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Transtensional Deformation of the Western Caribbean–North America Plate Boundary Zone

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Transtensional Deformation of the Western Caribbean–North America Plate Boundary Zone spe428-03 page 37 The Geological Society of America Special Paper 428 2007 Transtensional deformation of the western Caribbean–North America plate boundary zone Robert D. Rogers* Paul Mann John A. and Katherine G. Jackson School of Geosciences, The University of Texas at Austin, 4412 Spicewood Springs Road, Building 600, Austin, Texas, 78759-8500, USA ABSTRACT Divergence, expressed as the angle between the plate motion vector and the azi- muth of a plate margin fault, has been proposed to explain development of contrast- ing styles of transtensional deformation along transform margins. We present the western North America–Caribbean plate margin as a test of this hypothesis. Here, geologic, earthquake, marine geophysical, and remote sensing data show two distinct structural styles: (1) east-west extension along north-trending rifts normal to the plate margin in the western study area (western Honduras and southern Guatema- la); and (2) NNW-SSE transtension along rifts subparallel to the plate margin in the eastern study area (northern Honduras and offshore Honduran borderlands region). Orientations of rifts in each area coincide with the angle of divergence between the GPS-derived plate motion vector and the azimuth of the plate boundary fault, such that the western zone of east-west extension has an angle >10°, while the eastern zone of NNW-SSE extension occurs when the angle of divergence is between 5° and 10°. A narrow transition area in north-central Honduras separates the plate boundary– normal rifts of western Honduras from the plate boundary–parallel rifts to the east. Faults of the offshore Honduran borderlands extend onshore into the Nombre de Dios range and Aguan Valley of northern Honduras where tectonic geomorphology studies show pervasive oblique-slip faulting with active left-lateral river offsets and active uplift of stream reaches. Offshore, seismic data tied to wells in the Honduran borderlands reveal active submarine faults bounding asymmetric half-grabens filled by middle Miocene clastic wedges with continued deposition to Pliocene-Pleistocene. The north-trending rifts of western Honduras form discontinuous half grabens that cut the late Miocene ignimbrite strata. Plate reconstructions indicate the north- trending rifts of western Honduras developed in response to increased interplate divergence as the western margin of the Caribbean plate shifted from the Jocotan fault to the Polochic fault in the middle Miocene. Keywords: Honduran borderlands, oblique divergence, geomorphology, Caribbean plate. *Now at Department of Geology, California State University Stanislaus, 801 West Monte Vista Avenue, Turlock, California 95382, USA; [email protected] tan.edu. Rogers, R.D., and Mann, P., 2007, Transtensional deformation of the western Caribbean-North America plate boundary zone, in Mann, P., ed., Geologic and tec- tonic development of the Caribbean plate in northern Central America: Geological Society of America Special Paper 428, p. 37–64, doi: 10.1130/2007.2428(03). For permission to copy, contact [email protected]. ©2007 The Geological Society of America. All rights reserved. 37 spespe428-03 page 38 38 Rogers and Mann INTRODUCTION strain partitioning to another and where this occurs; and (4) how successive styles of transtension are superimposed as a plate Strain partitioning along plate margins produces complex boundary evolves. but characteristic deformation patterns along plate boundary We present the northwestern margin of the Caribbean plate faults. Most previous studies of strain partitioning have come as an example of strain partitioning in a transtensional setting from transpressive regions where convergent plate motion is and examine in detail the resulting deformational patterns as transformed into components of strike-slip and thrust faulting observed onshore in Honduras and Guatemala and beneath the in either ancient (cf. Teyssier et al., 1995; Jones and Tanner, adjacent Caribbean Sea (Honduran borderlands). This region is 1995; Claypool et al., 2002) or active settings (Marshall et ideal for such a study for several reasons: al., 2000; Calais et al., 2002; Mann et al., 2002; Meckel et al., 1. GPS-based geodesy from DeMets et al. (2000) places 2003). In contrast, there are few examples documented from firm constraints on the variation of interplate motion active transtensional settings where obliquely divergent plate and deformational styles across a 3100-km-long seg- motion is partitioned into coexisting strike-slip and normal ment of the North America–Caribbean plate boundary components of deformation (Ben-Avraham and Zoback, 1992; (Fig. 1). Ben-Avraham, 1992). 2. Plate boundary-related normal faults of a variety of orienta- Key questions for understanding strain partitioning in trans- tions and ages are present in northern Central America and tensional settings include (1) how much strain is accommodated in adjacent areas of the Honduran borderlands (Fig. 2). by strike-slip faulting versus normal faulting along each plate 3. Plate margin faults have known variations in position and boundary segment; (2) what controls different styles of coex- orientation that can be tied to quantitative plate recon- isting strike-slip and normal faulting along a plate boundary; structions based on the opening history of the Cayman (3) what controls the transition from one style of transtensional trough and surrounding plate pairs. North America CUBA Bahama Platform Oceanic Transpression Oblique collision subduction 20o HISP PR Transtension Predicted: 20 Predicted: 20 Strike-slip Observed: 21 Observed: 19 Fig. 2 Caribbean Predicted: 21 Observed: 20.5LA Predicted: 21 Observed: 23 10o Cocos South America Nazca Predicted GPS vector Observed GPSVector 0o -90o -80o -70o -60o Figure 1. Seismotectonic setting of the Caribbean plate. BR in upper diagram is the Beata Ridge. Line LNR shows the general location and trend of the Lower Nicaraguan Rise, which extends ~1000 km northeastward from the Caribbean coast of Nicaragua toward southern Hispaniola. Open diamonds show locations of GPS sites whose velocities are em- ployed in this study. Filled diamond shows 15°N, 75°W fiducial location employed for the analysis. Area enclosed in rectangle is displayed in Figure 6. All earthquakes above depths of 60 km and with surface- or body-wave magnitudes >3.5 for the period 1963 through 2004 are shown in the lower diagram. AVES, BARA, BARB, CRO1, FSD0/1, JAMA, ROJO, and SANA are site names discussed in text. spe428-03 page 39 -90o -88o -86o -84o -82o A Mexico 18o Belize Guatemala SEAMARCII sonar survey 16o Aguan NdDRange Valley N Nicaragua 0 km 100 E. S. Honduras Active rifts Inactive rifts Plateau o o o o o -90 -88 -86 -84 -82MCSC 9.8 6.0 0 B Swan 19.5 o Island 25.9 18 North America 33.3 43.1 CT1-4 CT1-9 49.3 CT1-10 CT1-3 CT1-8 cca B asin Bay Bona Islands CT1-6 FZ CT1-5 nd ca Basin Isla Castana Patu Caribbean an Punta Patuca o w sin 16 S Tela Ba Castilla Gracias a Dios Tela La Ceiba Trujillo Nicaragua SPS Polochic FZ LI Rise Z n F Motagua FZ LY ChamelecoGracias N CG Jocotan- Comayagua 0 km 100 C Rifts Inactive rifts Transition zone Borderlands N N N N W E W E W E W E outer circle = 14% outer circle = 22% outer circle = 33% outer circle = 33% n = 57 n = 9 n = 9 n = 71 mean dir. = 358 mean dir. = 343 mean dir. = 31 mean dir. = 59 Figure 2. GPS site velocities relative to the North America plate on an oblique Mercator map projected about the best- fitting Caribbean–North America pole of rotation. Numerals by site names give the site rates in millimeters per year. Open arrow indicates motion of site ESTI, where the antenna is mounted on a tall steel tower of questionable stability. The location of GPS site BARA discussed in the text is shown in Figure 1. AF—Anegada fault; CSC—Cayman spread- ing center; H—Hispaniola; HND—; LAT—Lesser Antilles trench; MAT—Middle America trench; MDF—Muertos deformed belt; NHDB—Northern Hispaniola deformed belt; NIC—Nicaragua; OF—Oriente fault; PR—Puerto Rico; PRT—Puerto Rico trench; SITF—Swan Islands transform fault; WF—Walton fault. AVES, BARB, CRO1, GUAT, ESTI, FSD0/1, JAMA, ROJO, SANA, and TEGU are site names discussed in the text. spespe428-03 page 40 40 Rogers and Mann STRAIN PARTITIONING OF THE NORTHWESTERN In the Honduran borderlands and the Nombre de Dios range CARIBBEAN PLATE of northern Honduras, normal faults bound elongate rifts and intervening basement blocks that are subparallel to the main left- GPS-determined motion of the Caribbean plate relative to lateral strike-slip plate boundary fault (Swan Islands fault zone) North America predicts significant along-strike variations in (Fig. 2). The westward extent of the borderland faults disappear the style of deformation along the 3100-km-long plate bound- at the longitude of the north-trending Yojoa-Sula rift basin at 88° ary (DeMets et al., 2000) (Fig. 1). The plate boundary extends west (Fig. 2A). from the Motagua Valley of Guatemala to the Lesser Antilles The Motagua fault offsets a staircase of Quaternary river arc and has a GPS-derived rate of mainly left-lateral displace- terraces in the Motagua Valley of Guatemala that yield long- ment of 21 mm/yr. DeMets et al. (2000) note that GPS-based term, left-lateral slip rates of 0.45–1.88 cm/yr (Schwartz et al., interplate velocities are consistent with the along-strike transi- 1979). There is no quantitative estimate of the cumulative lateral tion in structural styles from (1) transtension in northwestern offset on the Motagua fault since alluvium of the Motagua Val- Central America and the western Cayman trough where diver- ley obscures many of the adjoining and presumably offset rock gence between the Caribbean plate vector and the trend of the units. The Motagua fault is directly along strike of the offshore plate boundary faults predicts oblique opening over a wide area; Swan Islands fault to the east and is flanked by the active, left- (2) pure strike-slip faulting in the central Cayman trough where lateral Polochic fault zone to the north (Burkart, 1983; Burkart, the Caribbean plate vector and the trend of the plate bound- 1994) and the inactive Jocotan-Chamelecon fault zone to the ary faults are parallel with strike-slip faults (Rosencrantz and south (Ritchie, 1976).
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