Brief overview of the structural expression and influence of the principal transverse crustal lineaments across the South American Plate.  (Numbers of crustal lineaments correlate with regional geohistory chart for the Sub-Andean basins presented in Part 1 (Jacques in press; Fig. 4) and Figure 2.  Numbers in blue squares link lineament-controlled geological phenomena described in this table to Figure 2a & b.)

Transcrustal Fracture System	Tectonic Domain	Structural Expression in the Andean Region and Regional Extent	Influence across the South American Continent	

1.
ENE Tumbes /Guayaquil - Tacutu Tectonic Lineament	

Separates Northern and Western	

Defined by a major change in strike of the structural geometry of the Sub-Andean Fold and Thrust Belt (NNE) into the Talara and Progreso Basins (NW).  This change in strike is defined by the NW-SE trending Progreso Basin of Neogene age 1.1; an extensional basin bounded by two major NW-SE-trending fault systems (Chongón-Colonche and La Cruz Faults; see Jaillard et al. 1995) developed at a high angle to subduction.
It forms a major boundary between the northern volcanic zone of the Northern Andes (Jordan et al. 1983), and the “flat-slab” segment of the Nazca Plate that occurs at 2°S Fig. 2a (Part 1).  It correlates with the northernmost extent of thin-skinned deformation within the Santiago and Huallaga Belts of Peru (Sub-Andean Ranges) Fig. 2b (Part 1).  North of the tectonic lineament, the Cordillera of the northern Andes is represented by three mountain ranges Fig. 2b (Part 1): the Western (accreted arc terrane), Central and Eastern (“ancient and modern” fold-belts, respectively) Cordilleras (Cooper et al. 1995).  The Middle and Upper Magdalena Valley Basins separate the Eastern and Central Cordilleras, and the Cauca Valley divides the Western and Central Cordilleras.
The Tumbes/Guayaquil-Tacutu Tectonic Lineament may define the northern limit of two major intra-basinal basement arches, the Aguaja High-Contaya 1.2 and Iquitos 1.3 Arches, which extend southwards across both the Maranon and Acre Sub-basins of the Oriente Basin.  In the north, this basement lineament may define the southern limit of the Vaupes Shelf 1.4 and the NW-trending Vaupes Arch 1.5.  This lineament appears to extend across the entire width of the continent.	May form a long-lived terrane boundary, separating predominantly continental crust in the south (Peru) from a combination of oceanic and ‘exotic’ continental crust (Tertiary and older terranes) in the north (Ecuador and Colombia; see Noble et al. 1997; Jaillard et al. 1995).  This may explain important differences in geodynamic evolution seen among the Neogene intermontane basins of Peru and Ecuador (Marocco et al. 1995).
This crustal lineament coincides with the southern boundary of the Ecuadorian Block, which constitutes the southern corner of the triangular-shaped Andean Block, instrumental in accommodating deformation at the triple junction between the Nazca, South American and Caribbean Plates (see Jaillard et al. 2000).
Crossing the Oriente Basin, its trace coincides with the ENE-trending Tumbes-Guayana Megashear of Shepherd and Moberly (1981).  Buried beneath Quaternary cover, it has been suggested that this tectonic lineament displaced the continental margin by around 200 km.
In the Oriente Basin, a large number of Cretaceous igneous bodies are aligned ENE along the trace of the lineament.  Their age distribution and geochemistry strongly suggest that they are associated with an “intracontinental hot spot” (Barragan et al. 1997).  Moving eastwards across the Precambrian ortho- and para-gneisses, metasediments and amphibolite schists (aged between 4000 and 7000 Ma) of the Guayana Precambrian Shield, two sets of basement fabric are recognized, ENE-WSW and NW-SE, producing a network of tectonically-defined crustal blocks.  In this area, the Tumbes/Guayaquil-Tacutu Tectonic Lineament clearly delineates the southern extent of the NW-SE-trending Uafaranda Graben 1.7, and Suapure-Mavaca 1.6 and Labarejuri Valley Rifts 1.8.  The ENE-trending Sierra Unturan Fault System 1.9 defines it at the surface, extending eastwards as an anastomosing network of mega-fractures into the ENE-trending Tacutu Graben Basin (North Savannas Rift Valley) 1.10 (see Eiras & Kinoshita 1990).  This Mesozoic intracontinental, asymmetric graben system, is over 300 km long, 30-50 km wide and contains >7 km of Jurassic to Quaternary sediments.  Its origin has been linked to differential rotation in the Guayana Shield during South Atlantic opening and may mark the position of an aborted triple junction (Gibbs & Barron 1993) that could have been generated by a mantle plume during the Palaeozoic (see Schmitz et al. 2002).  It has also been suggested that the Tacutu Graben Basin occupies an ancient Precambrian shear zone within the heart of the Guayana Shield (Crawford et al. 1985).  From here the crustal lineament appears to have controlled the position of a major ENE-trending basement high (Bakhuis Horst) 1.11 before it cuts across the coastal Guyana Basin.	

2.
ENE Solimões - Amazonas Megashear
(Diffuse zone of deformation)	

Western	

The northern margin of this broad zone of deformation (possibly up to 150 km wide) may be represented by a major change in strike of the Andean Fold and Thrust Belt: the Huancabamba Deflection/Bend Fig. 2b (Part 1) (Gansser 1973), from north to northeast in the north, to northwest in the south.  The Huancabamba Deflection appears to have sinistrally displaced the axis of the Maranon Sub-basin by 100-150 km.
Where the centre of the Solimões-Amazonas Megashear intersects with the Andean Belt, there is a dramatic switch in the predominance of one deformational style over another.  In the north, a wide thin-skinned belt is prevalent across the Santiago and Huallaga Basins, whereas, to the south, this style of deformation only forms a very thin belt along the western margin of the Ucayali Basin, giving way to a wide zone of basement thrusting in the central belt  Fig. 2b (Part 1).
Shear system appears to be transcontinental, extending across the entire width of the South American continent.  It represents a very broad zone of deformation, possibly 100-150 km wide.	Referred to by some workers as the Amazon Shear or Solimões Megashear Zone, it has been suggested to have controlled rifting and magmatic activity during the latest Proterozoic to earliest Palaeozoic (e.g., Szatmari 1983) and intraplate deformation zone active during the Jurassic to Cretaceous (e.g., Caputo & Silva 1990, Burke & Lytwyn 1993).  Along a considerable length of the basement lineament (approx. 2750 km and 450-500 km wide) are the ENE-trending Phanerozoic Solimões (Upper Amazon) and Amazonas (Middle and Lower) intracratonic sag basins.  The Solimões Megashear may have tectonically controlled the position of several elongate ENE rift grabens associated with a widespread Palaeozoic sag event (see Neves 1990).  These basins contain sediments of Palaeozoic (Ordovician-Carboniferous), Late Cretaceous and Tertiary age.  The northern and southern limits of both basins are the Guayana and Brazilian Precambrian Shields, respectively.  The western limit of the Solimões Basin is taken as the Iquitos Arch 2.1, separating it from the Sub-Andean Oriente (Acre Sub-basin) Basin.  The influence of NW-SE deep crustal faults throughout the Amazon region is demonstrated by the presence of several major basin-bounding and intrabasinal highs: Purus 2.2, Carauari 2.3, Monte Alegre 2.4 and Gurupá 2.5 Arches.
Within both the Solimões and Amazonas Basins, Late Jurassic to Mid Cretaceous dextral transpressive deformation along the Solimões-Amazonas Megashear may have been responsible for the development of an ENE-WSW-trending, 1000 km long, fault and fold system through the centre of the two basins (e.g., Caputo & Silva 1990).  Positive flower structures have been identified in seismic section and, in outcrop, en echelon folds and hanging-wall anticlines associated with reverse faulting have been observed.
In the Amazonas Basin, Early Jurassic igneous activity has been attributed to hot spot activity (Aires 1985).  The track of its position through time remains controversial (Wilson 1997) but, in the light of the close proximity of such activity to these deep crustal lineaments (see below), it may have been preferentially sited along a lithospheric weak zone associated with the Solimões-Amazonas Megashear
At the Atlantic coastline, the tectonic lineament coincides with the aborted Triassic-Jurassic Marajó Rift (Gurupá, Mexiana and Limoeiro grabens) of the Foz do Amazonas Basin.  It has been suggested that during the Mesozoic this crustal lineament was intimately associated with movements along the Benue shear system in central west Africa.  Referred to as the “Equatorial Atlantic Megashear”, it may have formed part of a global sytem (Pelusium Line) that extended across South America, Africa and into Asia (Neev et al. 1982).	

3.
ENE Pisco /Abancay - Fitzcarrald Tectonic Lineament	

Separates Western and Central	Major change in orientation of the Andean Fold and Thrust Belt: the Abancay (Pisco) Deflection Fig. 2b (Part 1) (Ham & Herrera 1963; Marocco 1971).  It also appears to define the southern limit of thin-skinned thrusting associated with the Santiago and Huallaga Belts of the Sub-Andean Range and foreland basement thrusts of the Shira Uplift Zone Fig. 2b (Part 1).  Its position roughly coincides with the Urubamba offset of Roeder and Chamberlain (1995), where an approximate 50 km offset of the Sub-Andean Belt occurs.
It is interesting to note that its continuation offshore closely coincides with the position and orientation of the Nazca Ridge Fig. 2a (Part 1).  It is possible that this basement fracture system defines the southern edge of the Solimoes deformation zone, represented at surface by the ENE to NE trending Fitzcarrald Arch 3.1 (discussed above), which separates the Oriente and Ucayali Basins from the Madre de Dios Basin.	
During the Triassic and Jurassic, this structure marks a fundamental change in subsidence rates along the Andean Belt.  To the north, the Pre-Andean Retro-arc Extensional (I) Megasequence occurs between the Fitzcarrald Arch and the Tumbes/Guayaquil-Tacutu Tectonic Lineament Fig. 4 (Part 1), whereas, to the south, in the Madre de Dios and Beni Plain Basins, throughout this time-span sediments were either not deposited or have been subsequently removed by uplift and erosion.  The southern boundary of this tectonic domain is defined by the Boomerang Hills uplift zone, which may again represent the surface expression of an ENE-trending transcontinental fault (see below).  This tectonic lineament may define the boundary between the Amazonas and Tapajós Basins 3.2.	

4.
ENE Arica - Paraguai-Araguaia Tectonic Lineament	

Central	

Dramatic change in trend of the Andean Deformation Zone, from approximately N-S in northern Chile, to NW-SE in southern Peru: Arica Bend/Deflection or Santa Cruz Elbow or Bolivian Orocline Fig. 2b (Part 1) (e.g., Sonnenberg 1963).  Two major transverse structures occur in the vicinity of the Arica - Paraguai-Araguaia Tectonic Lineament: the ENE-trending Cochabamba Fault Zone and a NE-SW-orientated diffuse zone of deformation (approx. 90 km wide) referred to as the Padilla Zone.  These transverse structures define the southern and northern terminations of the Northern Bolivian and Southern Bolivian/Argentinian Sub-Andean thin-skinned belts, respectively (Kley 1999).  The former structure clearly accommodated sinistral displacements during the development of the Bolivian Orocline, as indicated by the formation of pull-apart basins and earthquake foci (Dewey & Lamb 1992).  Combined with dextral movements on the Padilla Zone, this may have produced a triangular central block, which moved parallel to the direction of convergence (see Kley 1999).  The Arica - Paraguai-Araguaia Tectonic Lineament marks a clear increase in the width of thin-skinned deformation from the two Sub-Andean ranges (Beni Plain and Santa Cruz Basins) Fig. 2b (Part 1).

The Cochabamba Fault Zone essentially terminates in the Boomerang Hills Oblique Lateral Ramp System 4.1 (see Welsink et al. 1995a), which directly coincides with the trace of this crustal lineament.  This deformation belt essentially separates the Beni Plain Basin from the Santa Cruz Basin and can be traced a long distance eastwards across the continent (see opposite).	During Mesozoic crustal shortening along the western margin of South America, this pre-existing crustal fault system separated counterclockwise crustal block rotations in the “Peruvian Block” from clockwise rotations in the “Chilean Block” Fig. 2b (Part 1) (see Scanlan & Turner 1992 and references therein) — Central Andean Rotation Pattern (CARP) of Somoza et al. (1996).  Palaeomagnetic data (e.g., Mitouard et al. 1990, MacFadden et al. 1990, Macedo-Sánchez et al. 1992, Beck et al. 1994) suggest that the average magnitude of rotation of the two “oroclinal” limbs of the Arica Deflection were roughly symmetrical and between 15 and 20°.  Kinematic modelling and crustal shortening estimates from balanced cross sections may indicate lower regional rotations in the order of 5-10° (e.g., Kley 1999).  For counterclockwise and clockwise rotations to occur simultaneously, sinistral shear would have to occur to the north and dextral shear to the south, of the Arica Deflection (e.g., Beck 1998, Scanlan & Turner 1992).  Although often referred to as the “Bolivian Orocline”, most workers today except that this feature is not an orocline in the sense of Carey (1958; see discussion by Sheffels 1995 and review of “block rotation” models by Beck 1998) and the Central Andean Belt was never entirely straight (e.g., Dewey & Lamb 1992, Scanlan & Turner 1992), suggesting that the Arica - Paraguai-Araguaia Tectonic Lineament had a profound effect on the original geometry of the plate margin, further enhanced during the Andean Orogeny.  This does raise the question whether these transverse crustal lineaments have an effect on the distribution of oceanic crustal age along the subduction margin and, if so, whether these spatial variations have had an important influence on partitioning slab pull forces.
This lineament has been interpreted as an ancient feature, which may have evolved from a hot-spot generated triple-junction rift system (Fletcher & Litherland 1981).  This failed arm may have once again opened and closed in the Mesozoic, siting the Velasco Alkaline Province Fig. 2a where it intersects with the NW-SE-trending Paraná-Chacos Deformation Zone (see Scanlan & Turner 1992 and references therein).  In this area, the Arica - Paraguai-Araguaia Tectonic Lineament may define the northern margin of the Tocantins Province, a group of Neoproterozoic mobile belts (Tucavaca, Paraguai, Araguaia and Brasília) that were developed along the southern edge of the Brazilian (Amazonia) Craton (see Pimentel et al. 2000).  Representing different crustal units, the tectonic evolutions of the fold belts are related to the Braziliano/Pan-African Orogeny (see Alvarenga et al. 2000).  The ENE-trending Paraguai Fold Belt 4.2 may define the actual trace of the crustal lineament.  A dramatic change in strike from ENE (Paraguai Fold Belt) to NNE (Araguaia Fold Belt), occurs across the basement lineament.  Along this zone is the ENE-trending Xingu Arch, which separates the Proterozoic Parecis and Xingu Basins in the north from the Cenozoic Pantanal and Palaeozoic Paraná Basins in the south.  The lineament defines the southern and northern boundaries of the Xingu 4.3 and Bananal 4.4 Basins, respectively.  Further east, it may form a structural boundary between the Palaeozoic Maranhão and Proterozoic São Francisco Basins, the São Francisco Arch 4.5.  The crustal lineament shows a strong spatial relationship with several Jurassic to Cretaceous alkaline igneous provinces Fig. 2aq, suggesting that it had an important control on the siting of lithospheric mantle melts during the Mesozoic breakup of Gondwana.
Onshore, and extending offshore, along the Equatorial Atlantic margin, the Arica – Paraguai-Araguaia Tectonic Lineament is defined by the ENE-trending, intracontinental graben system of the Potiguar Basin 4.6, a Neocomian rift inherited from the Proterozoic Porta Alegre shear zone.  Parallel to the ENE-trending basin bounding faults is a major dyke swarm related to the initial stages of rift evolution, along a structural trend that continued eastward into the Benue Trough of Nigeria (Milani 1998).  In Matos’s (1999) model for initial Aptian rifting in NE Brazil and West Africa, the Arica - Paraguai-Araguaia Tectonic Lineament may have been an extremely important structure in tectonically controlling his “Transversal Zone”; a giant accommodating structure, orthogonally arranged between the Potiguar-Benue Trough rift system and the Pernambuco Shear Zone (see discussion on reactivated Braziliano and Pan African shear zones and fold belts).	

5.
ENE Michicola Tectonic Lineament	

Separates Central and Southern	Major strike-swing and change in deformation style of the Sub-Andean Fold and Thrust Belt.  It defines the boundary between the Puna and Altiplano segments, which have experienced vastly different shortening histories during the last 10 Ma (Allmendinger & Gubbels 1996).  This change occurs between the Sub-Andean Ranges (Southern Sub-Andean Belt-Santa Cruz Basin) and the Santa Barbara Fold and Thrust System (Northwest Basin); separating thin-skinned deformation in the Central Andes from thick-skinned thrusting characterizing the Santa Barbara System Fig. 2b (Part 1).  It is defined at the surface by the NE-trending Michicola Arch 5.1, separating the Santa Cruz and Northwest Basins.  This arch forms the northern boundary to a major, Cretaceous to Tertiary ENE-trending rift system, the Lomas de Olmedo Trough of the Northwest Basin Fig. 6 (see Mon & Salfity 1995; Comínguez & Ramos 1995) located along the suture between the Amazonia (Brazilian) and Pampia Cratons (Comínguez and Ramos 1995).  Its position may roughly coincide with the seismically active Bermajo offset of Roeder and Chamberlain (1995), where an approximate 50 km offset of the Sub-Andean Belt occurs.
During the Late Devonian to Early Carboniferous, the site now occupied by the Lomas de Olmedo Trough was probably part of the Michicola Arch; a major structural high bounded by ENE-trending lineaments (Salfity et al. 1987).	
A number of smaller-scale lineaments have been recognized along and close to this crustal structure (e.g., ENE-trending Tomasito 5.2, Los Blancos 5.3, Isonza and Aconquija 5.4).  These lineaments localized extension and controlled the distribution of Early Cretaceous volcanism (see Welsink et al. 1995b).
This deep crustal tectonic influence on the siting of igneous activity is again demonstrated by the strong spatial relationship of Mesozoic alkaline igneous provinces along the Michicola Tectonic Lineament in the central part of the continent Fig. 2a & b.  Within this area, the crustal lineament may define the northern limit of the Paraná Craton and, further east, may structurally control the southern termination of the Sao Francisco Basin 5.5.
At the South Atlantic margin, the tectonic lineament correlates exactly with the RRR triple-junction rift system sited at Salvador in the Reconcavo Basin Fig. 2a, at the southern end of the intracratonic Tucano-Jatobá abandoned rift system (e.g., Mohriak et al. 2000).

6.
ENE La Serena - Ribeira Tectonic Lineament	

Southern	

Unclear.  This is possibly because this crustal lineament is of secondary importance, with NW-trending crustal lineaments dominating this tectonic domain.  However, where it intersects with the Andean Belt, it is interesting to note that this is fairly close to the boundary drawn by Mpodozis & Ramos (1989) to separate their tectonostratigraphically distinct segments ‘A’ and ‘B’ at approximately latitude 27ºS.

Several lines of evidence suggest that this structure is transcontinental (see opposite).
This lineament appears to extend a considerable distance across the continent.
	It roughly correlates with the northern margin of the Cuyo Basin and separates the main depocentre of the Northwest Basin from several small sub-basins in the south 6.1.  Further east, it appears to form a very broad basement high separating the Alhuampa and Chaco intracratonic sag basins.  From here, the crustal lineament continues through the centre of the Parana Basin, where it is defined by the ENE-trending Braziliano-Pan African Ribeira Fold Belt 6.2. Defined by such structures as the ENE-trending Jacuntinga and Lancinha-Cubatao Fault Zones, this zone of deformation passes into the southeastern Brazilian Coastal Range.  Within this area, major shear zones of the Ribeira Belt delineate the boundaries between a number of elongate ENE-trending terranes.  One such shear zone is the São Paulo Shear Belt, which extends over 1000 km and is up to 100 km wide (Campos Neto 2000).  In this region, a number of ENE, elongate, east-dipping half-graben basins (e.g., Taubate 6.3, Sao Paulo 6.4 and Resende 6.5) related to South Atlantic opening occur directing along the crustal lineament.  This is also true for the ENE-trending Santos-Rio de Janeiro Dyke Swarm associated with the Early Cretaceous (ca. 130 Ma) Paraná-Etendeka magmatic event.	

7.
NW Martin Garcia Tectonic Lineament	

Southern	

Its position correlates strongly with the southern limit of thick-skinned fold and thrusting within the Santa Barbara System and the northern extent of foreland basement thrusting associated with the Argentinian Sierras Pampeanas Fig. 2b (Part 1).  Within the Andean Belt, the trace of this crustal lineament intersects with the ENE-trending boundary between steep-slab and shallow-slab subduction at 28°S Fig. 2a (Part 1).  To the south, a similar relationship may occur between the NW-trending Valle Fertil Tectonic Lineament and the southern limit of shallow-slab subduction at 33°30´S.  It is interesting to note that these tectonic boundaries roughly define a rectilinear zone characterized by foreland basement thrusting that extends some 400 km into the interior of the plate (the Argentinian Sierras Pampeanas Fig. 2b (Part 1)).
Where this tectonic lineament intersects the Andean Belt, it closely coincides with the boundary drawn by Mpodozis & Ramos (1989) to separate their tectonostratigraphically distinct segments ‘A’ and ‘B’ at latitude 27ºS.
A major transcontinental and oceanic fracture system.	Although not exactly coincident with the trace of this tectonic lineament, the proximity and orientation of an important linear zone of NW-SE deep crustal lineaments (Calama and Olacapato-El Toro 7.1 Lineaments) may suggest that they were intimately related with the Martin Garcia Tectonic Lineament, accommodating variable extension across Patagonia during Late Triassic and Early Cretaceous rifting (see opposite).  Referred to as first-order lineaments by Welsink et al. (1995b; with a second set of lineaments oriented ENE, e.g., Tomasito 7.3, Los Blancos 7.4, Isonza 7.5 and Aconquija 7.6), this set of lineaments define the southern segment of the Altiplano-Puna Plateau; functioning as first-order transfer faults during Cretaceous rifting.  As mentioned by Welsink et al. (1995b), these basins line up en echelon with rift basins across the South American continent, predominantly occurring within a zone between the Agulhas-Malvinas transform (defined here as part of the ‘Gastre-Agulhas Megashear’) and the Martin Garcia High (defined here as part of the ‘Martin Garcia Tectonic Lineament’), leading them to conclude that they are related to the reactivation of the pre-existing structural grain within the Precambrian to Palaeozoic basement of southern South America (Uliana et al.1989).  Using seismic and potential field data, they also conclude that combined with the NW-SE set of lineaments, basin formation was controlled by NE-SW tectonic lineaments.  Many of these rift-bounding faults have been inverted during Andean reactivation.
A clue to the longevity of this crustal fault system may be provided by the NW-SE El Toro Lineament 7.1, which has been suggested to have structurally defined the southern limit of a major Cambrian rift system (see Mon & Salfity 1995) and records a protracted history of strike-slip activity (Salfity 1985).
Onshore, the Martin Garcia Fault Zone 7.3, an important dextral, transcurrent shear system operative during Late Jurassic to Cretaceous rifting (e.g., Tankard et al. 1995), expresses this crustal lineament.  This shear system is likely to represent the southern boundary of the Pelotas Terrane (see Schmidt et al. 1995).  Offshore, on the Atlantic margin, it is defined by the NW-SE-trending Martin Garcia High 7.4, a major basement arch that tectonically defines the northern boundary of the NW-SE-trending Salado Basin (interpreted as a “failed” arm of a rift-generated triple-junction (e.g., Stoakes et al. 1991)); separating it from the Montevideo-Canelones and Punta Del Este Basins.  It may have functioned as an important transcrustal zone of lateral accommodation during Late Jurassic rifting and South Atlantic opening (e.g., Nürnberg & Müller 1991), possibly separating NW-SE graben/rift development (perpendicular to the main rift axis) in the south from “true” passive margin style, coast-parallel rifting (i.e. NE-SW) in the north.

8.
NW Valle Fertil Tectonic Lineament	

Southern	
In the northern part of the Cuyo Basin, the position of this deep crustal lineament is defined by a major fault system over 300 km long.  Referred to as the Sierra de Valle Fértil Fault System 8.1, it has experienced a complex history of reactivation, including extensional, strike-slip and contractional throughout the Phanerozoic and has been an important control on Andean deformation (e.g., Baldis et al. 1984).  This fault system appears to represent part of the boundary (Valle Fértil-Bermejo Suture) between the Precordillera (Cuyania of Ramos et al. (1996) or “Texas Plateau” of Dalziel (1997)) and Pampean (Eastern Sierras Pampeanas) Terranes (see v. Gosen 1998; and references therein).  A postulated Mid Ordovician collision boundary (e.g., Astini et al. 1995), the reactivation of this weak zone during the Carboniferous to Permian resulted in the development of NNW-oriented transtensional pull-apart basins of the Guandacol depocentre (see Fernandez-Seveso & Tankard 1995).
A tectonic boundary between a foreland basement thrusting domain in the north (Sierras Pampeanas; see above) and thin-skinned deformation in the south (Argentinian Precordillera) Fig. 2b (Part 1).
Appears to extend across the entire continent and may form a broad inter-basinal high on the Atlantic margin.	It may structurally define the southern boundary of the Chaco Basin, separating it from the San Luis, Leboulaye/Lavalle and Macachin Basins to the south.  Further Southeast, the lineament is likely to pass into a very broad zone of deformation and uplift (ENE-trending S. Ventana Fold Belt 8.2) bounded by two major ENE-trending basement arches (e.g., Tandil High Fig. 2b).  This is coincident with the Tandilia Lineament, which has been interpreted as representing a major Neoproterozoic accretionary boundary (Ramos 1988b; Brito Neves & Cordani 1991; see Tankard et al. 1995).  This deformation zone essentially separates the NW-trending Salado Basin from the NW- to E-W-trending Colorado Basin (both interpreted as “failed” arms of rift-generated triple-junctions created during South Atlantic opening (e.g., Stoakes et al. 1991)).  Prior to their development, the Valle Fertil Tectonic Lineament may have controlled the position of the Claromecó Basin, an onshore NW-SE-trending Carboniferous to Permian basin developed between the NW-trending Tandil High and the Sierra Ventana (Sierras Australes) Fold and Thrust Belt.
The position of the Valle Fertil Tectonic Lineament roughly coincides with the northern limit of NW-trending Late Triassic to Early Jurassic extension.  Tectonostratigraphically, this lineament, together with the NW-trending San Rafael Tectonic Lineament (described below), may define a distinct sub-province represented in the Cuyo Basin by the Cuyo Intracratonic Rift and Post-rift Sag Megasequences Fig. 4 (Part 1).	

9.
NW San Rafael Tectonic Lineament	

Southern	The lineament’s position is defined by the San Rafael Uplift 9.1, which forms a broad basement arch between the Cuyo and Neuquen Basins.
Together with the Valle Fertil Tectonic Lineament to the north, this crustal lineament appears to be expressed at the surface by a shear zone system that bounds the Cuyo Basin (see Ramos 2000); an integral part (suture zone boundary) of Ramos et al.’s (1998) Cuyania Composite Terrane.
May define the southern limit of basement thrusting in the Frontal Cordillera and northern boundary to thick-skinned deformation confined to the western flank of the Neuquen Basin Fig. 2b (Part 1).
Coincides with the boundary drawn by Mpodozis & Ramos (1989) to separate their tectonostratigraphically distinct segments ‘B’ and ‘C’ at latitude 35ºS.
Appears to extend across the entire continent and may continue as an oceanic fracture system on the Atlantic margin.	

It represents a tectonostratigraphic sub-province boundary to both the Cuyo and Neuquen Basins.
In the east, it may tectonically separate the Colorado Basin from the Valdez and Rawson Basins Fig. 2b.

Devonian and Carboniferous, and Permo-Triassic acid igneous activity concentrated along this crustal lineament 9.2	

10.
NW Gastre - Agulhas Megashear	

Southern	In central Patagonia, it is represented by the transcrustal Gastre Fault System 10.1: a major shear zone (up to 30 km wide) closely associated with subvolcanic granite emplacement (see Rapela & Pankhurst 1992).  Despite uncertainties about the timing of displacement on the Gastre Fault System, it appears to have been an important structure in accommodating extension (or transtension) and associated crustal block rotations in a wide region of Patagonia during the early stages of western Gondwana breakup (Geuna et al. 2000).  It forms a major intracontinental fracture system separating the Neuquen and Nirihuau Basins and, further Southeast, it may define the northern faulted margin of the San Jorge Basin 10.2 (Tankard et al. 1995), which has been interpreted as a “failed” arm of a rift-generated triple-junction (e.g., Stoakes et al. 1991).  Offshore, it is expressed by the ENE-trending, 2.5-3 km high, submarine Malvinas Falkland Escarpment 10.3, which defines the northern margin of the North Falkland and Falkland Plateau Basins.
Coincides with the southern limit of thick-skinned fold and thrust belt development in the Neuquen Basin and the northern extent of basement thrusting in the Patagonian Cordillera Fig. 14b.
Coincides with the boundary drawn by Mpodozis & Ramos (1989) to separate their tectonostratigraphically distinct segments ‘C’ and ‘D’ at latitude 40º-41ºS.
A major transcontinental and oceanic fracture system.

It marks the northern limit of the Mesozoic to Cenozoic Patagonian batholith.

During South Atlantic opening, this structure is likely to have controlled the position of the Agulhas Fracture Zone, a major transform fault that defines the southern continental margin of South Africa, where five sub-basins of the Outeniqua Basin (Bredasdorp, Southern Outeniqua, Pletmos, Gamtoos and Algoa) form an en echelon NW-SE arrangement, which may suggest that Late Jurassic to Early Cretaceous rifting was intimately associated with transcurrent movements along the bounding Agulhas-Falkland Fracture Zone (e.g., Coward et al. 1999).  The most obvious ridge crest jump in the South Atlantic occurred along the Agulhas Fracture Zone (Nürnberg & Müller 1991).	

11.
NW South Malvinas Tectonic Lineament	

Southern	In southern Patagonia, it defines the northern margin of the Magallanes (Austral) Basin, forming part of a major structural high referred to as the Rio Chico High or Dungeness Arch 11.1.  This broad basement high separates the Magallanes Basin from the San Jorge Basin to the north.  Offshore, it forms an arcuate trace subparallel to the Gastre - Agulhas Megashear and the San Rafael, Valle Fertil and Martin Garcia Tectonic Lineaments to the north.  Expressed by the South Malvinas Fault Zone 11.2, it separates the Falkland Plateau Basin from the South Falkland Basin, and defines part of the northern margin of the Malvinas Basin.
The northern limit of thin-skinned deformation (Patagonian Cordillera) in the Magallanes Basin is defined by this crustal lineament.
An interesting feature is that where this crustal lineament intersects the Patagonian Cordillera it coincides with the Chile Rise-Chile Trench Triple Junction at approximately latitude 46°S.  As has been pointed out by Dalziel (1989), the elevation of the Cordillera diminishes markedly south of latitude 46°S, where the convergence rate of the Antarctic and South American Plates is significantly lower (approx. 2 cm/yr) than that of the Nazca and South American Plates to the north (approx. 9 cm/yr).
Where this tectonic lineament intersects the Andean Belt, it coincides closely with the boundary drawn by Mpodozis & Ramos (1989) to separate their tectonostratigraphically distinct segments ‘D’ and ‘E’ at latitude 49ºS.
A major transcontinental and oceanic fracture system. 	

As with the Gastre - Agulhas Megashear, this structure may have been important in accommodating extension (or transtension) and associated crustal block rotations in a wide region of Patagonia during the early stages of western Gondwana breakup.  Coupled with movements along the Gastre - Agulhas Megashear, this tectonic lineament was instrumental in the Late Jurassic to Early Cretaceous, transtensional development of the Falkland Plateau Basin.

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