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Caribbean Plate Boundaries Control on the Tectonic Duality in the Back‐Arc of the Lesser Antilles Subduction Zone During the Eocene

The Eocene tectonic evolution of the easternmost Caribbean Plate (CP) boundary, that is the Lesser Antilles subduction zone (LASZ), is debated. Recents works shed light on a peculiar period of tectonic duality in the arc/back‐arc regions. A compressional‐to‐transpressional regime occurred in the north, while rifting and seafloor spreading occurred in Grenada basin to the south. The mechanism for this strong spatial variation and its evolution through time has yet to be established. Here, using 3‐D subduction mechanical models, we evaluate whether the change in the trench‐curvature radius at the northeast corner of the CP could have modulated the duality. We assume asymmetrical CP boundaries at the north (from east to west: oblique subduction to strike‐slip) and at the south (subduction‐transform edge propagator‐like behavior). Regardless of the imposed trench curvature, the southern half of our modeled CP undergoes a NW‐to‐W‐oriented extension due to the tendency of the southernmost part of the South‐America oceanic slab to rollback. In contrast, the tectonic regime in the northeast corner of the CP depends on the trench‐curvature radius. A low radius promotes transtension‐to‐transpression, with a NE‐oriented compressive component of the principal stress. A high radius largely reduces the compressive component and promotes an extensional regime similar to that in the south. We thus propose that an initially low‐curvature radius of the NE‐LASZ triggered the tectonic N‐S duality in the Eocene and led to an ephemeral period of transpression/compression at the north. However, an additional mechanism might have been required to locally enhance compression.

Eocene, respectively (Bouysse, 1988;Garrocq et al., 2021). Thus, we postulate that these regional deformation patterns were induced by a compressional tectonic regime in the Northern Lesser Antilles and an extensional regime in the Southern Lesser Antilles. Hereafter, we refer to this peculiar regional stress field to as the Eocene-tectonic duality of the LASZ. This episode of latitudinal variation ended in the late Eocene and may have coincided with or preceded trench bending at the northern LASZ.
The present contribution aims to decipher whether the evolution of the trench curvature during the Eocene, along with a northern subduction-to-strike-slip boundary and a southern free subduction boundary (STEP fault), could have provoked a spatio-temporal strong variation in the state of stress from north to south at the easternmost Caribbean plate (Figure 1b).
The three-dimensional shape of the subduction trench and the convergence obliquity was shown to impact the stress field at the surface of the overriding plate (Bonnardot, Hassani, Tric, Ruellan, & Régnier, 2008). These authors showed that symmetric sea-wards (subducting-plate-wards) concave and convex margins lead to trench-parallel tension and compression, respectively, in the forearc/arc area near the apex of the curvature. That is because the direction of non-hydrostatic forces at the subduction interface either diverge from or converge to that area of the forearc in concave and convex settings, respectively. Furthermore, shear stresses along the subduction interface induce shear parallel to the trench in the forearc region where the convergence is the most oblique, for instance at both sides of a symmetrical curved margin (Boutelier & Oncken, 2010). Obliquity can further lead to strain partitioning and to localization of shear in pre-weakened areas such as the arc region (Chemenda et al., 2000). In nature, these 3-d effects may have affected regions of arcuate subduction trenches such as the Bolivian orocline (Boutelier & Oncken, 2010) or the western Aleutians (Ryan & Scholl, 1989). In the Northern Lesser Antilles, Paleogene V-shaped basins in the forearc may have resulted from the bending of the trench and from the development of a convex subduction setting which could have favored regional-scale block rotations (Boucard et al., 2021;Laurencin et al., 2017). The basins developed under the influence of a strong convergence obliquity along a highly curved trench which promoted trench-parallel forearc extension since at least the end of the Oligocene (e.g., Boucard et al., 2021;Feuillet et al., 2002). It is plausible that a temporal variation in trench curvature and subsequent convergence obliquity during the Eocene affected the spatio-temporal evolution of the stress field in the arc/backarc region of the LASZ, but such an impact remains yet to be quantified.
Here, by using three-dimensional mechanical subduction models, we show that a low trench-curvature radius could have promoted a tectonic duality in the LASZ from early to mid-Eocene, favoring a transpressive event in the northern arc/back-arc area. An increasing curvature radius from the middle-to-late Eocene may have assisted a relief of compressive stresses in the same region. Below, we first describe the geodynamical setting of the LASZ during the Paleogene, focusing on Eocene times. Then, we describe the numerical approach that we undertake before presenting our modeling results and their implication for the regional tectonic evolution.

Tectonic Setting
The integrated story of the Caribbean plate and associated subduction zones has been described in various tectonic reconstructions (e.g., Boschman et al., 2014;James, 2009;Meschede & Frisch, 1998;Pindell & Kennan, 2009). The onset of westward subduction at the north-eastern boundary of the Caribbean plate occurred in the Cretaceous, probably not later than 90 Ma (Mann, 2007;Pindell & Kennan, 2009). Until the late Paleocene, the Caribbean plate hosted a volcanic arc which spanned the width of the plate, called the Great Arc of the Caribbean (GAC; Burke et al., 1978). This former arc was associated with the SW-dipping subduction of a proto-Caribbean seafloor and was contemporaneous of a NE-SW relative convergence between the Caribbean plate and the Americas. From the end of the Paleocene to the early Eocene, the volcanic activity of the GAC ceased (Figure 2a). At the easternmost part of the Caribbean plate, corresponding to the LASZ at present-day, the volcanic front migrated eastwards from the Aves ridge to the Lesser Antilles arc between the early and the middle Eocene (Figure 2b). The relative convergence between the Caribbean and the American plates switched to E-W. This plate reorganization was accompanied by major tectonic events in Paleocene and Eocene times, which we highlight below. Our brief description follows a geographic path from North to South. From the Paleocene to the early Eocene, the northern segment of the GAC, presently corresponding to western and central Cuba, collided with the buoyant Bahamas platform and led to the formation of an orogenic belt (Cruz-Orosa et al., 2012;Garcia-Casco et al., 2008;Iturralde-Vinent, 1994; Figure 2a). Thrusting of the Cuban terranes onto the Bahamas platform was achieved by early middle-Eocene and led to the formation of the Cuban suture zone (Bralower & Iturralde-Vinent, 1997;Stanek et al., 2009). During the frontal arc-Bahamas collision, the direction of shortening in Central Cuba was reported to pass from a SSW-NNE orientation before the early Eocene, to a SW-NE orientation in middle-Eocene and to WSW-ENE after Mid-Eocene (Cruz-Orosa et al., 2012), which may illustrate a possible tectonic reorganization during the early Eocene.
The collision ultimately caused the jump of the Caribbean-North America plate boundary toward an E-W transform system south of Cuba ( Figure 2a). South of the Sierra Maestra, the strike-slip motion was accommodated by the opening of the Cayman Through from ∼50 to 49 Ma Rosencrantz et al., 1988). Prior to the spreading, a period of rifting (pull apart basin) may have started as early as the late Paleocene (Pubellier et al., 2000). Rosencrantz (1990) proposed that the E-W strike-slip motion between the plates was coeval with the thrusting of Cuba onto the Bahamas platform, and thus may have started as early as the late Paleocene-early Eocene. As shown below, this is consistent with the geological record in Figure 2. Illustrative cartoon of the evolution of the tectonic setting of the Caribbean. The stages at the late Paleocene and Mid-Eocene are modified from Pindell and Kennan (2009). We have also sketched a possible extension of the Bahamas platform following for example, Laó-Dávila, 2014. The stage at the late Eocene is modified from the Mid-Eocene reconstruction in Pindell & Kennan, 2009 by adding an assumption on the southern trench evolution following spreading in the Grenada basin. 10.1029/2021TC006885

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Hispaniola which does not display substantial compressive tectonics at that time, as it would be expected given the reconstructed position of the island facing a possible thrust of the SE end of the Bahamas platform ( Figure 2b).
Hispaniola records some pieces of evidence of compressive tectonics in the Eocene but most of the contractional structures (folds and thrusts) formed after the middle-Eocene (Heubeck et al., 1991;Huerta & Pérez-Estaun, 2002;Pubellier et al., 2000). Furthermore, recent geophysical imaging of the crust in western Hispaniola only suggests modest shortening (post-Cretaceous and pre-Neogene) across the Trans-Haitian belt (Corbeau et al., 2017). The lack of evidence of a major compressive event in Hispaniola during the Eocene may indicate that the collision with the Bahamas platform, if it occurred at that time, played only a minor effect on the regional tectonics or that it was mostly accommodated by a sinistral strike-slip motion. Our model setup below is based on such an assumption that the northernmost segment of the Caribbean plate was not a collisional front anymore by the early Eocene and was instead an oblique subduction-to-transform plate boundary, similar to the present-day configuration (Rodriguez-Zurrunero et al., 2020).
The position of Puerto Rico relative to Hispaniola was south or southeast in the early to mid-Eocene (Jolly et al., 2007;Pindell & Kennan, 2009). A volcanic activity of Eocene age with a geochemical signature of extensional tectonics has been reported in the southeast of Puerto Rico (Schellekens, 1991). In the northeastern part of the island, a volcanic activity is recorded up to the mid-Eocene (Jolly et al., 2007). Several lines of evidence support a transpressional (NE-SW) tectonic regime there across the Eocene (Figure 1b). This regime mainly affected the Southern Puerto Rico Fault Zone and the Northern Puerto Rico Fault Zone which accommodated the transpression by fold-and-thrusts belts and conjugate sinistral strike-slip faults (Laó-Dávila, 2014;Lao-Davila et al., 2012). The transpressional regime was active from the middle-Eocene to the early Oligocene, although it may have started before (Laó-Dávila, 2014;Roman et al., 2020). Furthermore, this regime may have been accommodated in the proxymal back arc through the formation of the east-west trending Muertos Trough and the overriding Muertos fold-and-thrust belt (Granja- Buña et al., 2009Buña et al., , 2014 which extends from southeast of Puerto Rico to the south of Central Hispaniola. Note that a period of contraction of Paleogene age was also reported in the Virgin Islands (St Croix; Speed, 1989).
Further east (or southeast), in the vicinity of the Saba bank, combined onshore and offshore geological and geophysical analysis revealed a period of compressional regime which inverted pre-mid-Eocene normal faults offshore in the region of the Saba Bank and lead to a top-to-the-W thrusting on the island of St Barthélemy dated between at least ∼42.5 Ma and up to ∼39.7 Ma . Put together, the above observations suggest a period of compressional and/or transpressional tectonic regime during at least part of the Eocene which affected a relatively large area of the arc/back-arc regions of the northeastern corner of the Caribbean plate (red domain, Figure 2b).
In the central and southern part of the LASZ, the GAC occupied the present-day Aves Ridge bathymetric feature and was active until c.a. 59 Ma (Fox et al., 1971;Neill et al., 2011;Wright & Wyld, 2011). The opening of the Grenada basin in the southern half of the plate was contemporaneous or followed an east-wards arc migration (Allen et al., 2019;Bouysse, 1988;Garrocq et al., 2021;Pindell & Barrett, 1990). Garrocq et al., (2021) has proposed a three-stage shaping of the basin, including a NNW-SSE stretching episode during the late Paleocene-early Eocene, followed by a NW-SE oceanic spreading of at least 100 km which ended in the late-middle Eocene (Figure 1c).
Based on the recent evidence on both the compressional regime at the NE corner of the Caribbean plate and the extensional regime in the region corresponding to the Grenada basin, the North-South tectonic duality of the LASZ lasted from the early Eocene to the late Eocene, thus for a duration of 10-20 Myr.
From the early Paleocene onwards, the southern boundary of the Caribbean plate was mainly characterized by an oblique arc-continent collision between the extinct southern-end of the GAC and South America (Pindell & Barrett, 1990;Wright & Wyld, 2011). From the Paleocene to the early middle Eocene, the Leeward Antilles collided obliquely with the northern Colombian margin northwest of the Maracaibo basin Montes et al., 2019). Behind the collision front, a dextral strike-slip system to the north of the colliding extinct arc accommodated the regional transpressional regime (Beardsley & Avé Lallemant, 2007). A net strike-slip motion involving the Oca -San Sebastian -El Pilar fault system as a part of a STEP fault may have only started in the late Eocene-early Oligocene . However, in our modeling approach, we make the case that a STEP fault-like boundary existed at the southern boundary of the Caribbean plate from the early Eocene, in consistence with the mid-Eocene reconstruction of Pindell and Kennan (2009) (Figure 2b).

Modeling Approach
To gain insights into the tectonic evolution of the LASZ during the Eocene, we perform mechanical models of subduction using the three-dimensional version of the code ADELI (Hassani et al., 1997) which is suitable for studying the effect of the trench curvature on the state of stresses within the overriding plate (see e.g., . In our approach (see governing equations in the Supporting Information S1), the lithospheric plates are viscoelastic solids and the mantle is treated as an inviscid fluid (Buiter et al., 2001;Gibert et al., 2012;Hassani et al., 1997) Models of subduction dynamics showed that an inviscid mantle produces results comparable to those that would be obtained with a mantle of low viscous resistance (viscosity lower than 10 20 Pa s), if the plates were sufficiently strong (viscosity ratios of about 10 4 ; Cerpa et al., 2014). Furthermore, as described below, the magnitudes of plate velocities at the LASZ are relatively low, and thus we postulate that mantle drag should be moderate, at least in the shallow upper mantle. Nonetheless, mantle viscous forces may deviate the dynamics from that observed in our models and we discuss in Section 5 this limitation of our modeling approach.
Our models consist of two 80-km thick homogeneous lithospheric plates initially separated by a planar fault ( Figure 3). The viscosity of the plates is 10 24 Pa s and their density exceeds that of the mantle by 50 kg m −3 . Therefore, the subducting plate has roughly the average characteristics of a 70-Ma old lithosphere, consistent with the reconstruction shown in Braszus et al. (2021) which suggest a subducted oceanic lithosphere of age between 50 and 100 My. The friction at the contact fault is set to a relatively low value of 0.01, consistently with previous modeling studies who found that the shear strength at the plate interface is relatively low (Behr & Becker, 2018;Crameri & Tackley, 2015;Duarte et al., 2015). The Young modulus and Poisson's ratio are set to average values for the lithosphere (Turcotte & Schubert, 2002), that is, 10 11 Pa and 0.25, respectively. conditions. An idealized north (N*) points in the same direction as the y-axis. Note that the southern boundary condition of the subducting plate is set to free-slip until it enters the subduction trench, after what we apply only a lithostatic pressure to simulate a STEP-like plate boundary. The inset depicts a 3-d view of the subducting plate to show the transitional plate boundary. The northern (TPN) and the southern (TPS) tracking points are used to track the evolution of the principal stresses in the idealized arc to back-arc regions.

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The overriding plate (Caribbean Plate [CP]) is 900-km wide, which approximately corresponds to the present-day width. It is fixed at its trailing edge given that the CP has been roughly immobile in an absolute reference since at least 50 Ma (Boschman et al., 2014). The velocity of the 1,650-km wide (2,400-km long) subducting plate (American plate [AP]) is imposed at its trailing edge ( Figure 3). The latter assumption is based on the fact that the motion of the Americas was probably controlled by the eastward-dipping subduction zones occurring at their western boundary since at least the Cretaceous (Ramos, 2009;Sigloch & Mihalynuk, 2013) and perhaps by a large-scale mantle circulation (e.g., Faccenna et al., 2017), which must thus have controlled the velocity of the subducting plate in the LASZ. We impose the present-day value (2 cm/yr) to the velocity of the AP, and thus neglect the potential transient effects induced by variations in kinematics (Cerpa & Arcay, 2020;Cerpa et al., 2018;Guillaume et al., 2018). The far-field kinematic boundary conditions on the plates are held from the start to the end of the models. The lateral edges of the AP are free to slip. Note that the southernmost lateral edge of the AP is let free when it plunges into the inviscid mantle, approximating a STEP fault.
The initial in-plane radius of curvature of the NE trench is set a value E R (Figure 3). This is one of the most important parameters of our models. However, it is little constrained at Eocene times. We hypothesize that an increase in trench-curvature radius is a plausible scenario after the jump of the Caribbean-North America plate boundary (Early Eocene, Figure 2a). After the jump, the new plate boundary system was indeed partly created by a cut in the former CP in the form of a transform fault that linked the Cayman rift/ spreading axis to the eastern subduction trench (Boucard et al., 2021;Pindell & Barrett, 1990). By that time, the latter plate boundary may have been more rectilinear than at present-day ( Figure 2). We nonetheless acknowledge that the reported evidence of trench bending at the NE corner of the Caribbean plate pointed out a post-late Eocene deformation. This includes a post-Eocene 45° counter-clockwise rotation of Puerto Rico (van Fossen et al., 1989), and a post-Oligocene 15-20° counter-clockwise rotation of the St Barthelemy island  associated with a more pervasive deeply rooting NE-SW fracturing, which fragmented the arc-forearc into a set of shallow spurs and deep valleys (Boucard et al., 2021;Laurencin, et al., 2017). Yet, it remains uncertain whether the bending of the trench was accommodated through block rotations or, instead, by a more diffuse deformational pattern, especially in regions weakened by active arc volcanism (Saba Bank, Puerto-Rico). In what follows, we explore two end-members for the trench-curvature in the models: a relatively low radius of 200 km and a relatively high radius of 600 km which is equivalent to the present-day apparent curvature of the LASZ ( Figure 1a).
Initially, the westward termination of the subduction plane (30° dip), that is the termination of the curved trench, is at a distance L trans from the eastward termination of the vertical (90° dip) transform fault (Figure 3 inset). In between these two points the dip-angle of the contact fault between the two plates increases westwards. This transitional interplate plane is hereafter referred to as the transitional plate boundary. Note that during the evolution of the model, the transitional plate boundary tends to extend westwards owing to the displacement of the westernmost termination of the vertical fault on the subducting plate side, while the easternmost termination of the transitional plate boundary on the overriding plate side tends to be stationary. As seen below, such a displacement as well as the imposed initial value of L trans can affect the modeled state of stress, mostly in the interior of the overriding plate. Since the value of L trans in nature cannot be constrained otherwise than qualitatively, we explore several values.
Finally, the tectonic duality in the Eocene is mostly inferred from tectono-sedimentary observations at the surface of the LASZ, mainly located in the arc and back-arc regions. We thus focus on the modeled deviatoric stress field at the surface of the CP in regions situated at a distance of 150-400 km from the trench and that we refer to as the idealized arc/(proximal) back-arc regions. Note that more distal regions away from the trench are referred to as intraplate regions. In particular, for describing the arc/back-arc stress field, we define two points ( Figure 3): the Tracking Point at North (TPN) and at South (TPS) which are initially at a distance of 200 km from the north and south CP boundary, respectively, and at a distance of 300 km from the eastern trench. For simplicity, we hereafter refer the deviatoric stresses to as the stresses.

Reference Model
We first consider a reference model where the trench-curvature radius is relatively low Figure 4). The length of the transitional plate boundary is L trans = 700 km. All models are characterized by an initiation stage where the convergence generates compression of the overriding plate (subduction initiation). Sufficiently after the subduction-initiation stage (i.e. at t ∼ 18 Myr), the subducting plate sinking into the mantle is well developed, yet with some variation along the margin. At south, a "classical" subduction occurs, where the trench-normal convergence increases the length of the subducting slab with time. At the NE corner of the overriding plate, the convergence partitions between a sinking of the slab into the mantle and an E-W displacement of AP relative to CP. West of the transitional plate boundary, the relative motion between the two plates is purely strike-slip. As aforementioned, the westward termination of the transitional plate boundary moves westwards on the subducting plate side. Thus, the apparent length of the transitional plate boundary tends to increase with time.
At the model-time of  21 E t Myr (Figure 4a), the tip of the subducting slab in the southernmost part of the model reaches a depth of 430 km. The length of the slab in the southern part is sufficiently long (i.e., the slab . The gray colorscale gives the second invariant of deviatoric stresses (J2) at the surface of the overriding plate using a top view. The lines give the direction of the in-plane principal deviatoric stresses (i.e., eigenvalues of the deviatoric stress tensor or the maximum and minimum value of normal stresses) at the surface of the overriding plate, the intensity of which is given by both the red-to-blue colorscale and the segment length. Negative (redish) values are for compression and positive (bluish) values are for extension. Note that we only represent the principal stresses at distances of more than 100 km from the interplate boundary as we focus on the tectonic evolution of the ideal arc/back-arc region. The green and yellow rectangles above the panels indicate the horizontal extent (each rectangle has a length trans E L ) of the geometric transitional plate boundary on both the subducting and the overriding plate sides, respectively. On the 3-d perspective view, we display depth contours every 100 km at the surface of the subducting plate. (c) Evolution of the magnitude of the principal stresses at the two representative locations of the overriding plate tectonic regime: Tracking Point at North (TPN) in cyan and Tracking Point at South (TPS) in magenta. The point locations are also reported in the top view of the overriding plate.
pull is sufficiently high) to generate a quasi-trench normal traction on the overriding plate. We hereafter refer this force to as the trench-normal traction. The traction occurs because the slab-pull force is transmitted to the overriding plate as non-lithostatic forces acting on the subduction interface. The resulting extension at the surface of the overriding plate is illustrated by the principal stresses in regions lying at distances of more than 200 km and less than 500 km from the trench. There, we observe a tensile principal stress that is oriented NNW-SSE to NW-SE and rotates to W-E along the southern-free slip boundary. Thus, this principal stress is oriented toward the southernmost part of the subduction trench where the trench-normal traction is the highest. The magnitude of the tensile principal stress is about 100-150 MPa at a distance of 200-400 km away from the trench (idealized arc/back-arc region) as illustrated at the southern-tracking point (TPS in Figure 4c). It reaches locally 200 MPa close to the southern boundary. Note that a compressive principal stress, with a relatively low magnitude (∼50 MPa, Figures 4c), is also observed in this southern-half of the CP. The magnitude of the second invariant of the stresses (J2∼300 MPa) along the southern boundary is controlled by both the trench-normal traction and the out-of-plane stress induced by flexure of the CP. At this stage, the tensile principal stresses in the southern back-arc area cause only moderate values of the second invariant of the deviatoric strain ( II E e <0.05), hereafter referred to as the strain, and a negligible trench retreat (see Figure S1a,b in Supporting Information S1).
Near the NE corner of the CP, we observe a region of relatively high in-plane stresses (J2 > 300 MPa). The high-stresses are located near the trench but reach locations as far as 300 km away from the interplate boundary, coinciding thus with the vicinity of the center of the curved margin. In this region, we observe principal stresses with both a NNW-SSE tensile component and an approximately WSW-ENE compressive component. The highest magnitudes of strain ( II E e ∼ 0.15) are reached in the NE corner (see Figure S1a in Supporting Information S1). There, some upper plate shortening occurs and leads to a slight trench advance (see Figure S1b in Supporting Information S1). At the TPN, the tensile and compressive principal stresses have magnitudes of 210 and 205 MPa (Figure 4c) and highlight a quasi-transpressional regime in the NE corner. Moreover, this high-sheared region overlaps another patch of moderate shear (J2 ∼ 200 MPa) situated along the trench at a horizontal position x  E −200 km. The latter patch of shear is induced by the indentation effect of the transitional plate boundary, as described below.
Finally, far away from the eastern subduction trench (distance of more than about 1,000 km), the stresses at the surface of the southern half of the overriding plate are relatively low (J2 < 150 MPa) and the W-E subduction-induced tensile principal stress vanishes. Instead, a modest N-S tensile principal stress (magnitude of ∼120 MPa) occurs in direction of the transform fault, and causes moderate values of strain ( II E e up to 0.10, see Figure S1a in Supporting Information S1).
Myr (Figure 4b), the southernmost slab tip has reached a 690-km depth. Because of the important trench-normal traction, the tensile principal stresses reach 200-250 MPa in the southern half of the arc to distal back-arc region at distances from the trench of 300-500 km. The point TPS displays a tensile principal stress of 206 MPa (Figure 4c). In the latter region, the strain now reaches moderate magnitudes of ∼0.05-0.07, and trench retreat at a rate of 0.2-0.3 cm/yr (Figure S1c and S1d in Supporting Information S1). As in the previous stage of the model, a patch of moderate-to-high stresses (J2 = 250-350 MPa) is observed in the vicinity of the center of the curved margin, that is in the arc/back-arc region of the NE corner of the CP. There, we observe that the NNW-oriented tensile and the ENE-oriented compressive principal stresses display magnitudes of 150-200 and 150-180 MPa, respectively. The tracking point TPN exhibits tensile and compressive components with magnitudes of 192 and 146 MPa, respectively. In the NE-corner, the ratio of compressive-to-tensile principal stresses is 76% and denotes a transtensional regime.
At the northwest of the TPN a patch of very high stresses is visible close to the transitional plate boundary along the subducting plate side which now lies between   550 E x km and  200 E x km. The stresses are particularly high (J2 > 400 MPa) near the eastern end of the transitional plate boundary on the subducting plate side which is impeded to subduct and creates a local indenter acting on the subduction interface. These very high stresses remain nonetheless in a region situated at a distance of less 150 km away from the interplate boundary. Furthermore, the indentation effect of the transitional plate boundary generates some compressive principal stresses (magnitude 50-70 MPa) oriented N-S to NNE-SSW in the back-arc to intraplate regions relative to the northern transitional plate boundary (area in the ranges   To sum up, at the mature stage of the reference model, four areas of varying tectonic regimes can be distinguished at the surface of the overriding plate: 1. A southern arc/back-arc region where the trench-normal traction induces WNW-oriented to NNW-oriented tensile principal stresses. 2. A NE corner undergoing high stresses. This area displays a transpressive to transtensional regime that is due to the curved margin, the obliquity of subduction and the limited slab length. Note that this area undergoes a WSW-ENE-oriented compressive principal stress. 3. A back-arc to intraplate region in front of the transitional plate boundary that undergoes compressive principal stresses oriented N-S to NNE-SSW which are due to the indentation effect of the transitional plate boundary. 4. Distal intraplate regions where the stresses vanish and undergo only a small N-S oriented tensile principal stress.

Model With a Higher Trench-Curvature Radius
We now consider a model with a higher trench-curvature radius (  600 E R km, Figure 5), equivalent to that of the present-day LASZ (Figure 1a). The transitional plate boundary initially spans the spatial range    400 300 E x km, and thus has the same length as that in the reference model. At  21 E t Myr (Figure 5a), at south, the trench-normal traction generates a prominent (magnitude higher than 100 MPa) NW-oriented to E-oriented tensile principal stress in the arc/back-arc region in the southern half of the CP. For instance, the point TPS display an tensile principal stress of 140 MPa. Unlike the reference model, the second invariant of the stress do not show a substantial increase in magnitude as we approach the NE corner, and the principal stress display a little compressive component. At the point TPN the tensile and compressive components of the principal stress are 105 and 25 MPa, respectively. The region of the overriding plate that overlies the transitional plate boundary undergoes high-shear stress, especially in the vicinity of its eastern-end. Yet, the high-stress region remains within a short distance to the interplate boundary (<150 km).

At the model time
Myr, the southernmost tip of the subducting plate reaches a depth of ∼690 km. The southern long trench-normal traction exerts a relatively strong tension on the overriding plate in the arc/back-arc region both in the north and in the south, as shown by the tensile principal stress (magnitude >100 MPa). Unlike the reference model, only modest stresses are observed at distances of more than 150 km from the trench in the NE corner of the CP. For instance, the point TPN displays a compressive component of 40 MPa, thus about 3 times lower that that observed in the reference model. The tensile principal stress is moderately high at the same location, displaying a value of 105 MPa, thus only two times lower than that observed in the reference model. The ratio of compressive-to-tensile principal stresses in the N-E corner is ∼40% (in the reference model at the same stage the ratio is 76%), and highlights a transtensional regime.
It is important to note that in the model with  600 E R km, we do not observe substantial a compressive principal stress in the idealized arc/back-arc region of the NE corner. That is because, in the high-E R model, the non-hydrostatic forces acting on the curved subduction interface converge toward a larger area compared to that in the reference model, thereby reducing the trench-normal compressive component of the principal stresses. More generally, the maximum non-hydrostatic forces acting on the overriding plate of a convex-shaped margin are inversely proportional to the trench-curvature radius, as described by Bonnardot, Hassani, Tric, Ruellan, and Régnier (2008). In contrast, the magnitude of the tensile principal stress is controlled by the length of the southernmost subducting slab, and that is why we do not observe substantial differences between this model and the reference model.
Further north(west), the only patches of very high shear stresses are restricted to a proximal region of the transitional plate boundary. As in the reference model, this part of the interplate boundary locally indents the overriding plate, creating a NNE-oriented compressive principal stress. Yet, the latter reaches only a smaller area in the intraplate domain (in the ranges    [ 500; 100] E x km and  [400;700] E y km) than in the reference model.
To summarize the mature stage (t = 33.3 Myr) of the model with  600 E R km, we identify four distinct tectonic areas at the surface of the overriding plate: 1. A southern arc/back-arc region where the trench-normal traction induces WNW-oriented to NNW-oriented tensile principal stress. 2. A NE arc/back-arc region under a transtensional/extensional regime with a tensile principal stress roughly oriented as that in the southern part. Note that the second invariant of stresses display only a moderate increase when approaching the NE corner, unlike the reference model. 3. A back arc to intraplate regions in the northern half of the plate which undergo tensile principal stresses oriented toward the eastern trench and some compressive principal stresses normal to the transitional plate boundary. 4. Distal intraplate regions where the stresses vanish and undergo only a small N-S oriented tensile principal stress.
Three of these domains are very similar to the ones simulated with a lower radius of trench-curvature (R = 200 km), that is, areas 1, 3, and 4. The area 2 strongly differs from its equivalent obtained in the reference model with R = 200 km, where the ratio of compressive-to-tensile principal stress is about two times higher, and denotes a regime that tends to be transpressional.

Model With a Weaker Overriding Plate
We emphasize that in our modeled subduction setting, the trench-curvature radius plays an important role in the distribution of stresses at the surface of the OP. However, because in the two models presented above, the plates are relatively strong (  24 10 E Pa s), the radius little evolves through time. We now run a model with the same initial radius of trench-curvature as in the reference model (  200 E R km) but with a weaker overriding plate (viscosity of  23 3 10 E Pa s) to increase the trench ability to bend. The overall evolution of the model with a weaker overriding plate is close to the one simulated in the reference model, except that because of its relative weakness the plate undergoes more deformation.
The compression occurring at the initial stages of subduction generates a greater shortening than in the reference model and is roughly homogeneous from North to South. At a mature stage of subduction, i.e. at  29.2 E t Myr (Figure 6a), the southernmost slab tip reaches a depth of ∼460 km. The slab rollback induces a NNW-oriented to W-oriented tensile principal stress in the southern arc/back-arc region, as in the reference model at an equivalent stage (see Figure 4a). The magnitude of the highest tensile principal stress is nonetheless lower than simulated in the reference model. For instance, the tensile principal stress is 64 MPa at the TPS, whereas it reaches up to 200 MPa in the reference model at a similar location. Such an extensional regime generates some trench retreat but at a small rate (∼0.1 cm/yr, see Fig. S2b in Supporting Information S1). Alike the reference model, a combination of in-plane extension and compression occurs near the NE-corner of the CP. The TPN displays magnitudes of the compressive and tensile principal stresses of 70 and 85 MPa, respectively, and thus denotes a quasi-transpressional regime. More generally, in the idealized arc/back-arc area of the NE-corner, the orientation of the compressive component of the principal stresses is E-W to ENE-WSW and its magnitude is up to 150 MPa at distance of more than 150 away from the trench. The stress field in the NE corner cause principally a E-W to ENE-WSW shortening as highlighted by the relatively high values of strain ( II E e < 0.25) and a trench westward motion at ∼0.4 cm/yr (FigS2a,b in Supporting Information S1).
At the end of the model time (  40.5 E t Myr, Figure 6b), the southern tip of the subducting slab reaches a depth of 690 km. The prominent extensional regime in the south causes important E-W stretching. This is specially illustrated by the higher values of strain achieved in the southern arc/back-arc area ( II E e < 0.10-0.15) and the southern trench retreat at a rate of ∼0.8 cm/yr (at least twice that in the reference model) at  40.5 E t Myr (see Fig. S2c and S2d in Supporting Information S1). More generally, in the model with a weaker plate, the apparent radius of trench-curvature tends to increase with time since the northernmost experiences a slightly higher E-W shortening relative to that in the reference model at the first mature stages of subduction (  E t 20-25 Myr). At later mature stages of subduction (  25 E t Myr), it is the southernmost part of the CP which undergoes more E-W stretching than that in the reference model.
Interestingly, we observe some decrease through time in the compressive principal stress while the tensile principal stress builds up (see e.g., Figure 6c). The latter occurs since both the southern trench-normal traction and the apparent trench-curvature both increase. At the TPS, the tensile and compressive principal stresses are 165 and 18 MPa respectively at  E t 40.5 Myr. At the TPN, these are 135 and 80 MPa with a ratio of compressive-to-tensile principal stresses of ∼60%. The latter value is thus intermediate between that observed in the reference model (∼80%) and that in the model with a higher trench-curvature radius (∼40%) for equivalent locations and at a similar stage of maturity of the subduction model.
We speculate that further trench unbending could reduce the compressive component of the principal stresses at north, and thus establish a strong transpressional regime self-consistently. However, we cannot consider models with a very weak OP (viscosity  23 10 E Pa) because a too large deformation of the mesh cannot be handled without an appropriate remeshing technique which, in turn, might propagate numerical errors.
Furthermore, in nature, the southern E-W stretching may have induced oceanic spreading (e.g., Garrocq et al., 2021) which, in turn, may have also impacted the evolution of the apparent trench curvature. This effect is however not included in our models.

Models With Various Initial Lengths of the Transitional Plate Boundary
We have highlighted the effect of the transitional plate boundary on the state of stresses close to the boundary as well as in the intraplate domain. Because there is no accurate constraint on its length in nature for the Eocene, and because it might have changed through time, here, we explore models with different lengths. The two models exhibit moderate (J2 > 200 MPa) to very high stresses (J2 > 400 MPa) along the transitional plate boundary. In particular, a patch of very high stresses is always located either close or east of the eastern-end of the transitional plate boundary (see green rectangles in Figures 7a and 7c) but remains within a distances shorter than 100 km from this boundary. This high-stress area has a little influence on the tectonic regime in the NE corner which is controlled by the trench-curvature radius.
The major effect of changing the length of the transitional plate boundary is on the stress field in the back-arc to intraplate regions. The smallest value of trans E L induces a N-S to NE-SW oriented compressive component of the principal stresses with a moderate-to-high magnitude (80-120 MPa) in this area (roughly between  400 E x and 200 km) that faces the transitional plate boundary. We refer this effect to as an indenter-effect induced by the geometry of the transitional plate boundary which impedes subduction. The compressive principal stress in the back-arc to intraplate areas remains however lower than that in the arc/ back-arc NE corner of the same model. In the model with the highest values of trans E L , such a compressive principal stress vanishes.

Application to the Tectonic Duality During the Eocene
The main results presented above which are relevant for the comparison with the tectonic regime in the LASZ during the Eocene are: 1. In the context of an asymmetrical subduction zone bounded by a STEP fault at the south and a transition from subduction-to-strike slip at the north, the high trench-normal traction adjacent to the STEP-fault provokes tensile stresses at the surface of the overriding plate (oriented from NNW-SSE to W-E) in the southern portion of the margin at distances from the trench between 150 and beyond 400 km, thus ideally comprising the arc and back-arc regions. 2. At the NE-trench corner, the trench curvature controls the obliquity of subduction. The obliquity hampers the lengthening of the subducting slab and hence the associated trench-normal traction. 3. In the arcuate part of the subduction zone, the non-lithostatic forces transmitted by the subducting slab to the overriding plate through the subduction interface tend to converge toward the center of the curved trench. Depending on the trench-curvature radius, this induces different tectonic regimes at the NE corner of the CP: (a) When the trench-curvature radius is relatively low, the idealized arc/ back-arc regions can undergo a compressive principal stress oriented E-W to ENE-WSW. The ratio of compressive-to-tensile principal stresses is relatively high (>60%) and denotes a tectonic regime that tends to be transpressional. (b) When the trench-curvature radius is relatively high, comparable to the present-day radius of curvature of the LASZ, the compressive component of the principal stresses is limited. The ratio of compressive-to-tensile principal stresses is less than 40% and denotes a clear transtensional regime. 4. If the overriding plate is sufficiently weak, the trench-curvature radius can self-consistently increase through time according to the related stress field. In particular, some W-E stretching in the southernmost portions of the CP occurs. As a consequence, in the NE-corner, the compressive component of the principal stresses is progressively relieved. 5. At north, the westward displacement of the transitional plate boundary, which connects the eastern subduction contact fault to the western transform fault, induces high shear stresses in the idealized forearc area. The transitional plate boundary also acts as an indenter on the overriding plate and can induce a N-to-NE oriented compressive principal stress in the back-arc to intraplate area. This indenter-effect is approximately inversely proportional to the length of the transitional plate boundary.
Based on our modeling results, we suggest that the trench curvature of the LASZ, as well as the northern strike-slip and southern STEP boundaries, were major contributors to the evolution of the tectonic stresses in the arc and back-arc regions of the eastern Caribbean plate (Figure 8). Back in the early to middle Eocene (from ∼55-50 Ma to ∼40-35 Ma), we hypothesize that the radius of trench curvature in the NE corner of the plate was relatively low (R << 600 km). This promoted a transpressional regime in the the vicinity of the highly arcuated trench and corresponding to the region overlying the obliquely subducting plate which comprised from east to west: the Saba Bank, the Virgin Islands and Puerto-Rico. We note however that in our models the compressive component of principal stresses in the NE corner equals, at most, the tensile component. Other factors may thus be required to induce a dominant compressive component. As discussed below, the arrival of a buoyant feature such as the Bahamas bank may have played such a role. In the south, our models suggest that the rollback of the South American oceanic subducting slab may have assisted the opening of the Grenada basin by generating tensile stresses pointing toward the southern parts of the subduction trench, which is consistent with the direction of oceanic spreading suggested by previous studies (Bouysse, 1988;Aitken et al., 2011;Garrocq et al., 2021).
Note that just after the jump in the plate boundary between the CP and the NAM, the transitional plate boundary might have been of a reduced length, and might also have helped to reach the conditions of a transpressional tectonic regime in the back-arc and intraplate areas. From the middle Eocene onwards, the trench-curvature radius may have increased and caused a relief in the tectonic stresses at the NE corner of the Caribbean plate. This may have facilitated the cessation of transpression in the NE Lesser Antilles by the late Eocene. Part of the increase in the apparent trench-curvature radius may have self-consistently been induced by the deformation of the Caribbean plate under the North-South varying tectonic regime, as in our model with a weak OP. Alternatively, the accretion of oceanic crust in the Grenada basin during the middle Eocene might also have increased the apparent trench-curvature radius.
A shift in the tectonic regime of the arc/back-arc of the Lesser Antilles occurred in the late Eocene to early Oligocene period, causing SW-NE extension in the north (Cornée et al., 2021;Legendre et al., 2018) and the end of spreading in the Grenada basin (Garrocq et al., 2021, Figure 1c). Our models do not address the cause of this tectonic reorganization.

Other Implications for the Tectonic Evolution During the Eocene
Besides addressing a possible (simple) mechanism for explaining the Eocene-tectonic duality in the LASZ, our models may also shed light on other geological and paleogeographic observations in the region. Garrocq et al. (2021) have proposed two extensive phases that shaped the Grenada basin from the early to the middle Eocene: a rifting and a spreading stage. The authors proposed a consistent NW-SE direction of extension through both stages. Their spreading direction is compatible with a possible NW-dipping subduction of the Atlantic seafloor in the southernmost part of the LASZ, as suggested by previous tectonic reconstructions (e.g., Pindell & Kennan, 2009). Our models suggest instead that the NW-SE rifting and spreading episodes may also be compatible with a more W-dipping subducting slab. The latter case may therefore be compatible with the approximately N-S oriented outer arc inferred from magnetic anomalies east of the Tobago Basin and which might be Eocene in age (Allen et al., 2019).
The underthrusting of the Venezuela Basin beneath Puerto Rico and Hispaniola at the Muertos Trough accommodated a relative, probably modest (Boschman et al., 2014), convergence between the Caribbean and the North American plates (Figure 1). The estimated date of formation of the Muertos Trough and the associated thrust deformed belt varies between the Cretaceous (Byrne et al., 1985) and the Miocene  but several studies have pointed out a possible start at Eocene Times (Granja-Bruña et al., 2014;Leroy et al., 2000;Mauffret & Leroy, 1999). It has been generally proposed that the arrival of the buoyant Bahamas platform at the Puerto Rico trench was the trigger of the formation of the thrust belt (Granja-Bruña et al., 2009;Mann et al., 2002;ten Brink et al., 2009). Our models suggest an alternative mechanism in which the intraplate region facing the northern transitional plate boundary undergoes a N-to-NE oriented compression. Furthermore, the modeled magnitude of the latter displays an inversely proportional relationship to the length of the transitional plate boundary. Although its length is unknown in the natural case at Eocene times, one may hypothesize that following the jump in the plate boundary (from NE Cuba to N of the Greater Antilles, Figure 2a) this transition was quite sharp. It follows that intraplate compression might have affected the north of the Venezuela Basin in the early to middle-Eocene and might have been accommodated through its underthrust at the Muertos Trough, releasing the compression at farther distances. At later times, the possible increase in the length of the transitional plate boundary may have limited this compressive component.
According to our models, two tectonic regimes may have coexisted during the Eocene in the arc/back-arc regions of northeastern and northern LASZ. In the former, a transpressional regime may have held in the arcuate NE corner for as long as the trench-curvature radius was relatively low. Slightly west of the NE corner another regional transpressional regime may have resulted from a sharp transitional plate boundary. Based on our modeling, we expect the two areas experiencing the most prominent transpressional regime to slightly migrate westwards through time mostly because of the westward displacement of the transitional plate boundary. As discussed above, following accommodation of inland compression at the Muertos Trough and an increase in the trench-curvature radius, the westward migration of transpression may have been coeval of a strong reduction in the magnitude of the compressive component of the stresses by the late Eocene. We nonetheless acknowledge the existence of evidence for an eastward migration of compressive stresses instead, as recorded by crustal exhumation episodes of decreasing age from Cuba to Puerto Rico (Roman et al., 2020). This eastward migration of compressive events is often regarded as the consequence of the eastward migrating front of the collision with the Bahamas bank which started in Cuba in the Paleocene (Roman et al., 2020). As discussed below, our proposed mechanism may be an additional process to take into account for understanding the geodynamical evolution of the northern Caribbean. Nevertheless, our models also suffer from other few limitations which we discuss in the next subsection.
A major tectonic event is thought to have occurred during the Eocene which may have caused the rise and the demise of a land bridge in the arc or back-arc areas, thus corresponding to the Aves Ridge (GAARlandia hypothesis, Iturralde-Vinent & MacPhee, 1999), thereby allowing for the dispersal of terrestrial fauna from South America to the Greater Antilles (e.g., Marivaux et al., 2020). However, this paleogeographic model has been regarded as controversial (e.g., Ali, 2012). Recently,  provided geological evidence that advocates for a geodynamical-triggered regional uplift consistent with the GAARlandia hypothesis (see also Cornée et al., 2021). They showed that the period of shortening in the arc/back-arc of the Northern Lesser Antilles was indeed associated to a regional uplift in the middle to late Eocene (emersion of the GraNoLA land) and suggested that the compressional event was triggered by a plate-kinematics reconfiguration. Our study provides an alternative geodynamical mechanism that may have helped to form emerged lands and later assisted their subsidence in the NE corner of the Lesser Antilles. It is a step forward in trying to connect deep-solid Earth dynamics and surface biogeographical evolution in the eastern Caribbean. Further studies are nonetheless required to decipher what caused a transient-period of uplift in the southern parts (Aves Ridge) which may have permitted the fauna dispersal from South America to the north-eastern Caribbean.

Assumption of an Inviscid Mantle
In our modeling approach, we only take into account the effect of the ambient mantle through the density contrast (Forsyth & Uyeda, 1975). A viscous mantle may however exert both normal stresses induced and shear stresses on the plates-mantle interface (Funiciello et al., 2003;Lallemand et al., 2008;Royden & Holt, 2020;Tovish et al., 1978). In particular, the toroidal flow, that is the horizontal-component of upper mantle flow occurring around the edges of the subducting plate from the rear of the slab toward the front of the slab (Funiciello, 2003;Schellart, 2004), induces shear stresses at the base of the plates and may facilitate back-arc opening (Alsaif et al., 2020;Chen et al., 2016;Schellart & Moresi, 2013). In the Caribbean, a toroidal flow around the southern termination of the American subducting plate might have favored the opening of the Grenada basin, while a more oblique subduction at north may have impeded it, thus facilitating a latitudinal duality of surface tectonics. We hypothesize that this effect, if of a sufficient magnitude, would thus have reinforced the tectonic duality observed in our models, but would not have drastically changed the first-order trends in the stress field. In addition, mantle resistance to slab rollback and induced toroidal flow around slab edges have been suggested to promote a SP-wards concave subducting slab shape at mid-upper mantle depths (Schellart et al., 2007). It is possible that such a deformation could have enhanced the unbending of the LASZ trench. Yet, laboratory analog models have shown that this effect might be minored for relatively narrow subduction zones such as the LASZ (Guillaume et al., 2021). Finally, it is noteworthy to mention that present-day upper mantle flow inferred from regional seismic anisotropy does not resemble to a classical toroidal flow beneath the eastern boundary of the Caribbean plate (Zhu et al., 2020). This may be due to the nearby presence of much larger subduction zones, such as the Andean subduction zone, which may affect the background mantle flow in the vicinity of the LASZ (Russo & Silver, 1994). Back in time, the background mantle flow is unknown and thus strong assumptions would have been needed for carrying out an accurate regional modeling. Overall, the modeling approach that we undertake, although neglecting the ambient upper mantle flow, offers a useful approximation of the forces transmitted by the subducting slab to the overriding plate and the induced overriding plate surface tectonics. The evolution through time of the trench-curvature radius in our models arising from the stress field, might be a lower estimation because of the neglection of the upper-mantle three dimensional flow.
Besides the effect of upper mantle flow, another potential caveat of our models is that we neglect the interaction of the subducting slab with the upper-lower mantle discontinuity at a 660-km depth. To date, no consensus exists on the subducting slab shape beneath the LASZ at and through the 600-km discontinuity since regional tomography has suggested both that the slab lies on top of the 660-km depth (van Benthem et al., 2013) and that its has penetrated into the lower mantle (Braszus et al., 2021). The latter scenario may diverge the most from the modeled geodynamical evolution in our study. Indeed, a viscosity increase at the 660-km discontinuity hampers the slab sinking and can lead to its vertical buckling and folding atop and through the discontinuity (Agrusta et al., 2017;Garel et al., 2014;Lee et al., 2011). Slab folding may, in turn, affect the overriding plate tectonics, producing alternate periods of compression and extension in the back-arc as shown in models of straight subduction zones (Boutoux et al., 2021;Cerpa et al., 2014Cerpa et al., , 2015Lee et al., 2011). To our knowledge, there is no study that has quantified the impact of slab folding at the 660 in the context of highly arcuate subduction zones. Thus, we only can hypothesize how slab folding might have affected the more straighter southern part of the LASZ. It is indeed possible that the extensional regime that we observe in our models and that we relate to the period of stretching and spreading in the Grenada basin, was coeval of the backward (SP-wards) motion of slab fold. The forward (OP-wards) motion of the slab fold might have provoked the reversal of the extensional tectonic regime and thus lead to the halt of back-arc spreading. Further modeling studies would be required to address this scenario if the penetration of the Lesser Antilles subducting slab into the lower mantle during the Eocene was confirmed.

Structural Heterogeneities Within the Caribbean Plate
At present-day, the north-eastern Caribbean crust has a thickness of ∼25 to up to ∼35 km from the backarc to the forearc (Kopp et al., 2011;Melekhova et al., 2019;Padron et al., 2021). The southern-eastern part of the CP is characterized by the presence of a thin (5-10 km) oceanic crust in the Grenada and Tobago basins ( Figure 1) (Christeson et al., 2008;Padron et al., 2021), separated by the post-mid Eocene volcanic arc-crust, that reaches a thickness of 29-33 km beneath the arc islands (Melehkova et al., 2019). West of the Grenada basin, the Aves Ridge has an average thickness of ∼25 km comparable with the northern crust (Christeson et al., 2008;Padron et al., 2021). Prior to the rifting episode which triggered the Grenada basin opening, the Caribbean crust might have been more homogeneous along the active arc. The rifting and the oceanic spreading likely induced spatio-temporal variations in the strength of the Caribbean plate from North to South. This may have reinforced the dual tectonic evolution of the Caribbean plate. In contrast, in our models, the homogeneous strength of the overriding plate cannot evolve nor in space neither with time. Moreover, the localization of tectonic deformations nearby the spreading center during the Eocene may have limited the transmission of stresses within the CP. If such a process was included in our models, we would expect it to hamper the NNW-oriented extension (due to the southern trench-normal traction) observed in the NE corner of our modeled CP, and to promote a dominant transtensional regime in this area.

Effect of the Subduction-Collision of the Bahamas Bank
We have not directly addressed the potential effect of the collision of the northern Caribbean plate with the buoyant Bahamas platform (apart our working assumption of a plate boundary jump in the Late Paleocene). Such a collision in Cuba is thought to have played a major role in the tectonic evolution of this region in the Paleocene-early Eocene, inducing ultimately a re-organization of the North America-Caribbean plate boundary. However, the effect of a possible (south)east-ward propagation of the collision front is yet to be determined. For instance, the arrival of the SE-end of the Bahamas platform into the subduction trench facing Puerto-Rico, was suggested to trigger a transpressional regime in the middle to late Eocene (Lao-Davila et al., 2012;Laó-Dávila, 2014;Román et al., 2020). In fact, Wallace et al. (2005) and Wallace et al. (2009) proposed a model for the tectonics nearby a transition from collision-to-subduction. In their model, the arrival of a buoyant feature (collision) generates the bending of the margin, and induces prominent compression in the regions facing the collisional segment while potentially inducing back-arc rifting away from the collision. The latter occurs as the bending of the margin is accompanied by a continued slab-rollback which is accommodated by the rotation of micro-forearc blocks. The model has been recently invoked by  and Boucard et al. (2021) to explain the formation of V-shaped forearc basins after the late Eocene.
Whether Wallace et al.'s model could explain the evolution of the LASZ for the entire Eocene remains an open question. The records of compression in Hispaniola indeed points out to a "soft collision" (i.e., leaving few markers of compression, see Section 2), if at all induced by the subduction of the Bahamas platform (van Benthem et al., 2014). Similarly, the record of a rather soft-collisional environment in Puerto-Rico during the Eocene, lead Laó-Dávila (2014) to propose that the nature of the buoyant feature entering the subduction trench was a thickened oceanic crust. It is worth noting that the underthrusting of the SE-continuation of the platform offshore Puerto-Rico has also been proposed to take place only later in the Miocene (Grindlay et al., 2005;Mann et al., 2002).
Here, we suggest that the effect of the Bahamas collision, if it occurred at Eocene times, may have been, at least, largely assisted by the effect of a nearby subduction zone under a highly curved trench and perhaps also by the indenter effect induced by a transitional plate boundary. This hypothesis is in line with the work of van Benthem et al. (2014) who proposed that a force exerted by the along-strike displacement of the western-edge of the slab (a "slab edge push") beneath the northern Caribbean plate boundary was the main driver of regional tectonics, and exceeded the effect of the Bahamas platform collision. Although these authors assumed that the Bahamas subduction only started in the Oligocene onwards, a similar force balance may have occurred if the subduction of the platform occurred earlier. Further work should nonetheless be carried out to quantify the joint effect of a (soft-)collision nearby a transitional plate boundary and a time-evolving curved subduction trench.

Conclusions
Recent studies have shed light on a singular tectonic regime in the arc/back-arc region of the LASZ for at least part of the Eocene. While the southernmost part underwent stretching in the Grenada basin, the northern part underwent thrusting and shortening under compressional and/or transpressional tectonic regime. Our mechanical models of subduction suggest that this Eocene-tectonic duality may have been generated by both a relatively low trench-curvature radius at the NE-corner of the Caribbean plate in the context of asymmetrical Caribbean plate boundaries at the North (from east to west: highly oblique subduction to a strike-slip system) and at the South (a STEP-like boundary). A compressional/transpressional regime at north and an extensional regime at south may have resulted in an increase in the apparent trench-curvature radius, especially if tensile stresses were accommodated by oceanic spreading at South. Our models suggest that trench unbending, that is the increase in the trench-curvature radius, could have relieved the compressive stresses in the northern part through time.

Data Availability Statement
The structural data ( Figure 1) used in our work is from published studies Garrocq et al., 2021) which provide the details on how to access their publicly available data.