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Pervasive Deformation of an Oceanic Plate and Relationship to Large >M 8 Pervasive deformation of an oceanic plate and relationship to large >Mw 8 intraplate earthquakes: The northern Wharton Basin, Indian Ocean Jacob Geersen1,2*, Jonathan M. Bull1, Lisa C. McNeill1, Timothy J. Henstock1, Christoph Gaedicke3, Nicolas Chamot-Rooke4, and Matthias Delescluse4 1University of Southampton, National Oceanography Centre Southampton, European Way, Southampton SO14 3ZH, UK 2GEOMAR Helmholtz Centre for Ocean Research Kiel, Wischhofstr. 1-3, 24148 Kiel, Germany 3Bundesanstalt für Geowissenschaften und Rohstoffe (BGR), Stilleweg 2, 30655 Hannover, Germany 4ENS Laboratoire de Géologie, CNRS UMR8538, PSL Research University, Paris, France ABSTRACT the Sunda Trench in the area that ruptured in the Large-magnitude intraplate earthquakes within the ocean basins are not well understood. 2012 earthquakes. The Mw 8.6 and Mw 8.2 strike-slip intraplate earthquakes on 11 April 2012, while clearly occurring in the equatorial Indian Ocean diffuse plate boundary zone, are a case in point, SEISMO-STRATIGRAPHIC with disagreement on the nature of the focal mechanisms and the faults that ruptured. We INTERPRETATION use bathymetric and seismic reflection data from the rupture area of the earthquakes in the The seismic data show three sedimentary units northern Wharton Basin to demonstrate pervasive brittle deformation between the Ninet- (Fig. 2; see the GSA Data Repository1) based on yeast Ridge and the Sunda subduction zone. In addition to evidence of recent strike-slip defor- stratigraphic geometry and reflection attributes, mation along approximately north-south–trending fossil fracture zones, we identify a new with total sediment thickness from 1000 m to type of deformation structure in the Indian Ocean: conjugate Riedel shears limited to the >4000 m (see also Geersen et al., 2013). Unit 1 is sediment section and oriented oblique to the north-south fracture zones. The Riedel shears present only in the central and eastern study area developed in the Miocene, at a similar time to the onset of diffuse deformation in the central and represents the trench wedge characterized Indian Ocean. However, left-lateral strike-slip reactivation of existing fracture zones started by parallel, high-amplitude reflectors onlapping earlier, in the Paleocene to early Eocene, and compartmentalizes the Wharton Basin. Modeled an unconformity (blue line in Fig. 2) separating rupture during the 11 April 2012 intraplate earthquakes is consistent with the location of two units 1 and 2. The distance between the defor- reactivated, closely spaced, approximately north-south–trending fracture zones. However, we mation front and the westernmost point of unit 1 find no evidence for WNW-ESE–trending faults in the shallow crust, which is at variance with combined with the convergence rate between the most of the earthquake fault models. Indo-Australian and Sunda plates gives an age of ca. 4 Ma (ca. 3.9 Ma, northern transect; ca. INTRODUCTION between ca. 36.5 Ma and 83 Ma (Fig. 1A; Dep- 4.3 Ma, southern transects) for the unit 1–unit 2 The breaking and fracturing of the Indo-Aus- lus et al., 1998; Carton et al., 2014; Jacob et al., boundary. Unit 2 is characterized by parallel, tralian plate is a spectacular example of an active 2014). These fracture zones recently attracted high-amplitude reflectors representing Bengal- diffuse plate boundary within the ocean basins. attention due to the 11 April 2012 Mw 8.6 and Nicobar Fan deposits. Buried channels are vis- In the Central Indian Basin, seismic reflection Mw 8.2 strike-slip intraplate earthquakes, which ible in units 1 and 2. Unit 3 can be distinguished data have imaged compressional faulting and seem to have been promoted by stress transfer from unit 2 by a low-amplitude reflection pattern, long-wavelength folding with an onset around following the A.D. 2004 and 2005 Sunda mega- lack of channels, and increased seismic velocity 15 Ma associated with north-south P axes (Bull thrust events (Delescluse et al., 2012). Although (Singh et al., 2011). The seismic properties of and Scrutton, 1992; Chamot-Rooke et al., 1993; modeling of the earthquake sequence is compli- unit 3 and its position directly above the Paleo- Krishna et al., 2001; Delescluse et al., 2008; Bull cated by the absence of remote-sensing and geo- cene oceanic basement suggest it is composed et al., 2010). In sharp contrast, within the Whar- detic measurements as well as by the complex of pelagic sediments. Unit 3 pre-dates Bengal- ton Basin, east of the Ninetyeast Ridge where faulting scenario, most earthquake models agree Nicobar Fan deposition at this latitude, which the Indo-Australian plate subducts beneath the that the Mw 8.6 main shock involved rupture on probably started in the middle Eocene, ca. 40 Sunda plate (Fig. 1A), deformation is predomi- one NNE-SSW–trending and two WNW-ESE– Ma (Curray et al., 1982). Based on the approxi- nantly strike slip with northwest-southeast P trending faults, with most of the seismic moment mated ages of the unit boundaries (unit 1–unit axes (Petroy and Wiens, 1989; Stein et al., 1989; released during NNE-SSW rupture (Meng et al., 2 = ca. 4 Ma; unit 2–unit 3 = ca. 40 Ma), we Delescluse and Chamot-Rooke, 2007). The spa- 2012; Wei et al., 2013). The Mw 8.2 aftershock, estimate the ages of seismic horizons assuming tial changes in deformation style are broadly which occurred two hours later, ruptured a sec- constant unit sedimentation rates (see inset table explained by Euler poles that define diffuse ond NNE-SSW–trending fault (Fig. 1; Wei et in Fig. 2). These data provide an approximate plate boundaries between the Indian, Capricorn, al., 2013). Due to sparse geophysical data cover- chronology for the stratigraphy that we believe is and Australian plates (Royer and Gordon, 1997; age, the basin-wide deformation pattern and its sufficient to resolve not only relative fault activ- Bull et al., 2010; Sager et al., 2013). temporal evolution are poorly understood. Here, ity but their absolute slip history. The top of the The Wharton Basin is dissected by long, we discuss multibeam bathymetry and seismic oceanic basement (TOB) defines the base of unit approximately north-south–trending fossil reflection data collected prior to the 2012 earth- 3, and is undulating and offset as much as ~900 fracture zones formed at the Wharton Ridge quakes, extending from the Ninetyeast Ridge to m by some faults (red arrows in Fig. 2). *E-mail: [email protected] 1GSA Data Repository item 2015129, high-resolution image of the seismic transects without interpretation, is available online at www.geosociety.org/pubs/ft2015.htm, or on request from [email protected] or Documents Secretary, GSA, P.O. Box 9140, Boulder, CO 80301, USA. GEOLOGY, April 2015; v. 43; no. 4; p. 359–362; Data Repository item 2015129 | doi:10.1130/G36446.1 | Published online 27 February 2015 GEOLOGY© 2015 Geological | Volume Society 43 | ofNumber America. 4 Gold| www.gsapubs.org Open Access: This paper is published under the terms of the CC-BY license. 359 Downloaded from http://pubs.geoscienceworld.org/gsa/geology/article-pdf/43/4/359/3548885/359.pdf by guest on 27 September 2021 Figure 1. A: Overview map 86˚ 88˚ 90˚ 92˚ 94˚ 90˚ 96˚91˚ 92˚98˚ 93˚ 10094˚ ˚ 91.0°91.5° 92.0°92.5° 93.0°93.5° 6˚ 6˚ 4.5° Fracture zones of eastern Indian Ocean 10˚ N 280 Multibeam bathymetry data ic Riedel shears (P) B A Sumatra S (data from GEBCO_08 o Riedel shears (R) 6 ONN Forearc Fig. 1D n b E 5˚ Seismic transects 5˚ 11 186- 240 this study Grid, version 20091120 a r Deformation front MD 2 F P-axes 4.0° [www.gebco .net /data a 200 n _and_products /gridded 8˚ 4˚ 4˚ Bengal Fa F8? 160 2 280 0 _bathymetry_data/]). 1 , 1 0 ig. 1E 240 3.5° Fracture zones (red solid 1 F 3˚ 3˚ 120 6- lines) and Wharton fossil Sunda 200 ast-Ridge Wharton BGR0 6˚ IN e , 104, 105 ridge (red dotted lines) Plate Basin Central 80 06-103 160 2˚ 2˚ 3.0° after Jacob et al. (2014). Indian AU Ninety BGR 40 120 Blue lines are faults Basin F7 F6 s F8 F7 F6 F 80 2012 modeled for the A.D. 1˚ 1˚ 0km earthquak 4˚ 90˚ 91˚ 92˚ 93˚ 94˚ rupturee Seismic 40 Jacob et al. (2014) 2.5° 2012 intraplate earth- ransect Fracture zones T Fig. 1C ) quakes (Wei et al., 2013). 0km 8 16 2012 earthquake F8 6 India (IN)–Australia (AU) rupture 4 West 2 East Faults (# 0 relative plate motion ° 0 0 0 0 0 0 2˚ 0 C 0 32 33 34 35 01 02 03 from Sager et al. (2013). Trend at seafloor Focal mechanisms: red ~N-S Fracture zones are main shocks of the F8? Riedel shears (R) 11 April 2012 intraplate 0˚ Mw 8.2 / 8.6 F6 ast-Ridge 11 April 2012 earthquakes; black are e F7 aftershocks (until 31 Wharton Basin April 2012) (both from Ninety 0km1020 International Seismo- −2˚ Wharton logical Centre catalogue, Fossil Ridge D www.isc.ac.uk/iscgem/); 0km1020 green are historic events es ~N-S Fracture zones −4˚ n Riedel shears (R) (A.D. 1897–2005) from F6 Indo- n Delescluse and Chamot- Mw 8 Plate F7 Rooke (2007). B: Multi- cture Zo Australia Mw 6 0km 150 300 beam bathymetric data Fra Mw 4 −6˚ from study area. Purple 86˚ 88˚ 90˚ 92˚ 94˚ 96˚ 98˚ 100˚ ~N-S Fracture zones E (west) and orange (east) Riedel shears (P) 0km1020 lines represent seafloor lineaments (compare panels C, D, and E), with inset histogram in bottom right corner showing their strike direction. Fracture zones (F6, F7, F8) after Jacob et al.
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