a significant part of the slip accumulated in the region during project with the German RV SONNE (refs 19–21). The gross the past ∼130 years, which is at present largely or completely seismic structure of the margin was modelled from land explosions 4,5,9 19 coupled . This was the case of the 2007 Tocopilla event (Mw 7.7) and air gun shots recorded only at land stations . However, which ruptured the southern region of the seismic gap (Fig. 1). the data from the ocean bottom hydrophones (OBHs) deployed Seismological and geodetic data indicate that the earthquake offshore Tocopilla were not included in that modelling. Here, rupture is confined in the deeper part (30–55 km) of the thrust we included 19 OBHs deployed along the trench region and interface4,6,7 whereas the upper plate contact remains unbroken. continental slope, which enabled us to image in great detail the Furthermore, the Tocopilla event presents low coseismic slip (<3 m) subduction interface and inner structure of the marine forearc. and released only 2–4% of the moment deficit accumulated in the Thus, we jointly used sea shots recorded in 19 marine and 30 1Departamento de Geofísica, Facultad de Ciencias Físicas y Matemáticas, Universidad de Chile, Blanco Encalada 2002, Santiago, Chile, 2Advanced Mining Technology Center, Universidad de Chile, Blanco Encalada 2002, Santiago, Chile, 3GEOMAR, Helmholtz Centre of Ocean Research, Wischhofstraße 1-3, D-24148 Kiel, Germany. *e-mail: [email protected]; [email protected]. 342 NATURE GEOSCIENCE j VOL 5 j MAY 2012 j www.nature.com/naturegeoscience © 2012 Macmillan Publishers Limited. All rights reserved. NATURE GEOSCIENCE DOI: 10.1038/NGEO1447 LETTERS a 1868 M 8.8 18 2001 w M 8.4 w b –2 –1 20 0 S) 1877 ° 1 Mw 8.8 Depth (km) 2 1967 –45 –30 –15 0 15 Latitude ( 22 Mw 7.4 Distance from the coast (km) 2007 Mw 7.7 24 1995 Mw 8.1 –8 –6 –4 –2 0 2 4 6 72 70 68 Topography (km) Longitude (° W) Longitude (° W) c 72 71 70 69 68 2007 M 7.7 w 050 : OBH Domeyko km : Land stations Cordillera ∗ ∗ 22 : Land shots 39 ∗ ∗ W S28 este S) rn Andes ° Nazca plate Latitude ( AFS 23 66 mm yr-1 Mejillones Salar de Peninsula South Atacama American plate Figure 1 j Seismotectonic setting of north Chile and seismic experiment. a, Rupture areas of historic and recent earthquakes. b, Coastal topography along the studied seismic line. c, Swath bathymetry and topography22,25, and location of the seismic experiment. The green dot and triangle indicate the seismic stations shown in Fig. 2. The purple star indicates the epicentre of the 2007 earthquake and the surrounding black dots indicate the aftershocks7. The dashed line denotes the Atacama fault system (AFS) that stretches linearly for ∼1;100 km at an average distance of 30–50 km from the shore line15. land seismic stations, and additionally we included two land coupled owing to the high fracturing degree and fluid pore pressure shots (Fig. 1c). The total length of the seismic profile is ∼420 km caused by subduction erosion20,22. and samples the trench outer rise, fore- and magmatic arcs. As observed in Fig. 2a, the plate geometry landward of ∼170 km Continental crustal refractions (Pg1), reflections from the top of and for depths >30 km is unconstrained by the wide-angle seismic the oceanic crust (PtocP), intracrustal continental reflections (PicP), data alone. We have therefore continued the geometry of the oceanic crustal refractions (Pg2) and oceanic Moho wide-angle plate boundary landward by fitting it to hypocentre data of the 7 reflections (PmP), were recorded with excellent quality, from which Tocopilla 2007 aftershocks . The results show that the slab dip a two-dimensional velocity model was derived by tomographic increases abruptly from 10◦ to about 22◦ at ∼85 km from the inversion (Fig. 2a). Figure 2b,c shows representative examples of trench axis. PtocP reflections recorded in both marine and land seismic record sections including the identified seismic phases stations deployed in the coastal region constrain the upper slab ◦ (see Supplementary Information for modelling, uncertainties and dip to about 10 . Near the slab-dip change, PmP reflections model assessment). recorded at land stations are consistent with the dip change (see The two-dimensional final velocity–depth model shows the Supplementary Information), although the resolution is low due internal structure of the erosive margin of north Chile, which to the lack of rays. Nevertheless, the best constraint for the slab is characterized by a ∼30 − km-wide wedge-shaped body, with dip at depths of 55 km < z < 20 km is the accurate hypocentre velocities ranging between 4.0 and 6:0 km s−1.
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