Abstract

Oblique convergent margins host slip-partitioned faults with simultaneously active strike-slip and reverse faults. Such systems defy energetic considerations that a single oblique-slip fault accommodates deformation more efficiently than multiple faults. To investigate the development of slip partitioning, we record deformation throughout scaled experiments of wet kaolin over a low-convergence (<30°), obliquely slipping basal dislocation. The presence of a precut vertical weakness in the wet kaolin impacts the morphology of faults but is not required for slip partitioning. The experiments reveal three styles of slip partitioning development delineated by the order of faulting and the extent of slip partitioning. Low-convergence angle experiments (5°) produce strike-slip faults prior to reverse faults. In moderate-convergence experiments (10°–25°), the reverse fault forms prior to the strike-slip fault. Strike-slip faults develop either along existing weaknesses (precut or previous reverse-slip faults) or through the coalescence of new echelon cracks. The third style of local slip partitioning along two simultaneously active dipping faults is transient while global slip partitioning persists. The development of two active fault surfaces arises from changes in off-fault strain pattern after development of the first fault. With early strike-slip faults, off-fault contraction accumulates to produce a new reverse fault. Systems with early lobate reverse faults accommodate limited strike-slip and produce extension in the hanging wall, thereby promoting strike-slip faulting. The observation of persistent slip partitioning under a wide range of experimental conditions demonstrates why such systems are frequently observed in oblique convergence crustal margins around the world.

1. INTRODUCTION

Oblique convergence often produces slip-partitioned fault systems that have different slip rakes on multiple parallel striking faults instead of a single fault with oblique slip (e.g., Fitch, 1972; Jones and Wesnousky, 1992; McCaffrey, 1992; Yu et al., 1993; Haq and Davis, 1997; Tikoff and de Saint Blanquat, 1997; Burbidge and Braun, 1998; Bowman et al., 2003; McClay et al., 2004; Leever et al., 2011). Slip partitioning can occur at multiple scales within the crust, ranging from local convergence within restraining bends along strike-slip faults (e.g., Gomez et al., 2007; Fitzgerald et al., 2014; Bemis et al., 2015) to thousands of kilometers along convergent margins (e.g., Fig. 1; Yu et al., 1993; Gaudemer et al., 1995; McCaffrey, 1996; Tikoff and de Saint Blanquat, 1997; Norris and Cooper, 2001). At subduction zones, slip partitioning typically involves two margin-parallel faults with a characteristic geometry: a dipping oblique-slip fault along the trench and a continental vertical strike-slip fault (e.g., Fitch, 1972). The development of two active faults within oblique convergent margins greatly increases the regional extent of seismic hazard and the interaction of slip-partitioned faults can complicate hazard forecasting (e.g., Bayarsayhan et al., 1996; Eberhart-Phillips et al., 2003; King et al., 2005).

Despite abundant documentation and observation, some aspects of the evolution and maintenance of slip-partitioned systems remain unclear. Why do these fault systems employ two active faults rather than a single fault surface with oblique slip? Because work is consumed in the creation of new fault surfaces (e.g., Lockner et al., 1991; Herbert et al., 2015), fault systems with a single oblique-slip fault should be more efficient than systems with two simultaneously active faults. Furthermore, how do previously non-partitioned margins become slip-partitioned? Finally, why do slip-partitioned fault systems remain so rather than shift to a single obliquely slipping fault?

Analytical derivations that employ least-energy or force balance assumptions examine resolved stresses that drive slip along existing strike-parallel dip-slip and strike-slip faults (Michael, 1990; Jones and Wesnousky, 1992; McCaffrey, 1992; Platt, 1993). These studies, along with numerical investigations of convergent margins (e.g., Upton et al., 2003; Vernant and Chéry, 2006), shed insight into the tradeoffs in the strength of faults and/or interfaces and convergence obliquity that act to maintain slip-partitioned fault systems but do not reveal how these systems develop. Numerical models with oblique slip on deep-seated faults highlight the asymmetry of the overlying stress field and show zones of potential faulting in the overlying crust that have distinct slip sense (Braun and Beaumont, 1995; Bowman et al., 2003). However, these numerical models do not elucidate the sequence of fault development or the mechanisms that might maintain slip partitioning.

Scaled physical experiments, with their controlled boundary conditions and known rheology, serve well to test the idealized analytical and numerical models by providing direct observations of emergent faulting (e.g., Schreurs et al., 2006; Cooke et al., 2016). Most of the previous scaled physical experiments investigating slip partitioning have used dry sand and angled basal conveyors or plates to apply oblique convergence to the overlying wedge (e.g., Richard and Cobbold, 1990; Haq and Davis, 1997, 2010; Schreurs and Colletta, 1998; McClay et al., 2004; Leever et al., 2011). In these experiments, the dry sand readily forms new faults and may develop slip partitioning along two simultaneously active faults because of the low cost to grow faults in this relatively weak material. In contrast, the significant strength of crustal materials is ubiquitously evident by persistent slip along unfavorably oriented fault segments and fault networks that utilize preexisting weaknesses.

In this study, we investigate the mechanisms that drive the onset of slip partitioning under oblique convergence both with and without preexisting vertical weaknesses that might simulate an existing transform margin at the onset of convergence. We use kaolin clay as a crustal analog for modeling the evolution of fault systems due to its nonzero cohesion, which facilitates the abandonment and reactivation of individual fault segments and approximates the evolution of faults in the crust (Oertel, 1965; Tchalenko, 1970; Withjack and Jamison, 1986; Ackermann et al., 2001; Eisenstadt and Sims, 2005; Henza et al., 2010; Cooke et al., 2013; Hatem et al., 2015, 2017; Bonini et al., 2016; Bonanno et al., 2017). By recording continuous high-resolution incremental displacements on discrete long-lived faults in the clay, we are able to record the evolution of slip partitioning along faults above an obliquely slipping basal discontinuity. Under convergence angles ranging from 5° to 25°, the experiments both with and without a preexisting vertical weakness demonstrate local and/or global slip partitioning.

2. BACKGROUND

Fitch (1972) first described slip partitioning as “where slip that is oblique to the plate margin is at least partially decoupled between parallel zones of transcurrent faulting and underthrusting.” The more general term “strain partitioning,” as used in many previous studies (e.g., Burbidge and Braun, 1998; Chemenda et al., 2000; McClay et al., 2004; Gomez et al., 2007; Loveless and Meade, 2010; Leever et al., 2011), sometimes includes the decoupling of off-fault deformation, such as buckling or inferred stress orientations, from the overall plate convergence direction. In this study, we will consider only the partitioning of localized strain along faults resulting from slip.

2.1 Development of Slip Partitioning within Oblique-Convergence Experiments

Leever et al. (2011) used digital image correlation (DIC) to track the evolution of slip vectors along faults throughout oblique convergence experiments. This 2011 analysis shows that the slip rake of faults in dry sand changes as the system evolves. While early active faults have oblique slip, the slip vectors evolve to have greater partitioning with faults outboard of the wedge accommodating greater convergence and the fault within the wedge accommodating greater strike-slip (Leever et al., 2011). From these experiments and others (e.g., Schreurs and Colletta, 1998; McClay et al., 2004), we understand that slip partitioning might not develop at the onset of faulting under oblique convergence as considered within analytical and numerical models, but that fault systems can evolve toward slip partitioning.

Previous scaled physical experiments show that convergence angle and fault strength control the initiation and continuation of slip partitioning (Richard and Cobbold, 1990; Schreurs and Colletta, 1998; Chemenda et al., 2000; McClay et al., 2004; Haq and Davis, 2010; Leever et al., 2011). Numerical and analytical models predict that deformation partitioning in brittle materials is limited to convergence angles below ∼25°–30°, measured from trench parallel (Braun and Beaumont, 1995; Burbidge and Braun, 1998; Leever et al., 2011). While experiments with dry sand over oblique conveyors confirm that strong deformation partitioning only develops when the convergence angle is less than 30° (McClay et al., 2004; Leever et al., 2011), Haq and Davis (2010) revealed that slip partitioning will develop in dry sand with convergence angles as high as 60°, when the sand overlies a sliver block that provides a vertical, pure strike-slip dislocation in addition to oblique-convergence dislocation. Because slip partitioning in the crust is observed at plate margins with convergence angles well above the predicted critical threshold of 30° (e.g., Dewey and Lamb, 1992; Yu et al., 1993), preexisting weaknesses in the crust may play a key role in the evolution of slip partitioning (e.g., De Saint Blanquat et al., 1998; Haq and Davis, 2010). Furthermore, scaled oblique-convergence experiments with cohesive material overlying a viscous layer show that a preexisting weakness is needed to produce slip partitioning under 40° oblique convergence (Chemenda et al., 2000). In this study, we investigate the role of a preexisting vertical fault on the development of slip partitioning in weak but cohesive material under a range of convergence angles.

2.2 Properties of Wet Kaolin

Although dry sand has many benefits as an analog for modeling crustal processes (e.g., strain-rate independence, well-constrained properties, and ease of use; Ritter et al., 2016, 2018; Schreurs et al., 2016; Reber et al., 2020), its low cohesion compared to wet kaolin favors the growth of new faults over fault reactivation (e.g., Eisenstadt and Sims, 2005; Cooke et al., 2013). The properties of wet kaolin that produce long-lived faults are particularly important for modeling the evolution of fault systems; the abandonment and reactivation of individual fault segments in scaled physical experiments approximate the fault evolution in the crust (e.g., Clifton et al., 2000; Ackermann et al., 2001; Schlische et al., 2002; Eisenstadt and Sims, 2005; Henza et al., 2010; e.g., Hatem et al., 2015, 2017; Bonini et al., 2016; Bonanno et al., 2017; Toeneboehn et al., 2018).

For the experiments of this study, we follow Hatem et al. (2017) and use #6 tile clay with 5%–10% sand, 30%–35% silt, and 60% clay-sized particles by mass. Rheological tests show that wet kaolin behaves as a Burger’s material, similar to crustal material, with both elastic and viscous properties (Cooke and van der Elst, 2012). We run all the experiments of this study at the same speed, 0.5 mm/min, in order to reduce rate effects from the findings. The strength of clay can be modified by changing its water content. Following the approach of Hatem et al. (2015), we adjust the shear strength of the overlying clay to 103 ± 3.5 Pa, which is five orders of magnitude weaker than the crust, assuming an upper-crustal strength of 10–20 MPa. Since the internal friction angle of wet kaolin is similar to the crust (e.g., Schlische et al., 2002) and density ratio of the wet kaolin to crust is ∼1.6:2.3 g/cm3, the five orders of magnitude strength difference corresponds to about five orders of magnitude scaling difference (Hubbert, 1937; Schlische et al., 2002; Henza et al., 2010; Cooke et al., 2013). Consequently, the strength ratio of wet kaolin to the crust equates 1 cm in the clay box to 0.7–1.4 km in the crust. Because slip partitioning is observed at a wide range of scales, from restraining bends along small strike-slip faults to subduction zones, the interpretations of the experimental results are not limited to the precise scaling of the experimental material. Similarity scaling described by Paola et al. (2009) allows application of experiment results outside of the scaling limits where similar processes are observed across a wide range of scales.

3. EXPERIMENTAL SETUP AND METHODS

For each tested convergence angle, we ran two experiments with identical boundary and loading conditions but different initial faults. One set of experiments has a precut vertical plane in the clay to simulate an existing transform margin at the onset of oblique convergence. A second set of experiments leaves the wet kaolin uncut. Both uncut and precut models simulate the development of faults loaded with oblique convergence, where a deep-seated, oblique-slip fault drives the deformation of the overlying material (e.g., Bowman et al., 2003).

The block geometry in the experiments of this study creates an oblique dislocation where the center block thrusts over the footwall of the driving (i.e., subducting) block (Fig. 2). Previous oblique convergence sand experiments superpose regional contraction and localized strike-slip, without capturing the dipping dislocation that characterizes oblique-convergent subduction margins (e.g., Richard and Cobbold, 1990; Haq and Davis, 2009; Leever et al., 2011). The three-dimensional displacement of the underlying rigid blocks implemented here simulates the oblique-slip dislocation where the overlying crust obliquely thrusts over the subducting slab. The experiments obliquely converge two 2.5-cm-thick rigid blocks with a contact dip of 30°; these blocks underlie an equally thick layer of wet kaolin clay (Fig. 2).

The block above the driving plate is displaced by two stepper motors (x- and y- axis) prescribed with net velocity of 0.5 ± 0.05 mm/min. This block drives toward the central (wedged) hanging-wall block that is allowed to rise along its 30° dipping front and back edges. The center block overrides both the driving block and the fixed block and is bounded laterally by fixed sidewalls. A bull’s-eye level shows if the block remains level as it rises.

We measure the shear strength of the clay before each experiment using the fall cone method (DeGroot and Lunne, 2007). The clay is mixed thoroughly in order to reduce heterogeneities before measuring its shear strength. The depth that a 10 g cone with 60° sides sinks into the clay surface over a 5 second period provides an empirical estimate of undrained shear strength (DeGroot and Lunne, 2007). We then adjust the water content of the kaolin to achieve the desired shear strength of ∼100 Pa. For the experiments presented here, the clay had a water content of 81 ± 1% by mass and shear strength of 104 ± 1 Pa. The upper 1 cm of the kaolin lost 4 ± 1% of water over the course of the 3.5–4-hr-long experiments corresponding to an increase of 5–6 Pa shear strength. The bottom of the clay pack only lost 2 ± 1% of water. For the experiments with a precut vertical surface, we cut the kaolin with an electrified probe that interrupts van der Waals forces and reduces puckering of the wet kaolin.

We document the deformation within each experiment using high-resolution digital images taken every 30 seconds with a pair of Canon® EOS Rebel T3i digital single-lens reflex (DSLR) cameras equipped with standard 18–55 mm lenses. The net stepper motor movement of 0.5 mm/min means this image capture rate records deformation every ∼0.25 mm of driving plate displacement. The resolution of the images ranges from 123 to 133 pixels per centimeter (Table 1). At the end of each experiment, we excavated a trench across the faults without disturbing their geometry in order to confirm the location of the basal dislocation and to observe the fault dips. Although the homogeneously colored kaolin doesn’t immediately reveal faults in cross section, further displacement of the basal blocks produces visible offset of the trench wall along the active faults.

Because the blocks have a width of 50 cm, the maximum lateral displacement is limited to ∼27 cm to maintain an 18-cm-wide region that is free of boundary effects (at least 2.5 cm margin on each side). The thickness and dip of the block contact limit the testable range of convergence to 4.33 cm. We use a 12 × 18 cm region of interest (ROI) for each experiment to capture the lateral variability in deformation.

3.2.1 Displacement Fields from Digital Image Correlation

To determine the horizontal incremental displacement field from successive photos of the deformation, we use digital image correlation (DIC). DIC relies on correlating pixel constellations between each image to determine the incremental displacements. Because the clay’s surface is relatively homogeneous in color and texture, we sieve high-contrast red and black medium grain-sized quartz sand onto the top surface of the clay at the beginning of each experiment to provide passive markers for tracking deformation. For this study, we use the particle image velocimetry (PIV) type of DIC and process the images using PIVlab (Thielicke and Stamhuis, 2014) and the Image Processing Toolbox™ from MATLAB®. Using an adaptive-iterative method (multi-pass) together with 50% overlapping windows, we achieve a final resolution of incremental displacement every 0.9–1.23 mm2 (Table 1).

In addition to collecting images for horizontal displacement fields, a second high-resolution DSLR camera provides images from an alternate perspective. We use these images to record the three-dimensional topography throughout the experiment. We follow the stereovision technique described by Toeneboehn et al. (2018) and describe the methodology within the Supplemental Text1. The uplift evolution confirms the interpretations made from the horizontal incremental displacement fields measured with DIC.

3.2.2 Fault Identification and Slip Sense (Rake)

The curl and divergence of the horizontal incremental displacement field provide spatial and temporal evolution of the strike-slip (vorticity) and contractional (-dilatational) incremental strain, respectively, at stages throughout the experiments. Since the calculation of the curl and divergence of the displacement field are independent of direction, the strains we measure are likewise independent of the orientation of the fault structures. This attribute is particularly helpful for measuring strain along the irregular fault traces; shear strain, εxy, in a global coordinate system doesn’t fully capture shear strain on faults that strike oblique to x and y axes. To assess uncertainty of the incremental strain estimates, we calculate the standard deviation of strain along a transect parallel to the block edge and far from the deforming portion of the ROI (Table 1).

Active faults are identified where the strain from the incremental horizontal displacement field, Δu, exceeds an empirically determined threshold. Hatem et al. (2017) used the first visible detection of offset along lines pressed into the kaolin to determine a shear strain rate threshold for faulting of 0.02 radians per minute. However, this threshold depends on the velocity of the motors, which can vary slightly through the experiment, and was based only on shear strain Because we have both contraction and shear in the oblique convergence system, we need to consider both the divergence and the vorticity of Δu . The total incremental strain sums the absolute values of both the divergence and vorticity, which is twice the curl, of Δu (left side of Equation 1a). Within the framework of Equation 1a, the threshold determined by Hatem et al. (2017) is equivalent to 0.08 times the net incremental displacement across the ROI, Δutot. Through further empirical testing, we found that this threshold works well for distinguishing initial localization of fault from distributed strain surrounding early faults but doesn’t capture reactivation of existing faults, such as the reverse fault at 70 mm of plate displacement in the 5° convergence experiment (Animation 1). To detect localized strain along reactivated faults, we use the threshold of 0.05 times Δutot for experiments of this study (Equation 1b). 
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Each active fault at the surface of the kaolin is manifest as a region with higher than threshold incremental strain. By using a fault threshold lower than that of Hatem et al. (2017), the early active fault zones include regions of surrounding distributed strain; however, this outcome impacts neither the slip sense calculated on the faults nor the evolution of slip partitioning investigated in this study. Once active faults are identified for each frame of the experiment, we calculate the median incremental divergence and vorticity for each fault to represent the overall slip sense of the fault within the ROI.

In order to quantify the obliquity of slip along the active faults at each stage of the experiments, we take the arctangent of the median incremental divergence divided by the vorticity of the portion of the incremental displacement field associated with each identified fault, Δuf. Because divergence provides positive dilatation and positive vorticity corresponds to left-lateral strain, we use the negative of divergence and vorticity for the primarily contractional and right-lateral system investigated here: 
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Using this method, a slip rake of 0° corresponds to a fault with pure dextral strike-slip and 90° corresponds to pure convergence. Faults with slip rakes between 0° and ± 45° have mostly dextral strike-slip (oblique strike-slip) with the sign indicating contraction (+) or extension (−). Slip rakes between +45° and +90° or between −45° and −90° indicate faults with mostly dip-slip (i.e., oblique-reverse [+] or normal [−] faults).

4. EXPERIMENTAL RESULTS

For clarity, we describe the results from the precut and uncut experiments separately. For each suite of experiments, we present strain-evolution animations for experiments that represent different styles of slip-partitioning evolution. Strain-evolution animations for all other experiments are available within the Supplemental Material (Supplemental Animations S1–S7 and Fig. S1 [footnote 1]). Because the stepper motors do not have servo-feedback, the prescribed convergence angle is not precisely matched throughout each of the experiments. Here, we refer to each experiment by the convergence prescribed to the motors and use the DIC data to carefully measure and track the convergence experienced by the kaolin (Table 1).

4.1 Precut Experiments

Across all precut experiments, slip partitioning develops along a laterally continuous sliver block bound by primarily strike-slip and reverse faults. The style of slip-partitioning development varies with convergence angle. For the 5° experiment, shear strain localizes as strike-slip along the precut vertical plane early in the experiment (∼5 mm plate displacement) and later a new reverse fault develops (∼40 mm plate displacement) to produce a slip-partitioned fault system (Animation 1). In contrast, within precut experiments with convergence angles >5°, a reverse fault forms first followed closely in time by strike-slip along the precut vertical fault and associated onset of slip partitioning. Animation 2 shows the incremental strain evolution of the 15° experiment, which is representative of the >5° convergence experiments. Early in the experiments, distributed strain starts to localize onto the new reverse faults. Even this early distributed incremental strain shows some partitioning with a zone of dextral shear closer to the hanging-wall block and contraction farther from the hanging wall (∼10 mm plate displacement, Animation 2). This incremental strain pattern matches the analytical predictions of Bowman et al. (2003) for stress above an oblique dislocation.

As convergence accumulates along the first generation of reverse faults, a second reverse fault forms outboard of the first in all precut experiments, and the earlier set of reverse faults is abandoned. The first generation of reverse faults initiates as echelon faults. As these early segments link, they form a scalloped fault-trace geometry, and the second generation of reverse faults forms lobate segments between the salients of the earlier reverse faults (Animations 1 and 2). The scalloped trace of the reverse faults also produces variable slip sense along different portions of the fault with greater or lesser incremental contraction along bends where the fault trace is oblique to the margin (Animations 1 and 2). Strike-slip along the precut surface continues throughout the development of the imbricate reverse faults.

During the reverse fault initiation, the surface of the kaolin shows a zone of early distributed incremental strain that becomes more localized over 5–10 mm of plate displacement and migrates away from the precut as it localizes (Animations 1 and 2). This strain evolution, which is supported by the uplift patterns (Fig. 3), suggests that the reverse fault grows upward from the underlying dislocation between the basal blocks.

Uplift maps of the 10° precut experiment show many features common to the precut experiments. Before the new reverse fault is well established, the uplift pattern shows a gentle warping of the clay surface across the incipient fault zone (Fig. 3A). The zone of high uplift gradient has irregular geometry along the margin, which correlates with the geometry of early echelon faults that subsequently link to form the scalloped reverse fault (Fig. 3B). The migration of the zone of highest uplift gradient away from the precut surface from 17 to 31 mm of plate displacement is consistent with the upward propagation of the dipping reverse fault. Although the precut surface has slipped by 31 mm of plate displacement (Fig. 4), the uplift map at 31 mm of plate displacement does not show any evidence of dip-slip along the precut surface, which is consistent with the strain analysis that indicates pure dextral slip along this fault (Fig. 4). Portions of the precut surface show slight amounts of dip-slip by the end of the experiment (Fig. 3C).

Once developed, the reverse faults show evidence for temporally variable slip rates (change in color saturation within Animations 1 and 2 and S1–S3 [footnote 1]), which may relate to small shifts in the basal block. For the 5° experiments, the primarily reverse fault temporarily stops slipping or has strain rates lower than the threshold for detecting slip during an interval with reduced measured convergence angle (Fig. 4). The stalled reverse fault reactivates later in the experiment when convergence resumes (Fig. 4).

The moderate convergence experiments develop several (one to three) small extensional features that strike oblique to the precut faults. These features develop adjacent to the dextral fault within the sliver between this fault and the reverse fault. For example, the 15° convergence experiment develops an extensional crack oriented 20° clockwise from the dextral fault at ∼85 mm plate displacement (right side of ROI near dextral fault; Animation 2). The crack in the 15° experiment, as well as those of other moderate-convergence precut experiments, opens too slowly for the incremental dilatational strain associated with opening to be distinguished out of the noise of the DIC. In addition to new extensional cracks in the moderate convergence experiments, the precut vertical fault accommodates increasing degree of extension (rake <0) with increasing convergence angle (Fig. 4).

4.1.1 Fault Geometry in Precut Experiments

We can estimate the geometry of the faults by presuming that all faults extend linearly from the surface trace to the position of the basal dislocation. To confirm this assumption, we created trenches across the faults at the end of each experiment and examined a few of the trenches from the precut experiment in detail (Fig. 5). The observation of faults within the trenches confirms that both strike-slip and reverse faults root at the block edge discontinuity (Fig. 5). Additionally, the dips of faults in the clay generally remain constant with depth (Fig. 5).

Due to the scalloped nature of the reverse faults, the dips of these faults vary spatially across the experiments as well as temporally through the evolution of the system. The minimum dip values are constrained by the fault scarp positioned farthest from the block edge, and the maximum dip approaches vertical where active reverse faults intersect the precut fault. Table 2 presents the range of active reverse fault dips calculated from the distance between the reverse fault trace and the precut surface both at the onset of slip partitioning and later in the experiment. The second generation of reverse faults has shallower dip than the first generation (Table 2). Interestingly, none of the reverse faults dips as shallowly as the 30° dipping basal discontinuity. The increase of fault dip with decreasing convergence is consistent with oblique convergence experiments of dry sand (e.g., Burbidge and Braun, 1998; Leever et al., 2011).

4.1.2 Slip Sense Evolution along Faults in Precut Experiments

To assess the overall slip sense of each fault throughout the experiments, we calculate the median incremental vorticity and divergence along each fault zone and use Equation 2 to find the slip sense. For all precut experiments, the simultaneous occurrence of reverse-slip on one fault and strike-slip on another signals the development of slip partitioning (Fig. 4). Within all precut experiments, once slip partitioning starts, the slip rakes on the reverse and strike-slip faults diverge from each other; the reverse faults accommodate greater contraction, and the strike-slip faults accommodate nearly pure dextral slip, with some extension later in the experiments. This suggests that slip-partitioned systems are more stable than single oblique-slip faults under oblique convergence.

Within the experiment with the lowest tested convergence angle (5°), the mean slip rake along the precut fault remains very close to purely strike-slip. This is lesser convergence than applied to the system, suggesting that early convergent strain is accommodated off of the fault. Just after 20 mm plate displacement, a set of new echelon faults develops with oblique- and mostly strike-slip rake (rake <20°, Fig. 4). With greater plate displacement, these faults link and accommodate greater degree of contraction reaching steady-state slip rake of ∼20°.

For precut experiments with convergence angles of 10° to 25°, reverse faults form first, and the precut surfaces do not show dextral slip until after the reverse faults are established (Animation 2 and Fig. 4). Prior to slip partitioning, the reverse faults have oblique-slip that is initially greater than the applied convergence angle (Fig. 4). This suggests that dextral strain is accommodated off of these faults. After the onset of slip partitioning, the reverse faults accommodate greater contraction as the fault system evolves (Fig. 4). The higher convergence-angle experiments produce higher slip rakes on the reverse faults (greater contraction). While the reverse faults accommodate increased contraction with slip partitioning, the precut surfaces that start with purely dextral slip accommodate increasing degree of extension later in the experiments (rake <0). Interestingly, higher convergence angles result in greater extension on the strike-slip fault (Fig. 4).

4.2 Uncut Experiments

The uncut experiments show three different styles of slip partitioning. The shallow convergence experiment (5° convergence) grows a subvertical dextral slip fault early in the experiment and later develops slip partitioning along almost the entire margin with the development of dipping reverse faults (Animation 3). This evolution is similar to that of the 5° precut experiment except that in the uncut experiment, the dextral fault coalesces from a series of echelon segments. The linkage of the echelon segments resembles that of pure strike-slip experiments within wet kaolin (e.g., Hatem et al., 2017), and the resulting irregular geometry strongly controls the pattern of slip rake on the dextral fault (Animation 3).

The other two styles of slip partitioning arise in the moderate convergence angle (>5° convergence) uncut experiments that all first grow dipping reverse faults. The uncut experiments with convergences angles of 10°–25° all develop local slip partitioning where two generations of dipping faults are simultaneously active. In this region of the experiment, the new outboard and more shallowly dipping fault accommodates greater convergence and the inboard steeper fault accommodates greater strike-slip (Animation 4, 30–70 mm plate displacement). This style of slip partitioning is limited to the region of the experiment where the two generations of faults are both active; this region varies throughout the evolution of the system. Outside of the region of local slip partitioning, deformation is accommodated as oblique slip along a single reverse fault, and the earlier generation is abandoned when the second generation of reverse faults develops.

The third style of slip partitioning involves development of a new strike-slip fault after significant accumulation of reverse-slip along the reverse faults in the 20° and 25° uncut experiments (Animation 4, >70 mm plate displacement). This slip-partitioning style, which extends along the entire experiment, resembles the slip-partitioning style of the precut experiments with moderate-convergence angle, except that the new strike-slip fault grows by coalescence of initially dilatational echelon cracks and develops much later in the experiment. The irregular geometry of this new dextral fault, and corresponding variations in slip rake, owe to the linkage of the echelon cracks.

4.2.2 Fault Geometry in Uncut Experiments

The uplift evolution of uncut experiments follows that of the precut experiments except that within the uncut experiments, the faults with dextral slip are non-vertical and consequently produce local differential uplift (Animation S2 [footnote 1]). Fault trenches made at the end of the 5°–20° uncut experiment confirm the location of the basal dislocation and fault geometry. Fault dips earlier in the uncut experiment cannot be confirmed because, unlike precut experiments, we don’t know the precise position of the basal discontinuity until we observe it within the trench. The position of the reverse fault traces relative to the basal dislocation shows that the overall dip of the reverse faults in the higher-convergence experiments is shallower than dips of reverse faults within the lower-convergence experiments (Fig. 6). These findings are consistent with those of the precut experiments and those in dry sand (Table 2; e.g., Leever et al., 2011). Within the 5° uncut experiment, different echelon strands of the strike-slip fault form with dips ranging from 67° to 90°. The reverse fault dips at the end of the uncut experiments (Fig. 6) are similar to the dips of the second generation of reverse fault dips within the precut experiments (Table 2).

Within the 10° convergence experiment, echelon opening cracks oriented 15°–20° clockwise from the basal discontinuity (at the end of the experiment) develop in the hanging wall of the reverse faults, primarily between the reverse fault and the basal discontinuity (Fig. 6B). Within the 15° convergence experiments, these opening cracks are oriented in 20°–25° clockwise from the basal discontinuity at the end of the experiment (Fig. 6C). At the end of the 20° convergence experiment, the echelon cracks are oriented 20°–35° from the basal discontinuity and have linked up to form a new strike-slip fault with irregular trace (Fig. 6D). Animation 4 shows that the echelon cracks rotate significantly during linkage and evolution to a dextral fault. The new strike-slip fault within the 20° convergence experiment develops over the basal discontinuity.

4.2.3 Slip Sense Evolution along Faults in Uncut Experiments

Within all uncut experiments, the simultaneous slip on two parallel faults with different slip sense indicates the development of slip partitioning (Fig. 7). The onset of both local and global slip partitioning is later in the uncut experiments than the experiments with an existing vertical weakness (Figs. 4 and 7). Furthermore, the onset of slip partitioning is earlier within the higher-convergence experiments. Whether the slip partitioning is local or global, after a second fault develops, the slip sense on the two faults diverge from one another; the steeper fault accommodates greater dextral slip, while the more shallowly dipping fault accommodates greater convergence.

Local slip partitioning in the 10°, 15°, and 20° uncut experiments generally develops earlier for higher-convergence angles (Fig. 7). This is consistent with greater convergence facilitating the development of the second generation of reverse faults that starts local slip partitioning. The local slip partitioning results in slip rakes on the two faults that differ by ∼25° (Fig. 7). The marked decrease in convergence angle from 45 to 52 mm plate displacement for the 15° experiment owes to an episode of slight tilting (back rotation) of the center block beneath the clay. During this period of basal block tilting, the previously oblique-convergence slipping fault accommodates oblique-normal slip. In this experiment, slip partitioning initiated immediately following the block rotation and associated extension.

Global slip partitioning in the 20° and 25° uncut experiments occurs when initially dilatational echelon cracks link and accommodate greater dextral slip (Fig. 7). While the slip sense along the new coalescing fault evolves, the reverse fault accommodates greater contraction than achieved within any of the experiments with local patches of slip partitioning. The local slip partitioning in the uncut experiments has lesser difference between slip rakes on the two faults than the global slip-partitioning styles of either the uncut experiments or the precut experiments (Figs. 4 and 7). Because both faults of the local slip partitioning dip, they are both able to accommodate convergence. This differs from the other two styles of global slip partitioning where the (sub)vertical fault cannot effectively accommodate convergence so that slip rakes differ more substantially between the two slip-partitioned faults.

5. DISCUSSION

Whether or not the experiments have a preexisting vertical weakness, slip partitioning develops in all experiments as one of three different styles. Two of the styles result in persistent slip partitioning along the entire margin of the experiment, while the third style of local slip partitioning is transient. Experiments with low convergence angle of 5° initially develop a strike-slip fault—either along the precut vertical surface or as a newly grown subvertical fault in the uncut experiment. In this first style of slip partitioning, the formation of the reverse fault marks the start of slip partitioning along the entire margin (Fig. 8 top row).

Higher convergence angle experiments (10°, 15°, 20°, and 25°) demonstrate the second and third styles of slip partitioning. The second style of global slip-partitioning evolution arises in the precut experiments with convergence >5° and in the uncut experiments with >15° convergence. In the precut experiments, the vertical weakness does not slip first due to the clamping effect of the convergence. Instead, a new oblique-slip reverse fault forms (Fig. 8 middle row). Once convergent strain is accommodated along the reverse fault, the precut fault begins to slip in strike-slip. This pattern of fault development is well illustrated in the 15° precut experiment (Animation 2). The second style of slip partitioning also develops in some of the higher convergence uncut experiments. Late in the experiments, the 20° and 25° uncut experiments grow a new strike-slip fault that produces global slip partitioning (Animation 4 and Fig. 8). Although the 10° and 15° uncut experiments did not develop a new strike-slip fault, dilatational cracks formed within the hanging wall of the reverse faults. If the experiments had continued to larger strain, these cracks may have coalesced to form a throughgoing dextral fault.

The uncut experiments with 10°, 15°, 20°, and 25° convergence angles also show a third style of local slip-partitioning development. Similar to the precut experiments under these same convergences, a reverse fault first forms in the uncut experiments (Fig. 8). The development of a second generation of reverse faulting outboard of the first can produce local slip partitioning, if both faults remain simultaneously active (Fig. 8 bottom row). Where this happens, the newer reverse fault accommodates greater contraction than the older and steeper dipping fault, resulting in local slip partitioning. This third style of slip partitioning is spatially limited and can be short-lived as the older fault segment becomes abandoned. Margins with the third style of local slip partitioning may develop the second style of global partitioning upon the linkage of new echelon fractures to form a new dextral fault.

5.1 Mechanisms for the Development of Slip Partitioning

The development of two parallel-striking faults that partition slip rather than a single oblique-slip fault may owe to both the geometry of the first fault to form and to asymmetry of the strain field associated with oblique slip. Under low convergence, i.e., 5° convergence tested here, the first fault forms a steeply dipping strike-slip fault. Because this steep fault cannot efficiently accommodate convergence, further deformation of the system leads to accumulation of off-fault contraction (Fig. 9A). The contraction on the driving block side of the strike-slip fault promotes the development of a new dipping reverse fault that marks the onset of slip partitioning. Under moderate convergence, 10°–25° tested here, the first fault to form is a dipping oblique-slip fault with scalloped trace. The along-strike roughness of the fault may limit the degree of strike-slip that the fault can accommodate as strike-slip is impeded around large asperities. Consequently, these scalloped faults more easily accommodate reverse-slip than strike-slip, and their slip rake has greater convergence than the overall convergence of the system (Figs. 4 and 7). Dextral shear strain not accommodated along the scalloped fault subsequently accumulates around the fault (Fig. 9B) and promotes either strike-slip along an existing steeper surface or the development of a new strike-slip fault.

The DIC from the experiments of this study reveal that asymmetry of the strain field around early reverse faults also contributes to the development of strike-slip faults. Dilation along a transect across the ROI within the 15° uncut experiment shows a region of extension within the hanging wall of the reverse fault (Fig. 9C). The development of both new dextral faults and dextral slip along existing surfaces occurs within the region of extension in the hanging wall of the reverse fault. Considering that the overall loading of the system is oblique convergence, the development of local extensional strain, while not unexpected, is nevertheless remarkable. The local extension could arise from a combination of flexure of the clay and/or unclamping by reverse fault slip. Shallow extension near the upper surface of the clay may develop from flexure of the hanging wall associated warping of the clay over the basal discontinuity (Fig. 3). Flexural stresses are only expected to be tensile above the neutral surface and may not account for dextral faulting observed at depth (Fig. 5). Furthermore, the change in fault dip from the 30° basal discontinuity to the steeper reverse fault would enhance contraction at depth. In contrast, dip-slip along the reverse fault may unclamp the full depth of existing surfaces in the hanging wall and promote slip. Such unclamping of strike-slip faults via reverse fault slip has been proposed within crustal slip-partitioned fault systems (e.g., ten Brink and Lin, 2004). Within the experiments of this study, some combination of warping and unclamping can account for why the vertical precut surfaces in the >5° convergence experiments do not slip until after accumulation of reverse-slip along the more shallowly dipping faults. These mechanisms also account for the observation that higher-convergence angle experiments produce greater local dilation on the dextral faults (Figs. 4 and 7); the greater reverse-slip in the higher-convergence experiments increases the local hanging-wall extension.

5.2 Comparison to Oblique Convergence Experiments in Dry Sand

The wet kaolin experiments here show many similar features of fault evolution under oblique convergence as experiments in dry sand. Pairs of slip-partitioned faults in both sand and wet kaolin have slip sense that diverges from one another after the onset of slip partitioning (Figs. 4 and 7; Leever et al., 2011). As faults remain active, the reverse fault accommodates greater convergence, and the subvertical fault accommodates greater strike-slip. This behavior suggests that slip-partitioned fault systems become more stable as they evolve, and slip-partitioned fault systems are not likely to evolve toward a single fault with oblique slip. The stability of fault-slip partitioning in experiments with very different rheology (i.e., dry sand and wet kaolin) and boundary conditions (oblique conveyor and basal discontinuity) suggests that the development and persistence of slip partitioning relies on fault geometry rather than rheologic properties or specifics of loading.

The wet kaolin experiments here show that the presence of a precut surface and higher convergence angles generally lead to slip partitioning at lower total accumulated strain. These results support the conclusions of previous experiments (Chemenda et al., 2000; McClay et al., 2004; Haq and Davis, 2010; Leever et al., 2011) that the evolution of a slip-partitioned fault system is controlled both by the angle of convergence and preexisting weaknesses. In particular, the earlier onset of slip partitioning when the vertical weakness is precut in the wet kaolin supports conclusions by Chemenda et al. (2000) as well as Haq and Davis (2010) that preexisting weak zones foster slip partitioning.

The experiments in wet kaolin develop slip partitioning within stages similar to those proposed by Leever et al. (2011) and also documented by McClay et al. (2004) in dry sand: (1) early strain accumulation, (2) separate formation of reverse- and strike-slip faults, and (3) active slip along both reverse and strike-slip faults. The wet kaolin experiments with moderate-convergence angle resemble experiments in dry sand that develop an early reverse fault before slipping along a strike-slip fault; however, low-convergence angle (5° tested here) produces strike-slip faults prior to reverse faults. The latter behavior is not observed in dry sand oblique-convergence experiments. Leever et al. (2011) observed early echelon cracks under low convergence (4°), but these cracks did not link to form a strike-slip fault until after two reverse faults formed in their experiments. Furthermore, across all of the tested convergence angles, slip partitioning within dry sand experiments develops under less total applied strain for similar convergence angle than in wet kaolin, which may reflect rheologic differences of the two materials. Dry sand is not able to compact as much as wet kaolin; upon compaction, sand forms force chains before localizing reverse faults (e.g., Rechenmacher et al., 2010). Consequently, dry sand readily forms reverse faults early in the oblique-convergence experiments, even under low-convergence angles. In concert with accommodating distributed compaction before localized faulting, the cohesion of the wet kaolin delays the onset of faulting and promotes long-lived activity along existing faults. The utilization of existing weaknesses in the wet kaolin experiments for both slip along precut surfaces and for local slip partitioning, rather than growing new faults, is also consistent with the lower cohesion of wet kaolin compared to dry sand. Despite the rheologic differences between dry sand and wet kaolin, both materials develop persistent slip partitioning along the entire margin, suggesting that this behavior should be expected in a wide range of crustal materials.

5.3 Implications for Development of Slip Partitioning in the Crust

Slip partitioning may initiate either at transform or convergent plate boundaries that begin to accommodate oblique convergence. For example, the Haida Gwaii portion of the Queen Charlotte transform fault in Canada accommodates slight convergence along young reverse faults within this part of the transform fault system (e.g., Lay et al., 2013; Rohr, 2015; Brothers et al., 2018; ten Brink et al., 2018). The low-convergence angle experiments of this study suggest that even with the introduction of convergence, transform faults can remain active because the reverse-slip on the new contractional fault system unclamps the transform fault, thereby facilitating slip. Consequently, we might expect slip-partitioned fault systems to persist as long as the oblique convergent loading, general fault configuration, and fault strength do not change.

Convergent margins may develop slip partitioning because they either develop new strike-slip faults or reactivate existing weaknesses so that they accrue strike-slip. Reactivation of existing weaknesses may facilitate the development of slip partitioning at higher convergence angles than otherwise permitted (e.g., Chemenda et al., 2000; Haq and Davis, 2010). Slip partitioning at margins with high-convergence angles may also be facilitated by magmatic weakening of the overriding plate. Weakening of the crust through magmatic intrusion may localize strain that initiates large, throughgoing strike-slip faults and facilitates slip partitioning (De Saint Blanquat et al., 1998). The findings from the scaled experiments of this study demonstrate that the presence of a weakness can facilitate slip partitioning at lower total strain than a more homogeneous strength experiment.

While magmatic weakening may facilitate strike-slip faulting, the initiation of strike-slip faults within convergent margins may also facilitate magmatism. The scaled experiments of this study show the initiation of strike-slip faults via coalescence of opening cracks that strike oblique to the margin. These segmented opening-mode cracks have similar geometric relationships with the convergent margin as volcanic fissures in the southern Andes of Chile (e.g., Lara et al., 2006; Cembrano and Lara, 2009). These fissures provide magma migration pathways that may thermally weaken the crust and promote the development of strike-slip faults. Furthermore, slip along reverse faults can invoke extension in the hanging wall, which promotes development of volcanic fissures. Volcanism increased in some fissures after the 1960 Chile earthquake due to temporal changes in the local stress field (Lara et al., 2004). Consequently, magmatism in oblique convergent margins can lead to a positive feedback loop—where convergence enhances magmatism that weakens the crust, enabling strike-slip fault development that provides conduits for magmatism (e.g., De Saint Blanquat et al., 1998). One result of this feedback can be sustained slip partitioning of fault systems within oblique-convergent margins.

6. CONCLUSIONS

The scaled experiments of oblique convergence over a basal dislocation exhibit slip partitioning along the entire margin; this laboratory-scale slip partitioning resembles slip-partitioned crustal systems regardless of whether the experiments have a precut vertical weakness or not. The experiments reveal three styles of slip-partitioning evolution delineated by the order of faulting and extent of slip partitioning. The first style observed in the low-convergent angle experiments (5°) grows strike-slip faults prior to reverse faulting along the entire oblique-convergent margin. The second style develops in all precut experiments with >5° convergence and uncut experiments with >15° convergence. In these experiments, the primarily reverse fault forms first, and slip partitioning of the entire convergent margin develops with the development of strike-slip either along the precut fault or as a new strike-slip fault from linkage of echelon extensional features. The uncut experiments also show a third style of local slip partitioning, where two generations of reverse faults are simultaneously active for a period of time in one region of the experiment.

Scaled oblique-convergence experiments in wet kaolin that simulate crustal materials develop a slip-partitioned fault system rather than developing a single oblique-slip active fault structure in order to accommodate oblique convergence. The development of two active fault surfaces, which consume greater work, arises due to the changes in the local stress state after development of the first fault. In systems that grow early, steeply dipping, strike-slip faults, off-fault contraction accumulates until a new reverse fault grows. In systems that grow early reverse faults, the lobate nature of these faults limits accommodation of strike-slip, which increases distributed shear strain. Furthermore, reverse-slip on the fault produces local extension in its hanging wall. Both of these mechanisms promote development of new strike-slip faults in the hanging wall of the reverse fault.

The emergence of fault-slip partitioning within the scaled experiments provides insight into the development of such fault systems at crustal margins. Transform margins that begin to accommodate convergence may develop a system of reverse faults, and convergent margins that begin to accommodate oblique plate motion may develop new strike-slip faults or activate inboard crustal weakness to accommodate strike-slip. Once the fault system is slip partitioned along a substantial portion of the oblique-convergent margin, this active fault configuration will persist. The observation of slip partitioning under a wide range of experimental conditions and materials in this study and others demonstrates how such systems are frequently observed at oblique-convergent margins around the world.

7. DATA MANAGEMENT

The experimental DIC data files and complete animations are available on European Plate Observing System (EPOS) repository for analog modeling of geologic processes hosted by GFZ Potsdam (Cooke et al., 2019). Animations of strain and uplift are available on the UMass Geomechanics YouTube channel transpression play list (https://tinyurl.com/y6fhkxeh).

ACKNOWLEDGMENTS

This work was funded by National Science Foundation grant EAR 1550133. MLC thanks David Bowman and Karen Leever for inspirational discussions on slip-partitioned fault systems. The authors thank Clare Bond and two anonymous reviewers for comments that improved the paper.

1Supplemental Materials. Strain animations from experiments not presented in the main text. Text describes uplift patterns obtained from stereovision technique for 5°, 10°, 15° and 20° oblique convergence experiments. Please visit https://doi.org/10.1130/GES02179.S1 or access the full-text article on www.gsapubs.org to view the Supplemental Animations.
Science Editor: David E. Fastovsky
Associate Editor: Clare E. Bond
Gold Open Access: This paper is published under the terms of the CC-BY-NC license.

Supplementary data