Abstract
SUMMARYTectonic slivers form in the overriding plate in regions of oblique subduction. The inner boundaries of the sliver are often poorly defined and can consist of well-defined faults, rotating blocks or diffuse fault systems, which pass through or near the volcanic arc. The Guanacaste Volcanic Arc Sliver (GVAS) as defined by Montero et al., is a segment of the Central American Forearc Sliver, whose inner boundary is the ∼87-km-long Haciendas-Chiripa fault system (HCFS), which is located ∼10 km behind the volcanic arc and consists of strike slip faults and pull apart steps. We characterize the current ground motion on this boundary by combining earthquake locations and focal mechanisms of the 2016 Bijagua earthquake sequence, with the surface ground deformation obtained from Interferometric Synthetic Aperture Radar (InSAR) images from the ALOS-2 satellite. The coseismic stack of interferograms show ∼6 cm of displacement towards the line of sight of the satellite between the Caño Negro fault and the Upala fault, indicating uplift or SE horizontal surface displacement. The largest recorded earthquake of the sequence was Mw 5.4, and the observed deformation is one of the smallest earthquakes yet detected by InSAR in the Central American region. Forward and inverse models show the surface deformation can be partially explained by slip on a single fault, but it can be better explained by slip along two faults linked at depth. The best-fitting model consists of 0.33 m of right lateral slip on the Caño Negro fault and 0.35 m of reverse slip on the Upala fault, forming a positive flower structure. As no reverse seismicity was recorded, we infer the slip on the Upala fault occurred aseismically. Observations of the Bijagua earthquake sequence suggests the forearc sliver boundary is a complex and diffuse fault system. There are localized zones of transpression and transtension and areas where there is no surface expression suggesting the fault system is not yet mature. Although aseismic slip is common on subduction interfaces and mature strike-slip faults, this is the first study to document aseismic slip on a continental tectonic sliver boundary fault.
Highlights
When tectonic plates converge obliquely, the slip is partitioned into a trench perpendicular component taken up by subduction and a trench parallel component accommodated within the overriding plate (e.g. Jarrard 1986; McCaffrey 1996a)
We focus on the Guanacaste Volcanic Arc Sliver (GVAS) Costa Rica, which formed as a result of the oblique plate convergence of the Cocos Plate beneath the Caribbean plate, at a rate of ∼88 mm yr−1 and angle of N23◦E (e.g. DeMets 2011, Fig. 1)
We consider the relationship between the deformation and the two largest earthquakes of the seismic sequence that occurred at the SE of the Cano Negro fault (CNF) trace, as they are the only ones large and shallow enough to generate detectable ground deformation (Funning & Garcia 2018)
Summary
When tectonic plates converge obliquely, the slip is partitioned into a trench perpendicular component taken up by subduction and a trench parallel component accommodated within the overriding plate (e.g. Jarrard 1986; McCaffrey 1996a). Jarrard 1986; McCaffrey 1996a) This leads to the formation of a tectonic sliver or microplate, which typically acts as a rigid block between the trench and a bounding fault system. The boundary fault system consists of one or more strike slip faults, such as the Sumatra Fault that bounds the Sumatra forearc McCaffrey 1996b), and the Liquine-Ofqui faults that bounds the Central and Southern Chilean forearcs The trench parallel component of motion is accommodated by block rotation, such as in the Mentawai forearc sliver off Sumatra (Berglar et al 2017), the Aleutian forearc (Geist et al 1988), the Cascadia forearc
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