Magellan SAR images are very useful to map the various tectonic features on the surface of Venus [Ford et al., 1989; Farr, 1993; Tanaka et al., 1994]. The tectonic features are wrinkle ridges, folds, fractures, and shear zones or fault systems, which are manifested in SAR images as lineaments and surfaces, whose radar brightness or darkness and tonal contrast are used to characterize the form, position, and orientation of these structures, and to establish the relative time relationship between them (e.g., crosscutting relationship). Hansen and Willis  and Ghent and Hansen  have succinctly summarized the methods of identification of the various tectonic structures using SAR images, and carried out structural and kinematic analysis for building the tectonic history of a few complexly deformed portions of Venusian crustal plateaus. In this present study, a detailed structural geological map has been prepared for the western, central and eastern segments using the right-looking, high-resolution Magellan SAR images (75 meters per pixel) to understand the overall tectonic history of the TBSZ. The details are given in the following sections.
3.1. Western Segment
 Figure 3 shows the SAR image and lineament map of the western segment, where the shear zone is narrow (width: ∼25 to 100 km) with an overall trend of 065°–075°. In the western segment, the contact zone between the TBSZ and the tessera terrain of NW block provides an important clue for understanding the kinematics of this shear zone (Figures 3a and 3b). Tuckwell and Ghail  did not include this zone in their kinematic analysis. The present study reveals that, north of this shear zone, the tessera terrain contains two intersecting sets of folds: the dominant NNW-SSE to N-S oriented folds (younger folds), which cut across the other set of NE-SW trending folds (older folds) (Figure 3a). Along the northern boundary of the shear zone, the younger folds of the tessera terrain are dissected by closely spaced minor shear zones (Figure 3c), and the folds are dragged into parallelism with the shear zones, which give rise to gradational change in the orientation of these younger folds from N-S to NE-SW toward the shear zones (Figures 3b and 3c). In addition, the widths of these folds also gradually decrease toward the shear zones. The observed deformation pattern is possibly a result of rotation and shortening accompanying a simple shear deformation. Displacement or rotation (deflection) of preexisting structures may be used as a good shear-sense indicator, especially if the movement direction is more or less normal to the preexisting structures [Ramsay, 1980; Carreras, 1997]. In the western segment, the trends of the younger folds of the tessera are more or less normal to the shear zone boundary (Figures 3a and 3b). While approaching the shear zone, these folds are gradually dragged into parallelism with the shear zone (Figures 3b and 3c), because of a clockwise rotation and possible shortening associated with a dextral or right-lateral motion. There is no indication of left-lateral or sinistral displacement of the preexisting structures along the TBSZ boundary. Interestingly, along the southern boundary of the TBSZ, the NW-SE striking ribbons (which are tightly spaced paired lineaments, oppositely dipping steep-sided walls with flat floors) and WNW-ESE trending fractures (single lineaments with uniform radar brightness) of the Thetis marginal belts (Figure 2b and 3a) abruptly terminate at the shear zone boundary, and are not dragged by the shear zone (similar to the brittle shear zones). It is not clear why the shallow crustal rheology in this part is so different compared to the northern boundary of the TBSZ.
Figure 3. (a) Right-looking, full-resolution Magellan SAR image of the western segment. See Figure 2a for its location in the TBSZ. The white boxes show the positions of Figures 3c, 3d, and 3e. The tessera contains two intersecting sets of folds, the older folds are NE-SW oriented (one of them is labeled 1), and the younger folds are NNW-SSE to N-S oriented (one of them is labeled 2). (b) Structural and kinematic interpretation. Inside the shear zone the Set 1 lineaments are sigmoidal folds, which are interpreted to be S bands, and the Set 2 lineaments are ridges and are shown as C bands. Note the preexisting younger folds of tessera (labeled early-formed structures) are dragged into parallelism with the shear zone, indicating dextral sense of displacement. (c) Preexisting northerly trending younger folds of the tessera (black arrow) are cut and dragged by closely spaced minor shear zones (white arrow). Labels: R, ridge; T, flooded trough. (d) The Set 1 lineaments, which are folds showing sigmoidal curvature similar to S bands of shear zones and are not transected by the minor shear zones shown in Figure 3c. (e) The NNW-SSE to N-S oriented fractures; one of them is labeled.
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 Inside the shear zone, three sets of linear structures are mapped (Figure 3): dominantly NE-SW striking tightly spaced lineaments (Set 1), ENE-WSW striking lineaments (Set 2), and NNW-SSE to N-S striking isolated lineaments (Set 3). These sets clearly cut across the low-lying plains, which are characterized by smooth, radar-dark fields, and may be composed of lava flows (Figures 3a and 3b). Therefore the shear zone lineaments are younger than the plain units. The Set 1 lineaments are oblique to the shear zone boundary, while the Set 2 lineaments are parallel to the shear zone boundary. The Set 1 lineaments are abundant close to the southeastern boundary of the tessera terrain as well as near the northwestern boundary of the Thetis marginal belts (Figures 3a and 3b), while the Set 2 lineaments occur all along the shear zone. Tuckwell and Ghail  did not include the Set 1 lineaments for structural and kinematic analysis, but they interpreted the Set 2 lineaments as fault scarps representing Riedel shears of a sinistral shear zone. The gradual change in brightness across the crest of the Set 1 lineaments indicates that they are folds (Figure 3d). These Set 1 folds are restricted only to the shear zone, as these are unaffected by the folding events of the tessera terrain. Clearly, the Set 1 folds are dragged into parallelism with the Set 2 lineaments, which are long and linear ridges with flooded troughs. As a result, the tightly spaced folds show sigmoidal curvature against the ridges (Figures 3b and 3d). Also, it appears that the ridges and troughs show bending toward the folds (Figure 3b). This would indicate the mutual interaction between the folds and ridges and troughs. The entire structural assemblage appears similar to S–C-like structures of the large-scale ductile shear zones on Earth. On the basis of form, position and angular relations, the Set 1 folds can be interpreted to be the S bands, and the Set 2 ridges and troughs can be related to the C bands of the large-scale ductile shear zones (Figure 3b). Acute angle between the S and C bands suggests dextral or right-lateral displacement. The closely spaced sigmoidal folds defining the S bands and the low-angle between S and C bands (10°–25°) would indicate a ductile deformation under high-shear strain. On Venus, the ductile shear zones with S–C-like structures were reported from Itzapapalotl Tessera of the northern Ishtar Terra [Hansen and Willis, 1996].
 The Set 3 lineaments are widely spaced, straight, and are abundant in the eastern side. Most of them strike in a NNW-SSE to N-S direction. Tuckwell and Ghail  interpreted these lineaments as dip-slip extensional faults. In the present study, these lineaments are interpreted to be fractures as they display uniform radar brightness and high tonal contrast compared to the surrounding plains (Figure 3e). Moreover, these fractures terminate abruptly against the Set 2 ridges and do not show bending toward them. It is possible that the fracture development may be the result of later reactivation of the TBSZ. Terrestrial examples also show that the reactivation of crustal-scale ductile shear zones produce large-scale fracture systems [e.g., Destro et al., 1994].
 S–C structures [Berthé et al., 1979; Lister and Snoke, 1984] are found to be associated with brittle [e.g., Lin, 1999, 2001], semiductile [e.g., Shimamoto, 1989] and ductile shear zones [e.g., Ramsay and Listle, 2000; Passchier and Trouw, 1997]. The two foliations (S and C) are formed synchronously during a single, progressive, noncoaxial deformation event. The C planes are formed parallel to the shear zone boundaries, while the S planes are developed oblique to the shear zone boundaries and are considered to be parallel to the plane of maximum flattening (XY-plane of the finite strain ellipsoid). Coaxial shortening and extension of the S planes would produce folds and wrinkle ridges on brittle-ductile to ductile surface layers of Venus. In addition, the simple shear operating on the C planes would drag these folds and ridges, giving a sigmoidal shape. At low shear strain, the angle between S and C planes is ∼45°. This angle decreases with progressive strain due to rotation of the principal axes of the finite strain ellipsoid during progressive simple shear deformation. Acute angle relationship between S and C planes can be used as a reliable shear sense indicator. The acute angle opens in the movement direction of the main shear zone. A third set of planes (C′ planes) may be formed at low angle to the C planes (∼15°–35°) [Passchier and Trouw, 1997]. Acute angle between the C and C′ planes opens in the opposite direction relative to the main movement direction of the shear zone. The C′ bands show same sense of movement of the main shear zone (synthetic movement). In addition, a limited antithetic shear may also operate on the S planes in consequence of rotation of the XY plane of finite strain. This antithetic shear occurs when the preexisting S planes are passively rotated in parallel with rotation of the XY plane of finite strain ellipsoid. When antithetic shear operates on S planes, it impedes the formation C′ planes. On the other hand, synthetic shear on S planes leads to the development C′ planes [see Hippertt, 1999].
 The study by Hippertt  shows that S–C geometry defining both S–C structures and S–C-like structures shows a scale-invariant geometry. The relationship between the average spacing between adjacent S and C planes (S spacing and C spacing) in a typical S–C structures as well as in the conjugate movement zones (which show S–C-like geometry) of different scales (few millimeter to several hundreds of kilometer) follows a simple function Cspacing = 2 Sspacing, with a goodness-of-fit R > 99%. This simple function shows that the relation between S and C spacing is statistically constant over a scale range of ten orders-of-magnitude. However, on the basis of fractal analysis, Hippertt  further indicates that S–C fractal set is restricted to the scale range of <1 mm to 1 km, where the S–C structures show antithetic shear on S planes (genuine S–C structures). Above this scale range, from 1 km to several hundreds of kilometer, S–C structures show synthetic movement on the S planes. These are designated as S–C-like structures. Therefore the term “S–C-like structures” is suitable to the large-scale shear zones showing S–C geometry, similar to the observed scale of deformation pattern of TBSZ (Figure 2).
3.2. Central Segment
 In the central segment, the overall trend of the shear zone is ∼055° (Figure 4). Width of the shear zone also increases to ∼150 km. The central segment is characterized by three sets of lineaments (Figures 4a and 4b): (1) straight to curvilinear Set 1 lineaments trending 010° to 035°, (2) ∼055° trending Set 2 lineaments, and (3) a small number of ∼080° trending Set 3 lineaments. The Set 1 lineaments are oblique to the shear zone boundary, while the Set 2 lineaments are parallel to it. Tuckwell and Ghail  interpreted the Set 2 and Set 1 lineaments as Riedel shears and normal faults with a few extensional grabens, respectively, in a sinistral strike-slip zone containing an extensional jog. Close examination of Figure 4a suggests that most of the Set 1 lineaments are physiographic ridges, as they display radar brightness on one side and have gradual transitions in brightness toward the other side, similar to a fold crest (Figure 4c). These ridges also show a weak sinuous pattern. Possibly these are wrinkle ridges. A few of the Set 1 lineaments are paired, which were interpreted as the extensional graben by Tuckwell and Ghail . The lineaments forming these pairs also show radar brightness on one-side and have smooth transition to radar darkness on the other side (e.g., Figure 4d). Clearly, these are ridges with their slopes dipping away from each other. The linear low-lying portion in between the two consecutive wrinkle ridges is a trough. At few places, these paired wrinkle ridges join each other to form single ridges (Figure 4d). The Set 2 lineaments also appear like the ridges at few places, but in other places they are possibly composed of a wide zone of compact deformation bands (Figure 4e). Beyond this, it is difficult to define the deformation bands robustly with the available resolution of SAR images.
Figure 4. (a) Right-looking, full-resolution Magellan SAR image of the central segment. See Figure 2a for its location in the TBSZ. White boxes indicate the positions of Figures 4c, 4d, 4e, 4f, and 4g. The wrinkle ridges define the S bands and are labeled S. The deformation bands represent the C bands, which are labeled C. The wrinkle ridges show sigmoidal curvature against the deformation bands. The fault scarps are labeled fs. (b) Structural and kinematic interpretation. Kinematic indicators suggest dextral sense of displacement. Note the presence of three sets of lineaments similar to the S, C, and C′ bands of large-scale ductile shear zones. (c) Set 1 lineaments, the wrinkle ridges, which are interpreted to be the S bands. (d) Also Set 1 lineaments, the paired wrinkle ridges to form single ridges. Note the wrinkle ridges sharply terminate against the fault scarp and do not show bending. (e) Set 2 lineaments, the deformation bands representing the C bands. (f) A dyke crosscutting the deformation bands but terminating sharply against the fault scarp. Note fault scarps are more prominent than the deformation bands. (g and h) A brittle-ductile shear zone displacing the NE-SW trending ridges right-laterally, clear evidence for dextral motion.
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 The Set 1 and Set 2 structures also show mutual crosscutting relationship, and have gradational change in their orientation at the intersection between these two sets. This would suggest that these are broadly contemporaneous. Lenticular domains of less deformed plain occur in between them. Form and geometric relationships between these two sets of lineaments suggests that these are traces of the large-scale S and C bands of the ductile shear zones, similar to the western segment. Therefore Set 1 and Set 2 structures are interpreted as a large-scale S and C bands, respectively. Development of sigmoidal wrinkle ridges is consistent with this interpretation. The acute angle relations between the S and C bands indicate dextral sense of displacement. Figures 4g and 4h show that the ridges defining the S bands are cut by ENE-WSW oriented brittle-ductile shear zone, which displace the ridges right-laterally, confirming dextral motion in the central segment. But using the angular relationship between the Set 1 and Set 2 lineaments, Tuckwell and Ghail  suggested sinistral sense of displacement considering the Set 2 and Set 1 lineaments as Riedel shears (R shears) and antithetic Riedel shears (R′ shears), respectively. In a sinistral shear zone, the R shears should show synthetic movement, i.e., sinistral sense of displacement. But Figures 4a, 4g, and 4h clearly show that the so-called R shear (shown as C band in the present study) is characterized by dextral sense of displacement. This evidence does not support the interpretation of R shears.
 A few lineaments (N-S oriented), which are straight, cut across the C bands (Figures 4a and 4f). Also, they do not show bending toward the C bands. These lineaments also show uniform radar brightness and high tonal contrast compared to the surrounding plains. These are possibly dykes. One such dyke is shown in Figure 4f. Some of the lineaments present in the southeastern part of Figure 4a, which are parallel to the Set 1 lineaments (wrinkle ridges) of the northwestern part, are problematic, due to insufficient resolution of the SAR image. These lineaments show curvature similar to the Set 1 ridges and are unlike the dykes that are straight. These are also probably the S bands but this interpretation should be considered with caution. The central segment shows evidence for reactivation of the shear zone. For example, development of fault scarps is observed in the central part (Figures 4a). These fault scarps are oriented in a ∼NE-SW direction, approximately parallel to the deformation (C) bands. These fault scarps appear more prominent than the deformation bands (Figure 4f). At few places the wrinkle ridges and dykes sharply terminate against the fault scarp, and do not show bending (Figures 4d and 4f). The fault scarps are possibly the product of reactivation of the preexisting deformation bands.
 The Set 3 lineaments are observed only near the southeastern boundary of the shear zone, and are less prominent to define their form with confidence (Figures 4a and 4b). The Set 3 lineaments are interpreted to be the subsidiary shear zones (C′ bands) displacing both the S and C bands synthetically. The C′ bands would cause synthetic curving of the S bands, which is akin to S-C structures. The Precambrian Rio Paraiba do Sul Shear Belt of southeastern Brazil is an excellent terrestrial example for a very large scale ductile shear zone containing a package of S–C-like structure similar to the western and central segments (Figure 5) [Ebert et al., 1996]. In the northwestern part, the Set 1 ridges and Set 2 deformation bands terminates near the lava plains. It is possible that the plains partly cover these tectonic structures.
Figure 5. A terrestrial example of >1000-km-long and ∼200-km-wide shear zone showing S–C-like structures, Rio Paraiba do Sul shear zone of SE Brazil (modified from Ebert et al. ). Granulite-facies rocks, migmatitic gneisses, granites and some supra-crustal belts comprising the metamorphosed volcanic and sedimentary rocks are the major rock types exposed in this shear zone belt.
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3.3. Eastern Segment
 The eastern segment forms the northeastern bend of the TBSZ. It is characterized by a wide zone (>200 km) of branching, anastomosing ductile shear zones (Figures 2 and 6). At several places, lava flow units (the smooth radar-dark areas) partly cover the shear zones, and at few places, the shear zones cut the flow units. Therefore it is possible that the volcanism and tectonics are coeval events in the eastern segment. Tuckwell and Ghail  did not include the eastern segment in their study. The present study reveals a pattern of imbricate ductile strike-slip shear zones delineating sigmoidal mega-lenses of less deformed materials (Figure 6b). The Set 2 shear zones of the central segment (C bands) continue to this eastern segment forming the main shear zone fabric. While the strike of main shear zones is ∼070°, the strike of imbricate shear zones is ∼040°. Clearly, the imbricate shear zones are brought into parallelism with the main shear zones. The sigmoidal internal fabric bounded by the imbricate shear zones is characterized by tightly spaced folds, which are gradually brought parallel to the main shear zones. The strong sigmoidal curvature of the folds consistently suggests dextral sense of displacement. This system of imbricate shear zones is interpreted to be the contractional ductile strike-slip duplexes. The formation of sigmoidal folds is possibly the result of compression associated with the duplex development.
Figure 6. (a) Right-looking, full-resolution Magellan SAR image of the eastern segment. See Figure 2a for its location in the TBSZ. (b) Structural and kinematic interpretation. Note the presence of strike-slip ductile duplexes at the restraining NE bend of the TBSZ. The sigmoidal folds defining the internal fabric indicate dextral sense of displacement. See text for more details.
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 Strike-slip shear zones commonly exhibit bends or steps along their length. Depending on the orientation of the bend and the shear sense, these bends can become sites of extension (releasing bend), or compression (restraining bend) [Woodcock and Fischer, 1986]. Releasing bends are typically associated with the development of extensional pull-apart basins, whereas restraining bends are associated with the formation of complex systems of shear zones called contractional strike-slip duplexes [Woodcock and Fischer, 1986]. The structures in the eastern segment of the TBSZ resemble contractional strike-slip duplexes, and may represent a kinematic pattern for strain accommodation in response to a bend of a ductile mega-shear zone [e.g., Vauchez and Egydio-Silva, 1992]. An excellent terrestrial example is the Potengi-Patos shear zones of the Borborema province in NE Brazil [Vauchez et al., 1995; Corsini et al., 1996] (Figure 7). If we take the interpretation of sinistral motion into consideration [Tuckwell and Ghail, 2003], the eastern segment should form the releasing bend of the shear zone, which would be the site of extension. Extension associated with such releasing bend should produce pull-apart basins, which are absent in the eastern segment. In contrast, the eastern segment shows clearly the development of strike-slip ductile duplexes, which are the products of compression. This is only possible when the main movement direction of this shear zone is dextral. Therefore the evidence found in the eastern segment further strengthens the interpretation of dextral motion.
Figure 7. (a) Landsat image of the Potengi-Patos shear zone of NE Brazil (Figure 2 of Corsini et al. , reproduced here with permission from Elsevier). (b) Structural sketch map of the ductile duplex developed in the Potengi-Patos shear zone (modified Figure 3 of Corsini et al. , reproduced here with permission from Elsevier). Migmatitic gneisses, granites, metamorphosed volcanic, and sedimentary schistose rocks are the major rock types constituting the shear zone belt. At several places the shear zones defining the duplex are composed of mylonites a few kilometers thick.
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