lable at ScienceDirect Journal of South American Earth Sciences 69 (2016) 226e242 Contents lists avai Journal of South American Earth Sciences journal homepage: www.elsevier .com/locate/ jsames The Alegre Lineament and its role over the tectonic evolution of the Campos Basin and adjacent continental margin, Southeastern Brazil Salom~ao Silva Calegari a, *, Mirna Aparecida Neves b, Felipe Guadagnin c, George Sand França d, Maria Gabriela Castillo Vincentelli e a Programa de P�os-Graduaç~ao em Geologia, Universidade de Brasília, Brasília, Brazil b Departamento de Geologia, Universidade Federal do Espírito Santo, Alegre, Brazil c Campus Caçapava do Sul, Universidade Federal do Pampa, Caçapava do Sul, Brazil d Observat�orio Sismol�ogico, Universidade de Brasília, Brasília, Brazil e Laborat�orio de Integraç~ao de dados Sísmicos e Geol�ogicos, Universidade Estadual Paulista, Rio Claro, Brazil a r t i c l e i n f o Article history: Received 29 July 2015 Received in revised form 9 March 2016 Accepted 14 April 2016 Available online 16 April 2016 Keywords: Brittle structures Reactivation Alegre Lineament * Corresponding author. E-mail address: salomaocalegari@hotmail.com (S.S http://dx.doi.org/10.1016/j.jsames.2016.04.005 0895-9811/© 2016 Elsevier Ltd. All rights reserved. a b s t r a c t The structural framework and tectonic evolution of the sedimentary basins along the eastern margin of the South American continent are closely associated with the tectonic framework and crustal hetero- geneities inherited from the Precambrian basement. However, the role of NW-SE and NNW-SSE struc- tures observed at the outcropping basement in Southeastern Brazil and its impact over the development of those basins have not been closely investigated. In the continental region adjacent to the Campos Basin, we described a geological feature with NNW-SSE orientation, named in this paper as the Alegre Fracture Zone (AFZ), which is observed in the onshore basement and can be projected to the offshore basin. The main goal of this work was to study this structural lineament and its influence on the tectonic evolution of the central portion of the Campos Basin and adjacent mainland. The onshore area was investigated through remote sensing data joint with field observations, and the offshore area was studied through the interpretation of 2-D seismic data calibrated by geophysical well logs. We concluded that the AFZ occurs in both onshore and offshore as a brittle deformation zone formed by multiple sets of fractures that originated in the Cambrian and were reactivated mainly as normal faults during the rift phase and in the Cenozoic. In the Campos Basin, the AFZ delimitates the western side of the Corvina- Parati Low, composing a complex fault system with the NE-SW faults and the NW-SE transfer faults. © 2016 Elsevier Ltd. All rights reserved. 1. Introduction During the evolution of rift-drift sedimentary basins, the geological and structural heterogeneities of the basement usually determine the tectonic evolution of the basins, controlling the location of its main depocenters, its subsidence rates and its tec- tonic and sedimentary evolution (Michon and Sokoutis, 2005; Wilson, 2005; Wilson et al., 2006). The development of the basins along the eastern margin of the South American continent are closely linked to the structural framework and crustal heterogeneities inherited from the crystal- line basement (e.g., Schaller, 1973; Ponte and Asmus, 1978; Dias et al., 1987; Guardado et al., 1989; Davison, 1997; Fetter, 2009). . Calegari). The work of Bezerra and Vita-Finzi (2000) and Bezerra et al. (2014) in NE Brazil demonstrates an important influence of the Precam- brian shear zones reactivations on the sedimentation and topo- graphic pattern of the continental margin up to the Quaternary. However, whereas the basement fabric in NE Brazil is orthogonal to the coast and can be easily traced from the onshore to the offshore part of the margin (e.g., Bezerra et al., 2014), in SE Brazil the basement fabric is parallel to the coast. Nevertheless, it is already known that in the SE Brazilianmargin, the Neoproterozoic foliation oriented to NE-SW and NNE-SSW, even being parallel to the coast, does control the geometry of the coastal basins (Ojeda, 1982; Chang et al., 1992). Here, the main and recent question is about the role of the NW-SE and NNW-SSE structures, which probably worked together with the NE-SW arrangement in the configuration of the basins. Some authors (e.g., Novais et al., 2004; Fetter, 2009) affirm that NNW-SSE struc- tures represented by the Colatina Lineament, in Northern of the Delta:1_given name Delta:1_surname Delta:1_given name Delta:1_surname Delta:1_given name http://crossmark.crossref.org/dialog/?doi=10.1016/j.jsames.2016.04.005&domain=pdf mailto:salomaocalegari@hotmail.com http://crossmark.crossref.org/dialog/?doi=10.1016/j.jsames.2016.04.005&domain=pdf www.sciencedirect.com/science/journal/08959811 http://www.elsevier.com/locate/jsames http://dx.doi.org/10.1016/j.jsames.2016.04.005 http://dx.doi.org/10.1016/j.jsames.2016.04.005 http://dx.doi.org/10.1016/j.jsames.2016.04.005 S.S. Calegari et al. / Journal of South American Earth Sciences 69 (2016) 226e242 227 Espírito Santo State, influenced the tectonic evolution of the Cam- pos and Espírito Santo basins. Fetter (2009) considers that NNW- SSE and NE-SW Proterozoic structures are responsible for the control of themain Campos Basins's depocenter, defining basement highs during the rift phase. The author shows a NNW-SSE structural trend as the prolongation of the Colatina Lineament that is pro- jected frommainland to offshore, together with another lineament positioned farther south. The study of this unknown geological feature, parallel to the Colatina Lineament, is the aim of this work. Located in the Southern part of the state of Espírito Santo, this NNW-SSE lineament is awell-marked trace viewed through remote sensing images, which we named here the Alegre Lineament. The Alegre Lineament runs through the entire southern region of the state and its projection into the offshore area reaches major oil fields, such as Enchova and Bonito (Fig.1). On the seabed, the NNW- SSE path of this linear feature is absent, but if one consider the line projection from the land up to the ocean, it will be noted the parallelism of the trace with an inflection of the oceanic slope to- wards the NNW-SSE direction. This inflection is coincident with the projection of the Colatina Lineament to the offshore area (Figs. 1 and 3), raising the possibility that the Alegre Lineament can also be prolonged to offshore, where it could act in the structural control of the offshore basin. In this paper, we used remote sensing, surveying data, seismic, and well data interpretation to show that this feature corresponds to a geological structure that outcrops onshore and extends to offshore up to the Campos Basin. Furthermore, we proposed that this structure acted in both, offshore and onshore, as a set of frac- tures originated in the Cambrian, which reactivated as normal faults during the breakup of the supercontinent Pangea and during the Cenozoic. 2. Geological and structural context 2.1. General features of the Campos Basin and its crystalline basement The crystalline basement of the study area consists mainly of Precambrian rocks (Fig. 1), including highly deformed orthogneiss and paragneiss of Paleo- and Neoproterozoic age, besides Neo- proterozoic to Cambrian granitoids (Silva et al., 2004; Pedrosa- Soares et al., 2007; De Campos, 2014). Siliciclastic Miocene sedi- ments of the Barreiras Formation cover partially the basement along the coast (Rossetti et al., 2013), in addition to quaternary alluvial, colluvial, fluvial and coastal deposits (Silva et al., 2004). Due to its Precambrian structural evolution, the area is well marked by the shear zones of the Late Brasiliano/Pan-African Cycle. These features are NE-SW to NeS straight bands where mylonitic foliation occurs due to dextral and obliquely convergent move- ments (Alkmim et al., 2006; Cunningham et al., 1998). However, the origin and constitution of the NW-SE and NNW-SSE structures of this continental area are not yet established. Silva et al. (2004) and Vieira et al. (2014) ascribe the NW-SE oriented structures to sinis- tral shear zones, or to faults and fractures. The Colatina Lineament (Fig. 1) is represented, in map, as a network of NNW-SSE oriented fractures (Vieira et al., 2014), and some authors (Valente et al., 2009; Novais et al., 2004) discuss the relationship between the dikes that occur along this Lineament and the Cretaceous basalts (Cabiúnas Formation) of the Campos Basin. Despite the absence of studies about the Alegre Lineament, segments of this feature were drawn in some geological maps (Silva, 1993; Vieira, 1997; Vieira et al., 2014), but correlations with outcropping structures were not shown. The oceanic portion of the crystalline basement is under the sedimentary sequences of the Campos Basin, the main oil producer in Brazil (Guardado et al., 2000). This coastal basin covers an area of about 100,000 km2, from which only 500 km2 are emerged (Mohriak et al., 1990). The geological feature known as Vit�oria High borders the Campos Basin to the north, separating it from the Espírito Santo Basin, while the Cabo Frio High is the southern di- visor, separating it from the Santos Basin (Fig. 1; Schaller, 1973; Guardado et al., 2000). Geological records of the Campos Basin show three main depositional environments, with a non-marine clastic sequence, an evaporite sequence and a frankly marine par- alic clastic sequence (Ponte and Asmus, 1978). 2.2. Tectonic and structural evolution of the onshore area The study area is located at the transition between the Araçuaí and Ribeira Mobile Belts, both components of the Mantiqueira Province (Almeida et al., 1981). The boundary between the Ribeira and Araçuaí Belts occurs close to the 21� parallel south (Pedrosa- Soares and Wiedemann-Leonardos, 2000), where the foliation strike inflects from NE-SW (Ribeira Belt) to NNE-SSW and NeS (Araçuaí Belt) (Pedrosa-Soares et al., 2001). The Mantiqueira Province originated from the continental collision of the Brasiliano/Pan-African orogeny that occurred be- tween the Neoproterozoic and Early Paleozoic (Almeida et al., 1981; Heilbron et al., 2000). The Brasiliano/Pan-African orogeny involved subduction of an oceanic lithosphere and the closure of an oceanic basin, with intense tectonism, high-grade metamorphism and granitic magmatism (c. 625 Ma to 570 Ma; Pedrosa Soares et al., 2001). Dextral-transpressive shear zones, such as the Guaçuí, Batatal and Al�em Paraíba (Fig. 1), formed in the final phase of this orogeny, probably in the interval between 560 and 535Ma (Alkmim et al., 2006). Their origin is considered the consequence of a lateral escape to the south after the propagation of the thrust fronts. The last magmatic and deformational manifestations of this orogeny occurred between 530 and 480 Ma (Pedrosa Soares et al., 2011; De Campos et al., 2004; De Campos, 2014; Gradim et al., 2014), with the establishment of theWest Gondwana Supercontinent. After the assemblage of the supercontinent Gondwana, further accretion throughout the Paleozoic and Mesozoic led to the formation of Pangaea. Details about the geological evolution of the Ribeira and Araçuí Belts can be found at Trompette et al. (1993); Pedrosa-Soares et al. (2001), (2007), (2011); Pedrosa-Soares and Wiedemann- Leonardos (2000); Wiedemann et al. (2002); De Campos et al. (2004); De Campos (2014); Heilbron et al. (2000), (2004), (2013); Alkmim et al. (2006), (2007); and Gradim et al. (2014). The fragmentation of Pangaea, initiated in the Mesozoic, defines the configuration of today's continents and oceans (e.g., Brito Neves, 2002; Veevers, 2004; Stampfli et al., 2013; Torsvik and Coock, 2013). The extensional events related to this continental rearrangement shaped the broad outlines of the continental margin of the SE Brazil. After a phase of thermal anomaly during the Jurassic, the rift phase took place in the Early Cretaceous, imposing to this region an extensional regime with NW-SE (Chang et al., 1992) to WNW-ESE orientation between 137 and 122 Ma (Stanton et al., 2010). By the end of the Paleocene and the end of the Oligocene, a NW- SE to NNW-SSE-oriented extensional stress acted in SE Brazil (Hiruma et al., 2010), giving rise to the Continental Rift of South- eastern Brazil (CRSB; Riccomini et al., 1989). Continental sedi- mentary basins, elongated in the NE-SW direction, occur along the CRSB, such as the S~ao Paulo, Taubat�e and Resende Basins in the states of S~ao Paulo and Rio de Janeiro (Riccomini et al., 1989; Almeida and Carneiro, 1998). In the Paleogene sequence of the Taubat�e Basin, Cogn�e et al. (2013) relate a transtensional state of stress with the greatest horizontal stress trending NE-SW, which is in agreement with the proposed by Salomon et al. (2015) to a Fig. 1. Geological framework of the area where the Alegre Lineament occurs and its projection into the oceanic region, where the main Brazilian oilfields are located. Geology simplified from Silva et al. (2004), bathymetry extracted from GEBCO (2013), 30 m ASTER digital elevation model (Advanced Space Borne Thermal Emission and Reflection Radiometer) of ERSDAC (2013), Campos Fault and structural highs from Guardado et al. (2000), oil and gas production fields from BDEP (2013), and shear zones from Alkmim et al. (2006). The main outlined shear zones: G ¼ Guaçuí, B ¼ Batatal, P ¼ Al�em Paraíba. Cities: A ¼ Alegre, CI ¼ Cachoeiro de Itapemirim, CG ¼ Campos dos Goytacazes, Gp ¼ Guarapari, L ¼ Lajinha, V ¼ Vit�oria. States: ES ¼ Espírito Santo, RJ ¼ Rio de Janeiro, MG ¼ Minas Gerais. S.S. Calegari et al. / Journal of South American Earth Sciences 69 (2016) 226e242228 farther south area. For the Neogene and younger times, many controversies remain about the existence of one or more effort arrangements in the SE Brazilian margin. Some authors propose an E-W sinistral strike-slip (Riccomini et al., 1989; Salvador and Riccomini, 1995; Silva and Mello, 2011) and others a transpressional tensor, with the greatest principal axis close to E-W (Cogn�e et al., 2013; Salomon et al., 2015). For Zal�an and Oliveira (2005), the sinistral strike-slip with the minor axis oriented to NW-SE comes from the Paleo- gene up to the Neogene. Younger events would be an E-W dextral transcurrence acting in the Pleistocene, followed by an extensional NW-SE event in the Holocene (Riccomini et al., 1989; Salvador and Fig. 2. Schematic arrangement with the tectonic events proposed by some authors for SE Brazil. S.S. Calegari et al. / Journal of South American Earth Sciences 69 (2016) 226e242 229 Riccomini et al., 1995). Fig. 2 summarize the main tectonic phases proposed by the authors cited here for times from the Early Cretaceous up to the Holocene. The cause of these variations is still an unresolved issue. Some authors argue that the subduction of the Nazca Plate beneath the South American Plate's western side influences the tectonic evo- lution of the SE Brazilian margin (e.g. Salomon et al., 2015; Cogn�e et al., 2013; Cobbold et al., 2001, 2007), generating a plate-wide compressional stress (Cogn�e et al., 2012). Another line thinking consider the westward rotation of the South American Plate about an Euler pole (e.g. Hasui, 1990; Thomaz Filho et al., 2005) located in NE Brazil (Szatmari, 2012) as the generator of tectonic effort over this intraplate region. By the other hand, Zal�an and Oliveira (2005) affirm that the state of stress imposed to the continental margin of SE Brazil in Cenozoic times is due to a gravitational collapse that followed the crustal uplifting caused by the passing of the plate over the Trindade Plume. The remoteness of this area of the heated region would be the responsible for a slightly oblique NW-SE distension that imposed a sinistral transtension from 58 to 20 Ma. The comparison between the Brazilian continental margin and its African counterpart does not solve the question. In the west continental margin of South Africa, Viola et al. (2012) establish a dozen deformational phases from the Precambrian up to nowadays. In the Cenozoic, they found a NW-SE distensional event (after 54 Ma) that was replaced by a NW-SE compression in present days. Nevertheless, Salomon et al. (2015) affirm that the evolution of stress regimes was significantly different in South American and African margins, the first one subjected to compressional stresses (resulting in strike-slip regimes with NE-SW to ENE-WSW compressional axis), and the second one subjected to extensional rifting and flexural bending since the Paleogene. Finally, an important fact that marked the onshore geological evolution of our study area was the crustal uplifting. Several au- thors relate an important uplift process of the Brazilian continental margin during and after the Late Cretaceous (eg. Hackspacher et al., 2004; Hiruma et al., 2010; Karl et al., 2013). Cogn�e et al. (2012) propose an episodic post-rift uplifting, with three accelerated pe- riods of crustal cooling; the first one in the Late Cretaceous, the other one in the Paleogene and the third in the Neogene. This last uplift phase would be accompanied by reactivations of inherited structures, erosion and renewing of the landscape. Jelinek et al. (2014) go further, relating four denudation and cooling episodes since the Permian/Eo Jurassic. According to these authors, a Late Cretaceous-Paleogene denudation occurred in the Mantiqueira Range (that includes part of the study area) possibly due to a thermal-isostatic uplift and magmatic underplating, followed by a Neogene denudation that would be provoked by a more erosive semi-arid climate. 2.3. Tectonic and structural evolution of the offshore area e Campos Basin Lithospheric extensional mechanisms that led to the breakup of the paleocontinent Gondwana and the formation of the South Atlantic Ocean originated the Campos Basin (Milani et al., 2000). Its tectono-stratigraphic evolution, similarly to that of the basins along the continental margin of Southeastern Brazil, is divided into four main phases: pre-rift, rift, transitional and drift (e.g., Cainelli and Mohriak, 1999; Ojeda, 1982). The pre-rift phase represents the intracratonic stage of the su- percontinent Pangea, marked by high rates of crustal uplift and the formation of large peripheral depressions (Cainelli and Mohriak, 1999; Ojeda, 1982). The first lava flows of tholeiitic basalts of the Cabiúnas Formation occurred during this stage (Mohriak, 2012). The rift phase is associated with intense tectonic activity Fig. 3. Location of studied outcrops in the continental area and interpolation area in Campos Basin, showing seismic lines and wells. ES ¼ Espírito Santo State, RJ ¼ Rio de Janeiro State, MG ¼ Minas Gerais State. Fig. 4. Illustration of stratigraphic markers used to define the age of seismic horizons (simplified from Winter et al., 2007). Stratigraphic sequences: 1 ¼ Basement, 2 ¼ Rift, 3 ¼ Post-Rift, 4 ¼ Salt, 5 ¼ Albian, 6 ¼ Cenomanian-Maastrichtian, 7 ¼ Paleocene- Oligocene, 8 ¼ Miocene-Pleistocene, TB ¼ Top of basalts, PNAU ¼ Pre-Neo-Alagoas S.S. Calegari et al. / Journal of South American Earth Sciences 69 (2016) 226e242230 resulting from normal fault stresses in the Early Cretaceous, which produced a system of elongated NE-SW oriented rift valleys sub- parallel to the main structures of the adjacent Precambrian base- ment. This phase developed horsts, grabens and half-grabens delimited mainly by synthetic faults with the same orientation (Dias et al., 1987, 1990). NNW-SSE and E-W striking faults are not so pronounced, but sometimes they control depocenters of the sedi- mentary basin formed during the rift phase (Dias et al., 1990). The Campos Fault or Cretaceous Hingeline is an important normal fault originated in this phase. This regional structure is approximately parallel to the present-day shoreline and dips towards the basin's main depocenter, separating Cretaceous sedimentary units from the shallow basement (Fig. 1; Dias et al., 1990; Guardado et al., 1989). The framework of the Proterozoic basement influenced the main depocenters of the basin during the rift phase, defining tec- tonic blocks delimited by NE-SW and NNW-SSE structures (Fetter, 2009). Cobbold et al. (2001) and Meisling et al. (2001) described a set of NW-SE transfer zones that obliquely segmented the Bra- zilian Southeast passive margin in the Early Cretaceous. These structures controlled variations in the dip of tectonic blocks and the most important accumulation zones of Barremian lacustrine sedi- ments, which formed themain hydrocarbon generating rocks of the Campos Basin (Guardado et al., 2000). The Neocomian volcanism (Mizusaki et al., 1988), which repre- sent the climax of basaltic lava extrusion from the Cabiunas For- mation (Winter et al., 2007), occurred in the rift phase with ages between 112 and 133 Ma (Fodor et al., 1983; Renne et al., 1992). Barremian sediments were deposited soon after, composed by proximal conglomerates and sandstones (Itabapoana Formation), fluvial-lacustrine pelites (Atafona Formation), shales and coquinas (Coqueiros Formation), corresponding to the lower part of the Lagoa Feia Group (Winter et al., 2007; Rangel et al., 1994). The transitional stage represents the early phase of thermal subsidence, marked by the suspension of lithospheric stretching and rifting of the continental crust (Cainelli and Mohriak, 1999). The sedimentary units are mainly composed by conglomerates and sandstones deposited near fault scarps (Itabapoana Formation) and shallow platform carbonates, marl and sandstone (Gargaú and Macabu Formation) covered by evaporites (Retiro Formation) in the upper part of the Lagoa Feia Group (Winter et al., 2007). The drift phase is characterized by minor regional un- conformities and increased thermal subsidence (Ojeda, 1982). Two main marine sequences occur at this stage: one transgressive and other regressive. The marine transgressive phase (Albian-Late Cretaceous) is characterized by the shallowwater carbonates of the Maca�e Group, with sandy (Goitac�as Formation) and calcarenite facies (Quissam~a Formation), which gradate to a sequence of marl and shale (Outeiro Formation; Dias et al., 1990; Mohriak, 2003; Winter et al., 2007). The Tamoios Member (Ubatuba Formation) corresponds to basin shales that mark the end of the marine transgression (Rangel et al., 1994). The marine regression occurred from the Late Cretaceous to the Neogene Period, with the Unconformity, PEU ¼ Pre-Evaporite Unconformity. S.S. Calegari et al. / Journal of South American Earth Sciences 69 (2016) 226e242 231 deposition of siliciclastic sediments of the Campos Group, composed by continental shelf sandstones (S~ao Tom�e Member), continental shelf carbonates (Grussaí Member), and calcirudites and calcarenites (Siri Member), which make up the Emborê For- mation (Mohriak, 2003; Winter et al., 2007). Basin pelites of the Ubatuba Formation (Gerib�a Member) and sandy turbidite deposits (Caraepebus Formation) complete the marine sequence of the Campos Group (Winter et al., 2007). The first record of salt tectonics occurs in the Lower to Middle Albian transition, caused by sediment overload and tilting of the Fig. 5. Characteristics of the studied continental area. (a) Position of the Alegre Lineament an the foliation of the basement framework; (b) near the coast, some sedimentary bodies are co Alegre Lineament (indicated by white arrows). Dikes: LA ¼ Lajinha, IT ¼ Itaici, JM ¼ Jerôni basin, resulting in the formation of salt domes and listric faults (Dias et al., 1990; Mohriak et al., 1990). A new phase of hal- okinetic movement occurred in the Neoalbian, evolving into the formation of growth faults (Dias et al., 1990). The interval be- tween the Late Cretaceous and the Paleocene corresponds to the passive margin period, with continuous subsidence processes and possible residual salt movements (Dias et al., 1990; Mohriak et al., 1990; Cainelli and Mohriak, 1999). The normal faults of the Campos Basin related to salt tectonics generally present a syn- thetic geometry (Mohriak, 2003). Guardado et al. (1989) point d the rosette diagram showing the outstanding NE-SW trend of lineaments that reflects ntrolled by the NNW-SSE lineaments; and (c) basic dikes (white/black circles) along the mo Monteiro, MU ¼ Muqui. S.S. Calegari et al. / Journal of South American Earth Sciences 69 (2016) 226e242232 out that these faults were reactivated from the Albian to the Holocene, playing an important role in the control of sedimen- tation and the formation of traps in the main hydrocarbon ac- cumulations of the Campos Basin. 3. Material and methods The study area is delimited by a polygon drawn around the Alegre Lineament. The continental portion covers a small area in the extreme southeast of the state of Minas Gerais, the entire southern portion of the state of Espírito Santo, and part of the northern region of the state of Rio de Janeiro, whereas the marine portion extends into the central Campos Basin (Fig. 3). The struc- tural analysis involved surface observations through remote sensing data and the acquisition of structural data in the field, and subsurface investigations based on analysis of seismic reflection profiles, in addition to correlation with geophysical well logs. The remote sensing analysis involved the integration of the 30m ASTER digital elevation models (ERSDAC, 2013) and orthophotos (IEMA, 2007) in a GIS environment. We outlined the lineaments manually over the ASTER image by identifying relief-aligned fea- tures, mainly enclosed valleys. The lighting orientation was changed in the software aiming to contrast different line directions and, posteriorly, the distortions of location in lines were corrected, Fig. 6. Gabbroic dikes encountered along the Alegre Lineament, named: (a) LA - Lajinha, (b one by one, using an orto-photo as control. Two interpreters repeated such procedure and only the lines viewed by both were considered, in order to minimize misinterpretations. The field survey included the geometric and kinematic analysis of joints, faults, striations and foliations, in order to correlate the field structures with those observed by remote sensing, as well as cross-cutting relationships between structures. The database of field structures includes 385 outcrops, with 322 foliation data, 1629 joints and 44 fault planes with striae. The foliations and joint measures were grouped into two sets; the first one included all outcrops located at a distance of 0e40 km from the path of the Alegre Lineament (40 km buffer), and the second included the outcrops within 0e3 km (3 km buffer; Fig. 3). The purpose of this divisionwas to search what kind of geological structures acts in the area influenced by the Alegre Lineament and to compare it with the regional background. The field structural data were statistically treated using low hemisphere stereographic projections on a grid of equal area, through the OpenStereo software (Grohmann et al., 2011). The fault data were treated separately in four areas or do- mains for paleotension analysis. The tectonic stress tensor was performed by the inversion of kinematic fault data by Rotational Optimization method using WinTensor v. 5.05 program (Delvaux and Sperner, 2003). The subsurface was analyzed through the structural ) JM e Jerônimo Monteiro, (c) IT - Itaici, and (d) MU e Muqui (see Fig. 5c for location). Fig. 7. Polar stereographic projections of ductile and brittle structures measured in the field, grouped in sets of 40 and 3-km buffers from the Alegre Lineament. (a) Gneissic and mylonitic foliation in the 40-km buffer, and (b) 3-km buffer; (c) joints in the 40-km buffer, and (d) 3-km buffer (low hemisphere projections in grid of equal area; n ¼ number of data). S.S. Calegari et al. / Journal of South American Earth Sciences 69 (2016) 226e242 233 interpretation of 31 2D seismic lines (3051.544 km) and 13 oil wells, whose datawere provided by the National Petroleum Agency (ANP; Fig. 3). The litho- and chronostratigraphic information obtained from the wells, such as unconformities and boundaries between formations (stratigraphy markers; Fig. 3), together with geophys- ical well logs (gamma ray, sonic and density) were used to define the ages of seismic reflectors and the lateral correlation between the lines. Thewells (in depth) were linked to seismic lines (in time), using the interval velocity recorded in the sonic profiles in micro- seconds per foot (ms/feet) for each well. Thus, the top of the basement was calibrated with the top of the basalts (TB) of the Cabiúnas Formation; the top of the Rift sequence with the Coqueiros Formation; the top of the Post-rift sequence with the pre-evaporite discordance (PED); the top of Salt with the Retiro Formation; the top of the Albian with the Outeiro Formation; the top of the Cenomanian-Maastrichtian sequence with the Tamoios Member (Ubatuba Formation); the top of the Paleocene-Oligocene sequence with the Siri Member (Emborê Formation), and the top of the Miocene-Pleistocene sequence with the Seabed (Fig. 4). The seismic horizons of the 31 2-D seismic lines were inter- preted in two-way time (TWT), generating a grid of points for each interpreted horizon. 3-D surfaces were generated for each horizon by interpolation of data (Fig. 3) using the minimum curvature method. The polygon was delimited according to the highest den- sity of seismic lines. Thus, two-way time surfaces were obtained for the top of the: Basement; Rift sequence; Post-rift sequence; Salt; Albian sequence; Cenomanian-Maastrichtian sequence; Paleocene- Oligocene sequence; and the Miocene-Pleistocene sequence. The interpolation of stratigraphic horizons interpreted on seismic sec- tions generated three-dimensional surfaces which, when projected on a map, revealed the structure of the packages. The bottom surface interpolated for each sequence was sub- tracted from the top surface, in order to calculate the interval (in time) of each one. Using themean velocity of each interval obtained from wells, the time intervals were converted into depth (in me- ters). These data were used to construct the isopach maps of the sedimentary packages: Rift sequence; Post-rift sequence; Salt; Albian sequence; Cenomanian-Maastrichtian sequence; Paleocene- Oligocene sequence; and Miocene-Pleistocene sequence. 4. Results 4.1. Structural analysis of surface data The Alegre Lineament is defined by valleys oriented predomi- nantly N25�W, subparallel to the Colatina Lineament (Fig. 1). The aligned feature is identified from the eastern region of the Minas Gerais State to the extreme south of the Espírito Santo State, where it becomes undefined. In this region, we assumed that the Linea- ment shifts towards the east (Fig. 5a), which is inferred by the control that it exerts on the deposition of Cenozoic sediments (Fig. 5b). The coastline in the extreme northeast of the state of Rio de Janeiro is also parallel to this direction, and from there, the feature was inferred to the central portion of the Campos Basin. In Fig. 5c we did not trace the lineaments, in order to permit the reader to observe how the Alegre Lineament is clear and contin- uous in most of the area. In spite of the continuously of the main trace, a set of minor NNW-SSE lines also can be seen, sometimes forming clusters of lineaments that control the shape of drain channels. The rosette diagram (Fig. 5a) shows the predominance of NNE- SSW (N25�E) and NE-SW (N45�W) lineaments, which correspond to the gneissic and mylonitic foliations, which have been studied previously (e.g. Pedrosa-Soares et al., 2011). In the NW-SE quadrant, a less marked set of lineaments appears (N55� to 65�W), but the Alegre set is the less frequent, showing that this feature is not a widespread structure and occurs along a narrow strip. In the northern portion of the continental area, the Alegre Lineament reaches the Guaçuí Shear Zone (560-535 Ma; Alkmim et al., 2006) where becomes ill defined; but, passing this zone, the trace is clear again. This fact could indicate that the shear zone affect or displace the Alegre Lineament, but according to the field data that we show bellow, the studied structure is newer than the mylonitic zone. When crossing the Santa Angelica Intrusive Complex (SAIC; ca. 520-480 Ma; S€ollner et al., 2000), the Alegre Lineament pass be- tween two gabbroic intrusions. This fact would imply that the lineament is a structure formed during the emplacement of these intrusions, but according to recent data of De Campos (2014), the magma segregation of this granitic complex was not affected by tectonic deformation. By the other hand, some sections of the Lineament coincides with the contact between units of the Neo- proterozoic basement and Neoproterozoic granitoids, as indicated on Vieira's geological map (1997). Four gabbroic dikes were identified along the Alegre Lineament (Fig. 5c), and are under study by the team of this work. The dikes called LA, IT, and JM have NW-SE to NNW-SSE strikes, subparallel to the Lineament, and theMU dike is oriented to NE-SW, following the foliation of the host rock. The dike thickness vary from 0.5 to 3.0 m. Cooling fractures are remarkable in LA, JM, and MU dikes (Figs. 6a, b, and d), while the characteristics of IT refer to a deeper emplacement level (Fig. 6c). Mendes et al. (2014) analyzed some of these occurrences, identifying two groups of dikes: an alkaline and a tholeiitic one. The authors describe the existence of at least two dike generations, providing from different magmatic sources dur- ing different tectonic events. Field measures along the whole area (40 km buffer) showed the regional foliation oriented to NE-SW, dipping towards SE (Fig. 7a). The gneissic foliation commonly has an intermediate dip angle, S.S. Calegari et al. / Journal of South American Earth Sciences 69 (2016) 226e242234 while the mylonitic foliation occurs predominantly at a high dip angle, characterizing the shear zones such as Guaçuí and Batatal. When analyzed in the 3 km buffer, the foliations show the same pattern (Fig. 7b), and do not show any relation to the Alegre Line- ament orientation. Families of joints oriented to WNW-ESE and NW-SE are the most frequent in the 40 km buffer, with others oriented NE-SWand NNE-SSW (Fig. 7c). In the set of measurements taken in the 3 km buffer, the joints of the NE-SW quadrant become less representa- tive and the high angle NW-SE family remains, with a WNW-ESE oriented group with intermediate dip angle towards NNE also present (Fig.7d). Faults measured in the field affect weathered rocks of the crystalline basement, and some of them have striations imprinted on infill material composed by Fe and Mn oxy-hydroxides and clay minerals (Fig. 8). These faults occur concentrated in four different areas or structural domains (Fig. 8a). The area I is exactly on the trace of the Alegre Lineament (NNW-SSE), where most of the Fig. 8. (a) Four structural domains where faults affect the weathered and/or lateritic baseme Guaçuí Shear Zone; (d) the area III is near the Itapemirim River; and (e) the area IV with f projection in grid of equal area; n ¼ number of data). normal/oblique faults has the same orientation of this feature and just a few faults is oriented according to the gneissic foliation, which vary between NE-SW and NNE-SSW (Fig. 8b). The area II is on the Guaçuí Shear Zone and the faults have equal orientation to the mylonitic foliation (NNE-SSW) that marks this regional struc- ture. In this area, we also found fault planes with striae marked on Mn oxide pellicle (Fig. 8c). The area III is near the Itapemirim River, the main drainage channel of the region; and the area IV is located farther south, on the Al�em Paraíba shear zone. In the last two areas, oblique/normal faults affect the weathered gneissic basement in an ENE-WSW main trend (Fig. 8d and e). The kinematic inversion of the fault dataset indicated, in the areas I, II, and III, an extensional stress field with the minor axis to NW-SE; and, in the area IV, the extensional axis is oriented to NE- SW (Fig. 9). The foliation's attitude is similar in all of them, varying between NNE-SSWand NE-SW. The joints more frequently occur in the areas I and II, where the Mn oxides commonly appear, indi- cating that these sites had a larger fracturing degree where the nt. (b) The area I is exactly on the trace of the Alegre Lineament; (c) the area II is on the aults affecting the weathered gneiss (stereograms show fault data in low hemisphere S.S. Calegari et al. / Journal of South American Earth Sciences 69 (2016) 226e242 235 rusty material filled the discontinuities before faulting. 4.2. Structural analysis of the subsurface Two predominant structural styles were found: (i) normal faults that affect the Basement and the Rift sequence; and (ii) extensional structures generated mainly by overload of the stratigraphic sequence and salt tectonics that affect the upper sequences (hal- okinetics deformation). Fig. 10 depicts the interpretation of three seismic sections perpendicular to the Alegre Lineament (strike sections; approxi- mately NE-SWdirection), positioned from the portion closest to the shoreline to the distal portion, close to the oceanic slope. Fig. 10a shows faults that delimit a structural high corresponding to the Badejo High, identified earlier by Guardado et al. (2000). Aero- magnetic data reported by Stanton et al. (2010) and Lourenço et al. (2014) show the alignment of a NNW-SSE trending negative mag- netic anomaly separating the Badejo High from the Campos Mag- netic High. Fig. 10b shows high-angle normal faults with apparent displacement in the section of the Alegre Lineament stretching toward the offshore area. These faults comprise a cluster along a stretch of 40 km, controlling a structural low in the NE portion of the basin, which corresponds to the Corvina-Parati Low (Guardado et al., 2000, Fig. 10c). It is important to note that at certain sites in the continental area, the Alegre Lineament also appears in the form of a lineament cluster (Fig. 5c). The occurrence of faults that appear to be linked to the Alegre Lineament is restricted to the proximal and central portions of the basin. However, this correlation cannot be made in the distal sec- tions, as illustrated in Fig. 10c. On the other hand, in this distal section, a structural low appears on the NE side, indicating the action of NW-SE oriented structures, which can be interpreted as a transfer fault. Transfer faults are high dip faults that transfer the displacement between two normal faults, and are approximately Fig. 9. Stereograms of foliations and joints and paleotensors obtained by inversion of fault d quadrant at (a) area I, (b) area II, and (c) area III; in the (d) area IV, the extensional axis is orie s1 ¼ maximum, s2 ¼ intermediate, and s3 ¼ minimum tension axis). parallel to theminor horizontal effort (Gibbs,1984). They are part of the extensional system, working as a balancing mechanism in rifts with different rates of crustal stretching (Harding and Lowell, 1979; Milani, 1990). The identification of transfer faults in seismic sections is based on elements that indicate strike-slip faulting, mainly due to the presence of flower structures (Zal�an, 1986). Indications of strike- slip motion were sought in the interpretation of seismic sections, but of the 31 sections available, only three showed evidence of strike-slip motion. Fig. 10b illustrates a negative flower structure associated with basement faults, which occur in the same position as the transfer faults described in the literature (Cobbold et al., 2001; Meisling et al., 2001; Lourenço et al., 2014). Most of faults that affect the Basement and the Rift sequence is observed in strike sections with apparent dip oriented to NE and in dip sections with apparent dip oriented to SE. The faults in the Basement and Rift sequence are intermediate to high-angle syn- thetic-antithetic faults with apparent normal displacement, which form horsts and grabens. Among the 218 faults that deform the Basement and Rift sequence, 20% also deform younger packages (Fig. 11a). In 14 of the 31 interpreted sections, we identified normal faults that affect the Rift sequence, with apparent normal displacement of about 40 mse300 ms (milliseconds; TWT), and also affect the post-Rift sequence, but with displacement of 10 mse200 ms (Fig. 11b). Such observations indicate the reac- tivation of structures formed during the rift phase. Faults associated with halokinetic processes were identified in 13 of the 31 interpreted seismic sections. These faults, which affect the base salt level and continue as far as the Miocene-Pleistocene sedimentary unit, are predominantly synthetic faults (Fig. 11c). The halokinetic deformation aremostly visible in the strike sections with an apparent intermediate dip angle oriented to NE. In dip sections, these faults occur with apparent SE-oriented dip. Although the strike of these faults occurs in the same direction as ata in different structural domains. Fault data indicate extensional effort in the NW-SE nted to NE-SW (low hemisphere projections in grid of equal area; n ¼ number of data; S.S. Calegari et al. / Journal of South American Earth Sciences 69 (2016) 226e242236 the rift phase faults, the processes whereby they are formed are related to eastward tilting of the basin and to differential sediment compaction after the period of tectonic quiescence (Guardado et al., 1989). However, movements related to the reactivation of rift phase structures associated with halokinetic faults may also occur. Faults that affect only the upper sequences were also observed, with displacements up to 120 ms (Fig. 11a). These are gravitational faults formed in response to theweight of the sedimentary cover on mobile basal levels, as compensation for the sedimentary package. The 3-D surfaces generated by interpolation of the interpreted horizons (Fig. 12) show an outstanding NE-SW structural control of the sedimentary surfaces, with more pronounced control in the region of the oceanic slope. The letter “A” indicates the projection of the Alegre Lineament from the land to the basin. The maps of the Fig. 10. Seismic strike sections selected from the 31 interpreted sections: (a) interpretation o of the 0221e6960 line. 1 ¼ Basement, 2 ¼ Rift sequence, 3 ¼ Post-Rift sequence, 4 ¼ Salt Pleistocene. top of the basement to the top of the Cenomanian-Maastrichtian sequence (Fig. 12h to c) show structural highs on the West side of the lineament and structural downs on the East side. The upper and lower portions are delineated by contours aligned in the NNW-SSE direction, parallel to the lineament. Note, also, the presence of in- flections oriented to NW-SE, suggesting that such structures also control the geometry of the packages. Nevertheless, in the top of the sequences Paleocene-Oligocene and Miocene-Pleistocene (Fig. 12b and a), this pattern is not observed. The isopach maps (Fig. 13) show the variations in sedimentary package thickness indicating depocenters developed since the rift phase. Although some influence of the seismic line positions had influenced in the isopachs outlines, it is possible to note that the distribution of depocenters is controlled by the NE-SW structural f the 0231e1233_A line; (b) interpretation of the SPP992323 line; and (c) interpretation , 5 ¼ Albian, 6 ¼ Cenomanian-Maastrichtian, 7 ¼ Paleocene-Oligocene, 8 ¼ Miocene- Fig. 11. Details of the stratigraphic and structural interpretation of the seismic lines. (a) Normal fault with apparent dip towards NE affects the Basement up to the Cenomanian-Maastrichtian sequence, with differential displacement (yellow polygon), and normal faults with apparent dip to NE affecting only the PaleoceneeOligocene sequence (white polygon). (b) Normal fault with apparent dip towards NE affecting the Basement with a displacement of 260 ms and the Rift, Post-rift and Salt sequences with displacement of up to 30 ms (red polygons). (c) Normal fault with apparent dip towards NE affecting the Salt layer (white arrow). (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.) S.S. Calegari et al. / Journal of South American Earth Sciences 69 (2016) 226e242 237 trend. Another structural control is also observable in the Rift, Post- Rift and Salt sequences (Fig. 13g to e), that show thicker packages in the Easter side of the Alegre Lineament projection (dashed line). An attenuation of the tectonic control occurred during the deposition of the Albian and Maastrichtian-Cenomanian sequences (Fig. 13d and c), when that structural feature seems to be inactive. The Paleocene-Oligocene sequence (Fig. 13b) shows the reactivation of the depocenter controlled by the Lineament, which seems to divide two tectonic domains into the basin. In the Miocene-Pleistocene sequence (Fig. 13a), the depression is completely filled and the accommodation space previously existing is no longer observed, shaping the seabed. Gravitational faults and residual halokinetic movements mark the structural stile of this phase. The integration between the seismic profiles, the structural maps and the isopach maps enabled us to create a schematic panorama of the main structural elements in the central portion of the Campos Basin (Fig. 14). Most of the identified structures are NE- SW normal faults dipping toward SE, which delimit structural highs and lows. We also found NW-SE normal faults dipping to SW and NE (Fig. 14c). The trend NW-SE connects NE-SW fault planes, as well as, reverse dipping NE-SW faults (Fig. 14c). Thus, those NW-SE faults were considered transfer faults (dashed black lines), which can be associated with the transfer faults described by Cobbold et al. (2001), Meisling et al. (2001), Stanton et al. (2010) and Lourenço et al. (2014). Oliveira (2015) also identified NW-SE transfer faults (blue dashed lines) near the shoreline, which sepa- rate various segments of the Campos Fault compounding an ech- elon pattern. In the central region of the study area, we identified NNW-SSE faults positioned on the projection of the Alegre Lineament (Fig. 14c). The NNW-SSE normal faults associated with the Alegre Lineament delimit the Corvina-Parati Low to ENE, with high blocks that give rise to the Cabo Frio High (Fig. 14c). The Corvina-Parati Low coincides in part with the Internal Depocenter of the Campos Basin identified by Fetter (2009). In addition, the NE-SW faults of the Cabo Frio High have terminations in trace of the Alegre linea- ment. Oliveira (2015) showed, besides the displacement of the Campos Fault along NW-SE structures, just one trace oriented to NNW-SSE near the shoreline, which coincides with the our outline of the Alegre Lineament at the same site (Fig. 14c). Also, note that the spatial arrangement of the Campo de Namorado reservoirs (Arienti et al., 1995) is restricted to the NE side of the area of action of the Alegre Lineament. 5. Discussion The integration of the surface and subsurface data reveals that the Alegre Lineament is a set of geological structures that acted as joints and faults during the structural evolution of the Campos Basin and adjacent continental area. Then we will call, from here, this feature as the Alegre Fracture Zone (AFZ). The continental field data show that, although the AFZ cut the ductile framework formed during the Brasiliano/Pan-African orogenic cycle, the outline of this brittle structure affect the con- tacts of some Neoproterozoic gneiss and granitic bodies. Viewed through remote sensing, it seems that the Guaçuí Shear Zone in- tercepts the AFZ outline, but the field data show that the last one is a brittle structure formed after the lateral scape of the orogeny, so after the ductile shear stage. The interaction between these features evidences reactivations of the mylonitic zone posteriorly to the formation of the Alegre structure. Then, we propose that the AFZ discontinuities originated as a set of joints in the Cambrian, in the final phase of the Brasiliano/Pan-African orogenic cycle. We did not find any kinematic indicator that could show lateral motions along this structure in its origin. Nevertheless, the presence of basic dykes along the AFZ indicates that it was a very profound set of fractures or a weakness zone in the crust subjected to extensional stresses. In the northern region of the Espírito Santo State, similar dikes occur along the Colatina Lineament or Colatina Fracture Zone (CFZ; Bel�em, 2014). One of these bodies was dated as Jurassic in age (Silva et al., 1987) and its formation was associated with the basaltic overflow of the Cabiúnas Formation into the Campos Basin (Valente et al., 2009; Novais et al., 2004). However, dating from zircon (UePb) performed in basic dikes subparallel to the CFZ attributed these intrusions to the Cambrian (Bel�em, 2014). The dikes of Southern Espírito Santo are currently being dated by the team of one of the authors of this paper. So far, what can be stated is that the presence of these dikes along the AFZ indicates that this belt was subjected to extensional stresses during more than one tectonic pulse. In the Early Cretaceous, beginning of the Atlantic Ocean open- ing, the pre-existing NE-SW to NNE-SSW foliation worked as weakness zones that controlled the coastal basin development. In the Campos Basin, these structures were reactivated forming NE- Fig. 12. Structural contour maps (TWT) showing the top surface of: (a) the Miocene-Pleistocene sequence; (b) the Paleocene-Oligocene sequence; (c) the Cenomanian- Maastrichtian sequence; (d) the Albian sequence; (e) the Salt; (f) the Post-rift sequence; (g) the Rift sequence and (h) the Basement. (A ¼ projection of Alegre Lineament). Fig. 13. Isopach maps of the sequences: (a) Miocene-Pleistocene; (b) Paleocene-Oligocene; (c) Cenomanian-Maastrichtian; (d) Albian; (e) Salt; (f) Post-rift; (g) Rift. In (h) we show the location of the seismic lines and wells used for interpolating data. (A ¼ projection of Alegre Lineament). S.S. Calegari et al. / Journal of South American Earth Sciences 69 (2016) 226e242238 SW normal faults, in response to the generally NW-SE extensional processes of the rift phase as described by various authors (e.g., Schaller, 1973; Dias et al., 1987, 1990; Guardado et al., 1989; Chang et al., 1992; Stanton et al., 2010). The configuration observed in the S.S. Calegari et al. / Journal of South American Earth Sciences 69 (2016) 226e242 239 offshore structural map (Fig. 14) results from a normal fault system that produced NE-SW elongated grabens, controlled by the main structures of the Precambrian basement. This NE-SW control was also important during the Cenozoic, which is highlighted by Schaller (1973) who describes onshore NE-SW normal faults delimiting deposits of the Barreiras Formation and Quaternary sediments of the Campos Basin, obliquely segmented by NW-SE striking faults. The NW-SE faults mapped in our work (Fig. 14) are considered transfer faults, in agreement with Cobbold et al. (2001), Meisling et al. (2001), Stanton et al. (2010) and Lourenço et al. (2014). A set of NW-SE transfer faults affects the Campos Fault and dislocates the NE-SW trace in various stepped segments (Oliveira, 2015). These faults, originated also in the Early Cretaceous, transect the passive margin obliquely and control the main depocenters of the Barremian sedimentary unit, which are responsible for most of the oil accumulations in the Campos Basin (Meisling et al., 2001; Guardado et al., 1989). In this phase, the AFZ acted as NNW-SSE normal faults in part of the Campos Basin, controlling the estab- lishment of the Corvina-Parati Low, where the NNW-SSE faults comprises a complex system together with the NE-SW fault set and the NW-SE transfer faults. In addition to the NW-SE transfer faults, the AFZ also dislocate the Campos Fault along the shoreline in the Fig. 14. Characteristics of the continental portion of the study area. (a) Fault planes identified of the Campos Basin, (c) Map of the main structural elements of the central region of the displaced along NW-SE transfer faults (blue dotted lines; data compiled from Oliveira, 201 ERSDAC (2013). (For interpretation of the references to colour in this figure legend, the rea North of Rio de Janeiro State (Fig. 14). In the continental area, we did not encounter temporal markers indicating how the behavior of the AFZ was during the rift phase. The majority of the observed faults affect the weathered basement or some lateritic material that we consider newer than the strong uplift that occurred in the region after the rift phase as related by some authors (e.g. Jelinek et al., 2014; Cogn�e et al., 2012). The in- crease in thickness observed in the Paleocene-Oligocene sequence of the Campos Basin (Fig.13b) reflects this uplifting, which probably affected a large area of SE Brazil, culminating in intense erosion of the continental area and significant increase in the input of sedi- ments to the adjacent marginal basins (Hackspacher et al., 2004; Hiruma et al., 2010). The faults registered in the onshore area, affecting the weath- ered and/or lateritic filling material, indicate reactivation of pre- existing structures. Probably, the preexisting discontinuities belonging to the AFZ assimilated the tectonic movements and reactivated the fracture planes as NNW-SSE normal faults. The same concept can be used to explain the brittle structural pattern that we found in the Guaçuí Shear Zone, where weathered and lateritic material over NNE-SSW discontinuities shows fault stria- tions. Various researchers highlighted the important role of older structure reactivations in the NE and SE Brazilian continental in 2D seismic section, (b) Map of the total sedimentary thickness of the central portion Campos Basin. The solid blue lines represent the slopes of the Campos Fault, which is 5). Bathymetry extracted from GEBCO (2013), 30 m ASTER digital elevation model of der is referred to the web version of this article.). S.S. Calegari et al. / Journal of South American Earth Sciences 69 (2016) 226e242240 margin (e.g. Bezerra and Vita-Finzi, 2000; Bezerra et al., 2014; Cogn�e et al., 2012; Gontijo-Pascutti et al., 2010). Then, we consider that the faults whose analysis generated the paleotensors showed in Fig. 9 are young faults, dating from the Neogene or less. Although the data fault indicate, in the areas I, II and III, a NW-SE distensional event (Figs. 9a, b, and c), it is possible that this local state of stress is a consequence of a different tensor arrangement acting regionally. According to previous researchers (Riccomini et al., 1989; Salvador and Riccomini, 1995; Silva and Mello, 2011), a sinistral transcurrent and a NW-SE distensional tectonic event acted in the SE Brazil, respectively, in the Neogene and Quaternary. Both of them have the minor tension axis in the NW-SE quadrant and such state of stress could generate the set of faults that we observed onshore. In spite of the local arrangement of faults encountered in the area IV (Fig. 9d) indicates a NE-SW distension, these structures are compatible with the dextral strike-slip tensor that acted in the Pleistocene according to some authors (Riccomini et al., 1989; Salvador and Riccomini, 1995; Silva and Mello, 2011). Another possibility is that these faults were generated by the gravitational collapse proposed by Zal�an and Oliveira (2005), which would generate a sinistral transtension with the minor axis ori- ented to NW-SE between 58 and 20 Ma. Analyzing these findings carefully, it is necessary to point out the observation of Bezerra and Vita-Finzi (2000) who, studying reactivated structures in NE-Brazil, affirm that the maximum hor- izontal axis recovered from reactivated structures can be quite different of the paleotensor acting regionally. Therefore, observing the structural data of continental area, we can only affirm that, from the Neogene, the AFZ was activated as a set of normal faults, sub- jected to a local tension relief. 6. Conclusions Based on the structural analysis performed in this study, allied to the information available in the literature, we concluded that: a The Alegre Lineament reflects a regional fault, that we named here as the AFZ. This geological structure acted both onshore and offshore, along an almost continuous line of approximately 250 km in length. b Onshore, the AFZ is identified as a set of NNW-SSE oriented fractures formed by extensional effort in the Early Cambrian, which were reactivated as normal faults during the Cenozoic, probably in the Neogene and Quaternary. We did not find temporal markers indicating how the behavior of the AFZ was during the rift phase. c Offshore, the NNW-SSE fault system associated with the Alegre Lineament acted in the generation of the Corvina-Parati Low during the rift phase up to the final Aptian, with reactivations in the Paleocene. This system comprises a complex arrangement of faults with the NW-SE transfer faults and the NE-SW faults. Acknowledgments We acknowledge CAPES (Brazil's Federal Agency for the Support and Improvement of Higher Education) for the scholarship granted to the first author, FINEP (Brazil's Research and Projects Financing Agency) for its financial aid to cover the fieldwork (under Agree- ment No. 01.10.0808.00), and the National Petroleum Agency (ANP) for providing the 2-D seismic sections and well logs. We are also grateful to Prof. Francisco Hil�ario Bezerra, Giulio Viola and the third anonymous reviser of SAMES, who greatly contributed to the improvement of this work. Appendix A. 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Introduction 2. Geological and structural context 2.1. General features of the Campos Basin and its crystalline basement 2.2. Tectonic and structural evolution of the onshore area 2.3. Tectonic and structural evolution of the offshore area – Campos Basin 3. Material and methods 4. Results 4.1. Structural analysis of surface data 4.2. Structural analysis of the subsurface 5. Discussion 6. Conclusions Acknowledgments Appendix A. Supplementary data References