Torque is the rotation of an object around an axis caused by the product of a force and the perpendicular distance from the rotation axis to the force’s application point [11] (). Torque is a magnitude that describes the dynamics of a rotating rigid body, the forces that mobilize objects and systems [11] . When the force acts perpendicularly at a greater distance from the lever arm, the effectiveness of the torque is maximum [11] (; . Lower torque is produced depending on the magnitude of the force, the distance of application of the force to the centre of rotation or the direction of application of the force [11] (). Torque deformation results in secondary forces, rotations, folds, and fractures [12] (). At the torque support point, there is extension in the convex area and compression in the concave area [12] - [14] ( (c) ). If the force acts on the lever arm at an angle less than 90˚, transpression or transtension generates parallel forces inside the lever arm body that cause shear deformation [12] [15] [16] ( (c) ). As the deformation of the fold progresses, extension fractures originate that converge at the support point [12] ( Figure 2 ). illustrates the natural breaking of a tree by torque. The torque on the tree trunk occurred instantaneously, under ambient temperature conditions. In detail, the torque generates fractures and deformation geometries similar to those found in rocks ( (b) ). On the scale of South America, the torque occurred over a period of about 148 Ma, on rocks with different rheological properties, taking advantage of pre-existing fractures and with heat sources provided by the magmatic rise. There is a clear and large difference in the geometries of the structures and in the tectonic morphology of the regions deformed by compression, extension and torque. In the Sierras Pampeanas of Argentina there are examples of torque deformation related to NE-oriented compressive forces [13] [14] [17] [18] .

According to the literature, the separation of South America and Africa occurred through extension, giving rise to the Atlantic Ocean. This extension is supposed to cause horizontal displacement and rotation in South America, generating continental drift. Three domains exist along the margins of South America and Africa [19] . The South Atlantic extensional domain developed from the southern tip of Argentina to the northeastern tip of Brazil. The location of the magnetic poles is evidence that during the Late Triassic to the Sinemurian, the South American continent would have been located in its southernmost position, then moved northwards, where it remained until the end of the Early Jurassic (). Finally, South America moved southwards again, and in the Middle Jurassic, it reached latitudes of almost 30˚S similar to those present [20] ( Figure 4 ). In the Equatorial Atlantic domain, a dextral strike-slip trend developed with an E-W direction and produced the rupture of the crust, creating a pattern of high-angle oblique faults that controlled rifting and resulted in the development of large-scale fracture zones parallel to the coast between the Aptian and the Cenomanian ( Figure 4 ). The third Central Atlantic extensional domain is in the region north of the mouth of the Amazon River, whose first rifting phase occurred in the Triassic.

Euler’s theorem describes the relative motion between two plates on the Earth’s surface by angular separation around a pole of relative motion, known as the Euler Pole [3] . Thus, in relative plate motion, the pole of any two plates tends to remain fixed relative to each other for long periods, even though the plate velocities are equally constant over periods of several million years [3] .

Western South America was situated on an eastward-tilted subduction zone since the Paleozoic and contraction events shortened the crust in the back arc during the Carboniferous, Permian and Jurassic [7] ( Figure 4 ). The opening of the Atlantic Ocean between South America and Africa begins with convection currents in the Earth’s mantle that generate the forces that push the plates [1] [21] . The opening of the Atlantic extended from the Upper Jurassic in the south (Rawson-Outeniqua segment) to the north (Pelotas/Walvis segment) in the Barremian [4] [22] [23] ( Figure 4 ). Between 138 and 127 Ma (Ar⁴⁰/Ar³⁹ geochronology) [24] , effusive activity at the Walvis hotspot gave rise to the Serra Geral Basalts in the Paraná and Etendeka Basin in Namibia [1] ( Figures 4-6 ). The breakup of Gondwana generated semi-grabens on the continent due to the reactivation of Paleozoic structures [4] that were filled with continental volcaniclastic deposits from the Late Triassic to the Early Jurassic, related to dextral displacement along the main strike-slip faults that limit the continental plates [4] [25] .

These basins were associated with N, NW-trending horizontal faults and dextral displacement, such as the Gastre fault system, and some blocks underwent rotation [4] [20] [23] [25] . The clockwise rotations observed in the rocks of the Deseado Massif, which occurred between the Jurassic and the Early Cretaceous, document the deformation of southern Patagonia during the breakup of western Gondwana [27] ( Figure 4 ).

The opening of the South Atlantic Ocean in the Early Cretaceous cut Paleozoic-Mesozoic cratons and sedimentary basins and caused the South American plate to push westward at a speed of 3 cm/year, separating Africa from South America, controlling variations in the convergence rate along the subduction zone [1] [2] [21] [30] . South America increased westward drift after the Cenomanian [31] ( Figure 4 ).

The Cretaceous basins of the Sierras de Córdoba originated by dextral strike-slip faults, arranged in an echelon, associated with the Eastern Pampean Lineament that presents a dextral horizontal displacement [29] . The largest depocenter of the Cretaceous rift is formed in northern Argentina by the Tres Cruces and Metan-Alemanía basins, which trend NNW, and the Lomas de Olmedo basin, which trend east-west. The latter represents the basin’s most active and deepest depocenter, limited to the north by the Michicola Ridge, whose faults reach more than 6 km of rejection, and to the south by the Quirquincho Arch [32] . Radiometric dating of the eruptive rocks in the Pirgua Subgroup sequence indicates ages of 128.95 Ma and 78.75 Ma [33] ( Figure 4 ). In South America, the Triassic basins were reactivated during the Cretaceous, spreading in an NNW strike from the Salado and Colorado basins, covering a large part of NW Argentina to southern Bolivia [1] . The Amazon and Marajó basins were formed during the extensional tectonic phase of the middle Cretaceous to early Tertiary [34] , and the Amazon River began as a transcontinental river between 11.8 and 11.3 Ma [35] ( Figure 4 ). The definitive opening of the Atlantic Ocean in the equatorial zone during the Albian was the beginning of the absolute displacement of the South American plate, starting the compressive deformation in the segments of Peru and Colombia at 100 Ma [30] ( Figure 4 ).

The geometry of the Nazca Plate beneath the South American continental plate [36] [37] is related to the collision zones between the Nazca and Juan Fernández ridges with the edge of the continent [38] - [40] . The first widespread contractive events in the Andean Cycle appear to have occurred in Santonian-Campanian times, shortly after the final disconnection between Africa and South America in the present-day Equatorial Atlantic [41] ( Figure 4 ). A Cretaceous-Paleogene (pre-Andean) episode of back-arc bending subsidence is recognized, followed by a Neogene Andean episode of crustal shortening reflecting the eastward propagation of the orogenic wedge to its present position ( [7] . Between 14˚ - 28˚ S, the volcanism that occurred from 65 to 0 Ma is closely related to deformation, in particular, the preferential grouping of volcanic centres at the intersections of the frontal arc with areas of NW-trending lineaments [42] . In the Luracatao and Calchaquí valleys, there is evidence of these Paleogene deformations [43] ( Figure 4 ). Some morphotectonic processes in the Andes, such as horizontal rotations and N-S compressions, cannot be fully explained by plate kinematics or simple compression-extension schemes [44] - [51] . In the Chilean forearc, strike-slip faults parallel to the margin develop, which do not seem to depend on the velocity or obliquity of convergence or the mode of mass transfer at the subduction front [52] . Different sectors of the Andes show a great variety of complex processes, such as mountain formation, which do not fit the type of non-collisional orogen that formed a mountain chain by subduction of oceanic crust under a continental plate, proposed by other authors [21] . On the Atlantic coast of Tierra del Fuego, the front of the Fuegian Andes fold and thrust belt migrated northwards due to compression 50 - 40 Ma ago, which may have ceased in the Early Miocene [53] ( Figure 4 ). The folded folds involving Neogene strata in the foreland of the Central Andes of the Precordillera, Sierras Pampeanas, Famatina System, Eastern Cordillera and Santa Bárbara System show an NNE shortening [51] . Different models explain the pattern of rotations observed in the Andean margin [44] [45] [54] - [57] . Paleomagnetic analyses of Jurassic to Neogene rocks in the flat subduction Pampean segment and the south, in the high-angle subduction segment, show clockwise rotations of up to 40˚ induced by a coupled model of the Bolivian Orocline-Juan Fernández Ridge [58] . In the Neogene, Andean tectonics caused crustal shortening, shaping the morphology of the South American foreland [59] [60] . Clockwise tectonic rotations are one of the most important structural features of the Andes of northern Chile, generated by transpressional deformation that affected large areas during the deformation that occurred in the Eocene and lower Oligocene [61] [62] ( Figure 4 ). The zone with the most remarkable shortening of the Andes is central Bolivia [63] . The hypotheses on the formation of oroclines refer to forces acting perpendicular to the axis of the orogen [64] or parallel to the axis of the orogen [65] generating a triangular tension zone in the convex part of the oroclines [44] . Paleomagnetic data of Paleozoic rocks show counterclockwise rotations in southern Peru and clockwise rotations in northern Chile and indicate that the Bolivian Orocline was formed during the Eocene-Oligocene by differential horizontal shortening coinciding with the most significant shortening of the Eastern Cordillera in this period [49] [66] ( Figure 4 ). Paleomagnetic results document a pattern of clockwise (25˚ + 11.6˚) rotations after the Paleocene and counterclockwise (19˚ + 9.7˚) rotations after the early Oligocene north and south, respectively, of the Huancabamba bypass, the coastal area of northern Peru (04˚ LS) [67] ( Figure 4 ). These results are consistent with those obtained from Cretaceous formations [68] and with those obtained from Mesozoic formations [69] , which indicate counterclockwise rotations of −30˚ south of the Huancabamba bypass. The WNW and NW shortening that reflects the Miocene and Pliocene structures, respectively, in the Uyuni-Atacama region, seems to be related to a rearrangement due to the absolute movement of the South American Plate to the WNW [70] ( Figure 4 ). The Andes’ escape towards the NE occurred during the 1.8 Ma due to the subduction of the Carnegie Ridge beneath the South American plate [71] , and the Santa Marta Massif experienced a clockwise rotation on the vertical axis in the Upper Eocene [72] ( Figure 4 ).

Convection currents in the Earth’s mantle generated the forces that exerted pressure on southern Argentina, and the South American plate began a process of torque deformation. In our concept of the deformation of South America, the horizontal and rotational movements of the continental plate were not independent of each other; they did not act separately. The rotation did not occur as a hinge ( (a) ), turning the entire continental plate of South America as if it were a solid monolithic block. On the contrary, these movements acted together at some point. The rupture and horizontal displacement of the Mid-Atlantic Ridge at a point in the south began to move the continental block that was anchored at its northern end (cratonic zones), generating an internal deformation by Torque ( (c) and Figure 3 ). The ruptures occurred in those areas of greatest weakness, intracratonic, keeping the cratonic zones together. We started a reverse path of the trajectory of South America, from its current position to its joining with the edge of Africa (), trying to follow the arrangement of the magnetic bands of the ocean floor generated by the hot spots [1] [22] [28] ( Figure 5 ). The geometric argument of the joining edges between South America and Africa is coherent, considering that between them there was a rupture and detachment by an extensive, constructive process. The western edge of South America must have been different from the current morphostructure because, since the separation of the continents in the Cretaceous, it has suffered destruction by compressive tectonic processes ( Figure 5 ). The first movement shows the southern coast of South America, which is slightly away from the southern coast of Africa, and the continents remain joined in the north ( Figure 5 ; indicated by the red line). This union marks the deformation’s beginning with torque and clockwise rotation. In the second stage, South America begins to detach from Africa, the rotation continues, and the torque’s support point is in Namibia ( Figure 5 ; position of the pink line). The deformation continues with clockwise rotation, and the torque now has its support point in the current areas of Belén and Sao Luís ( Figure 5 ; position of the dark green line). From the initial position of South America joined with Africa to the position of the light green line, the eastern edge of South America suffered a clockwise rotation and began to drift towards the SW ( Figure 5 ). Finally, South America moves west and north to its current position (blue line) from the position occupied by the eastern edge with the light green line ( Figure 5 ). This journey undergoes a clockwise rotation also ( Figure 5 ).

Towards the Triassic-Jurassic, the force generated by convection in the Earth’s mantle was in the extreme south of Argentina ( Figure 4 ); the pivot zone was located about 1800 km and 3100 km to the north, at the southern end of Africa ( Figure 5 ; red and pink lines) and (). The South American plate began a clockwise rotation path ( Figure 5 ). This torque deformation maximized the effectiveness of rifting and basin formation on the continental sector, where the geological units offered less resistance ( Figure 1 and Figure 6 ). The zones occupied by cratonic rocks (West Africa, Amazonia, Sao Francisco, Congo, Rio de la Plata, Kalahari) ( Figure 1 ) served as support and pivot points for the torque. The force exerted transtension on the southern edge of the rift basins ( Figure 6 ). This geometry allowed the formation of the Triassic and Jurassic rift basins along the western edge of South America, the dextral displacement of the faults that limit it and the clockwise rotation of some blocks ( Figure 6 ). This torque deformation process caused a clockwise rotation of South America from its initial position to the location of the eastern edge indicated by the dark green line ( Figure 5 ).

The forces that dominated the displacement of South America in the Early Cretaceous were in the region of the Colorado and Salado basins ( Figure 6 ), whose lever arms were about 4400 km away from the pivot point in the Belén-Sao Luis area ( Figure 5 and Figure 6 ). These forces opened the Cretaceous rift basins in the continental zones, bordering the Amazon, Río Apa and Río de la Plata cratonic zones to the west ( Figure 1 and Figure 6 ). The Paraná River basin in Argentina did not develop fully and constituted an aborted rift ( Figure 6 ). The edge of South America, represented by the dark green line ( Figure 5 ), had already begun to separate but was still very close to the coast of Africa. The displacement of South America continued to the SW, to the position occupied by the light green line ( Figure 5 ). The Amazon basin has an NE orientation similar to the Olmedo Basin in Argentina ( Figure 6 ). Both were formed in the Cretaceous and are oriented perpendicular to the remaining Triassic, Jurassic and Cretaceous basins ( Figure 6 ). The Amazon and Olmedo basins are likely to have been formed by extension generated by the torque in the outer part of the system, when the continents finally separated, as shown in (c) and Figure 3 . At that time the torque acquired greater magnitude until it finally broke the cratonic zones of Amazonia and west Africa ( Figure 1 ).

South America begins a journey towards the west and north from the light green line, continuing with the clockwise rotation ( Figure 5 ). This geometry means that the convergence is not strictly compressive, as reported in the literature. The Rio Grande Ridge (RGR) and the Walvis Ridge (WR) ( Figure 5 and Figure 6 ) are large igneous provinces in the South Atlantic, formed on the South American and African plates, respectively, mainly by the volcanism of a hot spot that erupted between 83.6 Ma and 66.4 Ma [73] ( Figure 4 ). At this time, we locate the east coast of South America at the position of the light green line ( Figure 5 ). The Rio Grande Ridge exerts the strength that moves South America in an NW direction ( Figure 6 ). Its position in the central area of South America displaces it towards the NW, where the ridges collide with the west coast of the continent at different angles of incidence ( Figure 5 and Figure 6 ). The violet line marks the position of South America when it probably begins to interact with the Juan Fernández Ridge in the Upper Eocene, as indicated by different authors in the literature [50] ( Figure 4 and Figure 5 ). Later, Iquique, Nazca and Carnegie ridges collide with the west shore of the South American Plate ( Figure 5 ). To reach its current position (blue line), South America must still travel to north with a clockwise rotation ( Figure 5 ). A new stage of torque deformation begins on the west coast of South America, which gave rise to the Andean chain ( Figure 6 ). The joint action of the Río Grande, Juan Fernández and Nazca ridges generated The Bolivian Orocline by transpression and torque. Each ridge collision with the west coast of South America constitutes a support and pivot point, developing a rotation with horizontal and vertical displacement. The speed of movement of the Juan Fernández Ridge was greater than that of the South American plate [2] [30] [39] . The Nazca Plate pushed towards the NE and the South American Plate towards the NW, resulting in an north trajectory ( Figure 6 ).