2. Regional geologic setting

The N-trending MFTB is constructed principally of Mesozoic–Cenozoic sedimentary and older basement rocks of the narrow, N-trending segment of the northern Neuquén basin system (Figs 1, 2). The Neuquén basin was initiated as a back-arc basin during latest Triassic extension, producing fault-bounded depocentres with N–S-, NW–SE- and ENE–WSW-trending orientations (Digregorio et al. Reference Digregorio, Gulisano, Gutiérrez Pleimling and Minitti1984; Legarreta & Uliana, Reference Legarreta, Uliana and Macdonald1991; Vergani et al. Reference Vergani, Tankard, Belotti, Welsink, Tankard, Suarez Soruco and Welsink1995). Latest Triassic – Early Jurassic back-arc extension was followed by Middle Jurassic – Early Cretaceous thermal subsidence (sag phase), with punctuated inversion events (Vergani et al. Reference Vergani, Tankard, Belotti, Welsink, Tankard, Suarez Soruco and Welsink1995), and subsequent Andean Late Cretaceous – Cenozoic shortening.

Figure 1.

Shaded relief map of the Andes at 33–40°S showing regional tectonic elements (PC – Principal Cordillera; FC – Frontal Cordillera; SR – San Rafael block; Py – Payenia volcanic field; NqB – Neuquén basin) and location of geologic map of the Malargüe fold–thrust belt (box outline, Fig. 2). Extensional faults of Late Triassic – Early Jurassic age (short line segments) in the Neuquén basin are simplified from previous work: south of 36°S (Vergani et al. Reference Vergani, Tankard, Belotti, Welsink, Tankard, Suarez Soruco and Welsink1995), north of 36°S (Manceda & Figueroa, Reference Manceda, Figueroa, Tankard, Suárez Soruco and Welsink1995; Bechis et al. Reference Bechis, Giambiagi, García, Lanes, Cristallini and Tunik2010).

Figure 2.

Geological map of the Malargüe fold–thrust belt showing major structures, E–W traces of cross-sections A–A′ to E–E′ (grey lines, Fig. 5), zones of complex deformation (wavy symbols) and localities (Fig. 3) discussed in the text (after Kozlowski, Baldi & Mancilla, Reference Kozlowski, Baldi and Mancilla1981; Kozlowski et al. Reference Kozlowski, Cruz, Condat and Manceda1989; Bechis, Reference Bechis2009; Turienzo, Reference Turienzo2010).

The MFTB belongs to the Principal Cordillera, the westernmost of the classic morphotectonic zones of western Argentina (e.g. Ramos, Cegarra & Cristallini, Reference Ramos, Cegarra and Cristallini1996). The easternmost morphotectonic zone, the Frontal Cordillera, is defined by the Carrizalito range, a major basement structure that plunges southwards into the subsurface beneath Cenozoic synorogenic strata adjacent to the northernmost MFTB (Figs 1–3). The region is currently situated above a 30°E-dipping segment of the subducted Nazca plate, with the Pampean flat-slab region located ~ 200 km further north (Ramos, Reference Ramos1999). The total E–W distance from the trench to the frontal (external) structures of the easternmost MFTB foothills is in the order of 350 km. Andean magmatism in this region constitutes a complex history of eastward migration, with important late Cenozoic magmatic centres that have sporadically invaded the foreland (Folguera & Ramos, Reference Folguera and Ramos2011) and potential short-lived flat-slab episodes. For example, the Payenia volcanic field (Fig. 1), a < 5 Ma igneous plateau, has been related to asthenospheric influx due to the steepening of the subducted Nazca plate after a proposed cycle of shallow subduction (Kay, Burns & Copeland, Reference Kay, Burns, Copeland, Kay and Ramos2006; Folguera et al. Reference Folguera, Naranjo, Orihashi, Sumino, Nagao, Polanco and Ramos2009).

Figure 3.

Index map of the Malargüe fold–thrust belt (comparable to Fig. 2) showing key topographic, structural and petroleum features, and location of detailed maps (Figs 6, 8). AMA – Arrollo Matancilla anticline; CMF – Cerro Mollar oilfield; CR – Carrizalito range; DS – Dedos-Silla block; EIF – El Infiernillo fault; ESF – El Sosneado oilfield; LBA – Los Blancos anticline; LBTZ – La Brea triangle zone; LLT – Las Leñas thrust; LM – Loma del Medio; LMF – Loma de la Mina oilfield; LVA – La Valenciana anticline; MA – Malargüe anticline; MT – Mesón thrust; PRF – Puesto Rojas oilfield; RAA – Rio Atuel anticlinorium; RA – Rio Atuel; RS – Rio Salado; SA-BB – Sierra Azul-Bardas Blancas; ST – Sosneado thrust; TS – Tristeza syncline.

Large basement-involved structures and a complex array of thin-skinned thrust systems compose the MFTB. The principally N–S orientations of the Andean contractional basement structures closely correlate with the trend of Mesozoic extensional faults (Fig. 1), and half-graben inversion has been proposed as the main mechanism of thick-skinned deformation (Manceda & Figueroa, Reference Manceda, Figueroa, Tankard, Suárez Soruco and Welsink1995). The eastern part of the fold–thrust belt is characterized by large basement-cored antiformal structures and outcropping or shallowly buried frontal thin-skinned thrust sheets (Fig. 2). In the south, south of the Rio Salado drainage, the large basement-cored Malargüe anticline persists for ~ 50 km along strike. In the north, the northward along-strike projection of this basement structure is represented by the Rio Atuel anticlinorium, which exposes a thick pile of Jurassic rocks in its hanging-wall, over a comparable ~ 50 km strike length (Fig. 3). East of the Rio Atuel anticlinorium, the frontal part of the thrust belt is defined by a thin-skinned thrust system involving Cenozoic foreland basin and older strata. The Tristeza syncline is situated above this frontal thrust system, defining a large-scale morphological feature > 50 km in length (Figs 2, 3). Andean E–W shortening calculated in this region is relatively modest, in the order of 15–30 km (Giambiagi et al. Reference Giambiagi, Mescua, Bechis, Tassara and Hoke2012), with ~ 25% shortening values for the frontal part of the thrust belt (Giambiagi et al. Reference Giambiagi, Bechis, García and Clark2008; Turienzo, Reference Turienzo2010). Mean topographic elevations along the MFTB range between 2 and 3.5 km (Giambiagi et al. Reference Giambiagi, Mescua, Bechis, Tassara and Hoke2012).

The region is distinctive in that it preserves a complete record of the Andean foreland basin system, which has been largely exhumed and eroded along most of the Neuquén basin. To the east, the San Rafael block, a low-relief major basement structure oblique to the thrust belt, has been related to foreland uplifts such as the Sierras Pampeanas further north. The San Rafael basement block uplift separates the Neuquén basin from the Triassic depocentre of the General Alvear sub-basin to the east and has been attributed to the proposed Payenia phase of shallow subduction (Folguera et al. Reference Folguera, Bottesi, Duddy, Martín-González, Orts, Sagripanti, Vera and Ramos2015). The San Rafael block may act as an erosional barrier, helping preserve the Cenozoic basin fill from large-scale exhumation related to headward erosion of foreland drainage systems.

3. Stratigraphic framework

The Mesozoic–Cenozoic stratigraphic succession of the Neuquén basin (Fig. 4) was mostly developed on top of Permo-Triassic igneous rocks of the Choiyoi Group, and underlying metasedimentary and low-grade metamorphic Palaeozoic rocks. The widespread Choiyoi Group makes up the bulk of the uppermost mechanical basement, as shown by the thick panels exposed in the Carrizalito range, Dedos-Silla structure, Malargüe anticline, and to the east in the San Rafael block (Figs 1, 2). The Choiyoi Group is composed of extrusive and intrusive acidic to mesosilicic igneous rocks, and associated non-marine clastic deposits. Along the southern termination of the Frontal Cordillera, in the S-plunging Carrizalito range, lower Palaeozoic metasedimentary rocks are intruded and overlapped by Choiyoi Group rocks (Volkheimer, Reference Volkheimer1978; Tickyj et al. Reference Tickyj, Rodríguez Raising, Cingolani, Alfaro and Uriz2009). Mesozoic–Cenozoic basin evolution is recorded by: (1) Upper Triassic to Lower Jurassic rift deposits; (2) Middle Jurassic – Lower Cretaceous sag deposits; and (3) Upper Cretaceous – Cenozoic foreland basin deposits.

Figure 4.

Upper Palaeozoic through Cenozoic stratigraphic charts showing pronounced thickness variations between the Atuel depocentre (west) and the foreland platform (east).

Evidence of earliest basin evolution in the region is locally preserved along the Malargüe anticline, where remnants of Triassic rift-related strata crop out as the Chihuiu, Llantenes and Remoredo formations (Artabe et al. Reference Artabe, Morel, Spalletti and Brea1998). To the north, synextensional deposits recording the early stages of the Neuquén basin development include the Arroyo Malo, El Freno and Puesto Araya formations (Lanés et al. Reference Lanés, Giambiagi, Bechis and Tunik2008). Upsection, the Pliensbachian–Callovian upper part of the Cuyo Group comprises a number of units, including offshore mudstones, marine sandstones and evaporites of the Tres Esquinas, Lajas and Tábanos formations, respectively, whose accommodation was influenced by former rift-related structures. Aeolian deposits of the Callovian Lotena Formation, and carbonates and evaporites of the Oxfordian La Manga and Auquilco formations make up the Lotena Group (Gulisano & Gutiérrez Pleimling, Reference Gulisano and Gutiérrez Pleimling1994). The Lotena and lower units are only present in the west. In the foreland platform to the east, the Kimmeridgian Tordillo Formation onlaps Choiyoi basement, as shown by exploration wells and seismic data (e.g. Giambiagi et al. Reference Giambiagi, Bechis, García and Clark2008; Boll et al. Reference Boll, Alonso, Fuentes, Vergara, Laffitte and Villar2014). The Tordillo Formation is mostly characterized by fluvial and aeolian strata with abrupt lateral thickness changes. The overlying Tithonian Vaca Muerta Formation has marked facies changes from coastal facies in the eastern platform (Legarreta, Kozlowski & Boll, Reference Legarreta, Kozlowski and Boll1981) to thick marine shales with high total organic carbon (TOC) values in the Rio Atuel anticlinorium to the west (Boll et al. Reference Boll, Alonso, Fuentes, Vergara, Laffitte and Villar2014). The thin Valanginian Chachao limestone separates the Vaca Muerta from the Agrio Formation, which also shows facies changes from coastal deposits in the east to offshore marine marls in the west. The Aptian–Albian Rayoso Group contains the Huitrín and Rayoso formations, with mixed clastic, limestone and evaporite facies.

A basin-scale unconformity (the ‘Intersenoniana’ unconformity) separates the underlying succession from the thick clastic deposits of the Neuquén Group. This unit has very coarse facies locally, and thicknesses vary from 900 m in the west to < 100 m in the eastern platform. The Neuquén Group has been interpreted as the oldest stratigraphic unit related to initial shortening and foreland flexural subsidence (Ramos & Folguera, Reference Ramos, Folguera, Spalletti, Veiga, Schwarz and Howell2005; Tunik et al. Reference Tunik, Folguera, Naipauer, Pimentel and Ramos2010; Fennell et al. Reference Fennell, Folguera, Naipauer, Gianni, Rojas Vera, Bottesi and Ramos2015).

The overlying Malargüe Group is composed of the Loncoche, Roca, Pircala and Coihueco formations (Legarreta, Kokogian & Boggetti, Reference Legarreta, Kokogian and Boggetti1989). The Loncoche Formation consists of dark mudstone and is capped by thin limestones of the Roca Formation. The Pircala and Coihueco formations are dominated by mudstone with minor sandstone. Regionally, the Malargüe Group is markedly tabular, with uniform thicknesses in the order of 600 to 700 m.

A protracted regional unconformity, of roughly 20 Myr duration, separates the fine-grained Coihueco Formation (uppermost Malargüe Group) from the overlying coarser Agua de la Piedra Formation and younger units (Horton & Fuentes, Reference Horton and Fuentes2016). The Agua de la Piedra is the first unit that is considered to be an unambiguous synorogenic deposit generated during Andean shortening. Exploration wells indicate a thickness up to ~ 1500 m, with fluvial and subordinate aeolian deposits. Upsection, volcaniclastic debris-flow deposits of the Loma Fiera Formation record proximal volcanic sources and high topographic gradients. This unit grades vertically and laterally into finer and more distal facies of the Tristeza Formation, with thicknesses up to 900 m according to well data, which is overlain by Pliocene and Pleistocene deposits of the Diamante and Los Mesones formations.

4. Structural geology

The MFTB is characterized by large basement structures (Manceda & Figueroa, Reference Manceda, Figueroa, Tankard, Suárez Soruco and Welsink1995; Giambiagi et al. Reference Giambiagi, Bechis, García and Clark2008, Reference Giambiagi, Ghiglione, Cristallini and Bottesi2009; Turienzo, Reference Turienzo2010; Turienzo et al. Reference Turienzo, Dimieri, Frisicale, Araujo and Sánchez2012) and thin-skinned thrusts systems developed both on top of these basement structures and along the eastern thrust front, as revealed by regional map relationships (Fig. 2) and five new E–W cross-sections (Fig. 5). From east to west, the general structural framework includes: (1) a mostly undeformed foreland platform with thin Mesozoic deposits, covered by a thick pile of Cenozoic synorogenic sediments; (2) the S-plunging Carrizalito range of the Frontal Cordillera; (3) a frontal thrust system, including the Sosneado and Mesón thrusts, and a series of smaller blind thrusts; (4) large basement structures of the Malargüe anticline and Rio Atuel anticlinorium; (5) complex thin-skinned structures capping the Malargüe and Rio Atuel basement structures; and (6) a western hinterland region showing a complex array of both thick- and thin-skinned structures.

Figure 5.

E–W structural cross-sections A–A′ to E–E′ of the Malargüe fold–thrust belt at 34.75°S to 35.25°S (see locations in Figs 2, 3).

Figure 5.

(Continued) Palinspastic restorations of cross-sections A–A′ and E–E′.

The structure of the foreland platform is known from extensive 2D and 3D seismic reflection data. Most structures consist of low-displacement basement faults, some of which show subtle inversion due to Andean contractional deformation (Boll et al. Reference Boll, Alonso, Fuentes, Vergara, Laffitte and Villar2014). These basement faults show principally N–S orientations, with additional NE- and NW-striking set orientations, and an origin related to the Triassic–Jurassic extension (Bechis et al. Reference Bechis, Giambiagi, García, Lanes, Cristallini and Tunik2010; Boll et al. Reference Boll, Alonso, Fuentes, Vergara, Laffitte and Villar2014). Along strike to the north, the foreland platform intersects the S-plunging Carrizalito range of the Frontal Cordillera. Structural reconstructions by Turienzo (Reference Turienzo2010) show a thrust fault detached at depths of ~ 10 km, with related basement folding that can be traced to the south into the subsurface.

The easternmost thrust systems include the Mesón, Sosneado and additional smaller-offset thrusts that carry Cenozoic foreland basin strata and underlying, relatively thin Mesozoic units (Figs 2, 3, 5). The large Tristeza syncline is the combined product of these thrust faults cutting upsection to the east, along with the folding in the forelimb of the Rio Atuel anticlinorium (Fig. 3). The surface trace of the Sosneado thrust continues for ~ 60 km in a N–S direction and shows a persistent hanging-wall flat in mudstones of the lower Cenozoic Pircala and Coihueco formations (Figs 2, 5). To the north, the fault progressively cuts down-section along a low-angle lateral ramp, eventually detaching from the Rayoso Group and underlying units (cross-sections D–D′ and E–E′ of Fig. 5). Seismic data and fault geometric reconstructions (Giambiagi et al. Reference Giambiagi, Bechis, García and Clark2008, their fig. 8) suggest that the Sosneado thrust connects at depth with the Rio Atuel basement fault. To the west, the Mesón thrust gains displacement north of the town of El Sosneado, and shows a low-angle hanging-wall ramp cutting the Cenozoic Agua de la Piedra, Coihueco and Pircala formations that merges into a flat in the uppermost Cretaceous Loncoche Formation of the Malargüe Group. Further north, the Sosneado and Mesón thrusts detach from different units, leaving the thick and mechanically resistant Upper Cretaceous Neuquén Group in between.

These structural relationships are consistent with the generation of a large duplex system to the north (cross-section E–E′), which has been largely overlooked in previous work but is outlined in detail below. The interpreted structural reconstruction of this duplex system is based on three main observations. First, geological relationships north of the Tristeza syncline (Fig. 6, Kozlowski et al. Reference Kozlowski, Cruz, Condat and Manceda1989) show a thrust system repeating multiple slices of the Neuquén Group. These thrust slices appear to continue to the south within the Tristeza syncline, but are obscured by overlapping Neogene to Quaternary deposits. Second, the Arroyo Matansilla anticline, west of the Tristeza syncline, shows Upper Jurassic – Cretaceous Mendoza, Rayoso and Neuquén group rocks more than 2.5 km above their regional elevation, but the Neuquén Group exhibits no stratigraphic separation from the overlying Loncoche Formation (cross-section E–E′). Third, the Arroyo Matansilla exploration well encountered four stacked thrust sheets, including the structure of the Arroyo Matansilla anticline. Collectively, the thrust branching relationships deduced from geologic maps (i.e. thrust sheets repeating Neuquén Group slices branching out below the Malargüe Group in the Tristeza syncline), the stratigraphic separation in front of the Arroyo Matansilla anticline, and the existence of repeated thrust sheets at the surface and in the Arroyo Matansilla subsurface support the interpretation of a duplex system with a roof thrust in the Loncoche Formation and horses involving the Neuquén Group and lower units. This duplex system involving Cretaceous rocks is exhumed to the north, affording a down-plunge view from north to south. This interpretation is detailed in geometric reconstructions of section E–E′ (Fig. 5). The reconstruction differs substantially from that of Turienzo (Reference Turienzo2010), along his section S–S′, which interprets the Arroyo Matansilla anticline as being thrust over the Tristeza syncline, despite the lack of stratigraphic separation and the aforementioned constraints.

Figure 6.

Geological map of the region north of Cuchilla de la Tristeza (simplified from Bechis, Reference Bechis2009, after Kozlowski, Baldi & Mancilla, Reference Kozlowski, Baldi and Mancilla1981) showing key relationships along E–W cross-section E–E′ (grey line; Fig. 5). Our interpretation of the northern segment of the Mesón thrust differs from previous maps in that it forms a roof thrust of the Arroyo Matansilla duplex system to the north and west. Thrust sheets (or exhumed horses) repeating panels of the Neuquén Group are buried beneath Neogene to Quaternary deposits of the Sierra del Perdido, but likely have branch lines at depth connecting with the Mesón thrust.

Both the Mesón and Sosneado thrusts are frontal splays of the basement fault system beneath the Rio Atuel anticlinorium (Fig. 5). The Rio Atuel anticlinorium and the correlative Malargüe anticline are the two dominant structures of the frontal basement domain in this region (Figs 2, 3). The Malargüe anticline is breached such that the Permo-Triassic Choiyoi Group is exposed along its core and in the hanging-wall of a large fault splay (Kraemer et al. Reference Kraemer, Silvestro, Achilli, Brinkworth, McClay, Shaw and Suppe2011). Along strike to the NNW, the Rio Atuel anticlinorium exposes Lower Jurassic units, but no Choiyoi basement rocks. The basement fault carrying the Rio Atuel anticlinorium has been referred to as the La Manga fault (e.g. Giambiagi et al. Reference Giambiagi, Bechis, García and Clark2008); however, we prefer to match the fault name with the transported hanging-wall block (i.e. Rio Atuel fault). In this scheme, the exposed La Manga and Arroyo Blanco faults (Giambiagi et al. Reference Giambiagi, Bechis, García and Clark2008) within the Loma del Medio locality represent shortcut splays of the larger Rio Atuel fault.

Debate persists over whether or not the Rio Atuel anticlinorium is produced by Cenozoic contractional reactivation (inversion) of a Mesozoic rift-related structure. Structural models by Turienzo (Reference Turienzo2010) and Turienzo et al. (Reference Turienzo, Dimieri, Frisicale, Araujo and Sánchez2012) neglected inversion tectonics, and instead showed a stacked system of large basement thrust slices. In contrast, Giambiagi et al. (Reference Giambiagi, Bechis, García and Clark2008) proposed models of inverted half-graben structures that fed slip eastwards into the frontal thin-skinned systems, similar to our interpretation. Subsurface data provide several critical constraints indicating the presence of synrift deposits in the hanging walls of basement structures, but also reveal important along-strike variations. Whereas subsurface data east of the Rio Atuel anticlinorium show that the Choiyoi Group is covered by a thin panel of Kimmeridgian Tordillo Formation (e.g. Boll et al. Reference Boll, Alonso, Fuentes, Vergara, Laffitte and Villar2014), atop the anticlinorium there is a thick (at least 1500 m) pile of Lower–Middle Jurassic deposits in which wells have not reached the basement (Fig. 5). Part of this thick Jurassic succession consists of coarse fan-delta facies and turbidite deposits, likely associated with syndepositional extensional faults (Lanés et al. Reference Lanés, Giambiagi, Bechis and Tunik2008). In the south, the Malargüe anticline only shows local Triassic rift deposits (Kraemer et al. Reference Kraemer, Silvestro, Achilli, Brinkworth, McClay, Shaw and Suppe2011) and relatively thin Jurassic units; nevertheless, this structure appears to be related to inversion of the Rio Atuel extensional depocentre. A structural map of the top of the Choiyoi Group based on our cross-sections, cross-sections along the Malargüe anticline (Kraemer et al. Reference Kraemer, Silvestro, Achilli, Brinkworth, McClay, Shaw and Suppe2011) and well data from the foreland (Fig. 7) confirms a genetic link between the Rio Atuel and Malargüe antiforms. Our preferred explanation is that both of these basement-involved structures can be related to an extensional fault system that accumulated volumetrically important synrift deposits along the present location of the Rio Atuel anticlinorium and must have tipped out to the south.

Figure 7.

Structural map of the top of the basement (including the Permian-Triassic Choiyoi Group and older rocks), showing the basement–cover interface in metres above sea level, derived from our cross-sections, a cross-section for the Malargüe anticline (Kraemer et al. Reference Kraemer, Silvestro, Achilli, Brinkworth, McClay, Shaw and Suppe2011) and well data.

Our analysis, and past interpretations of seismic data (e.g. Giambiagi et al. Reference Giambiagi, Bechis, García and Clark2008; Kraemer et al. Reference Kraemer, Silvestro, Achilli, Brinkworth, McClay, Shaw and Suppe2011; Boll et al. Reference Boll, Alonso, Fuentes, Vergara, Laffitte and Villar2014), constrain the position of footwall cutoffs for basement (Choiyoi Group) and overlying units, and the deep ramp geometry responsible for the Rio Atuel basement hanging-wall anticline (Figs 5, 7). The position of the autochthonous footwall cutoffs is further constrained by the amount of shortening recorded by structures to the east. The position of these cutoff lines is of importance for potential source rock maturation beneath the Rio Atuel structure, as explained below.

A complex array of thin-skinned structures distinguish the top of the Rio Atuel basement structure. The Puesto Rojas oil field (cross-section A–A′ of Fig. 5) produces hydrocarbons from several horses of a duplex system defined by a lower detachment in the Vaca Muerta shale and a roof detachment in evaporites of the Rayoso Group. The evaporites are tectonically thickened along the front of this shallow thrust system (Ploskiewicz & Gorroño, Reference Ploskiewicz and Gorroño1988; Giampaoli, Ramirez & Gait, Reference Giampaoli, Ramirez, Gait, Kozlowski, Vergani and Boll2005). To the west, complex trailing structures of the Puesto Rojas thrust system are exhumed (Dajczgewand, Reference Dajczgewand2002) (Fig. 5). The eastward extent of this shallow duplex thrust system coincides with marked changes in facies and thickness both in Vaca Muerta and Rayoso deposits, which localize the floor and roof thrusts, respectively. Thick, detachment-prone shales of the organic-rich Vaca Muerta Formation are controlled in turn by greater subsidence due to the Rio Atuel extensional fault system (Boll et al. Reference Boll, Alonso, Fuentes, Vergara, Laffitte and Villar2014). Along the foreland platform, the Vaca Muerta grades laterally eastward into greenish siltstones of more proximal deposystems. A similar trend is expressed within the Rayoso evaporites, which pinch out to the east, and whose deposition seems to have been controlled by the Atuel depocentre. These relationships suggest that the location of the shallow duplex and triangle zone was controlled by facies changes originally dictated by the contrasting Mesozoic subsidence regimes east and west of the rift-related fault system (Fig. 4). Development of this shallow duplex system probably occurred during earlier shortening, before contractional reactivation of the Rio Atuel fault, such that the floor detachment was later lifted and tilted into its present E-dipping configuration (cross-section A–A′ of Fig. 5). Therefore, following its development, the whole duplex system was lifted and exhumed along the Rio Atuel inverted block. Shortening along this shallow thrust system can be linked with growth of the Los Blancos anticline to the west (Fig. 5), a basement-cored inversion anticline (see Manceda & Figueroa, Reference Manceda, Figueroa, Tankard, Suárez Soruco and Welsink1995). Inversion of the Los Blancos structure fed slip eastwards into Jurassic units, with thrusts eventually climbing upsection to shallow levels creating the Puesto Rojas and related duplex structures.

A possible highly exhumed analogue is present ~ 40 km north of Puesto Rojas, in the Loma del Medio area (Fig. 8) west of the Arroyo Blanco. Here, Lower Jurassic Puesto Araya sandstones are in thrust contact with Oxfordian Auquilco anhydrite in the footwall. To the east, near-vertical beds of the Tordillo and Vaca Muerta formations define the eastern flank of the Rio Atuel anticlinorium, which is capped by highly deformed thrust slices of the Huitrín Formation stacked beneath mostly undeformed Rayoso evaporites. These relationships are overprinted by a number of late shortcut faults that omitted sections in an already vertical to steeply overturned panel of deformed strata. This structural scenario is similar to that of the Puesto Rojas field, with the only difference being the younger stratigraphic units involved in the shallow thrust system (i.e. Huitrin rather than Chachao-Agrio formations). In map view, the spatial gap between the thrust trace of Puesto Araya on Auquilco strata and the basal thrust of the stacked Huitrín carbonate slices can be considered a tectonic window. Thus, the Auquilco, Tordillo, Vaca Muerta and the thrust-omitted Agrio formations represent exhumed footwall rocks. The regional importance of this system is that (1) it provides a genetic link to the Puesto Rojas duplex system, over a ~ 40 km strike distance, and (2) it provides important kinematic constraints in that the shallow duplex system must pre-date inversion and uplift of the deep Rio Atuel structure. Although we identify here the kinematic linkage of the frontal exhumed duplex horses with a trailing thrust further west, and the intervening tectonic window, the first recognition of a duplex system later tilted to its current subvertical position belongs to Dimieri, Fortunatti & Nullo (Reference Dimieri, Fortunatti and Nullo2005).

Figure 8.

Geological map of the Loma del Medio area. The major thrust is exposed in two areas, such that the mapped western thrust trace along the Arroyo Blanco matches the eastern thrust trace at the base of Huitrín Formation to the east of Loma del Medio. Closely spaced thrusts involving the Huitrín Formation correspond to an exhumed duplex system with a roof thrust near the contact between the Huitrín and Rayoso formations. The Auquilco, Tordillo and Vaca Muerta formations form a tectonic window in the footwall of this main thrust. Further folding by inversion of the deeper Rio Atuel basement structure produced thinning in its forelimb units, and shortcut splays in an already deformed panel, generating localized stratigraphic omission. Teeth along thrust traces denote the hanging-wall block, not the fault dip or transport direction.

Shortening estimates along our cross-sections (Fig. 5) range from ~ 14.5 km in the south (cross-section A–A′) to ~ 13.9 km in the north (cross-section E–E′). The shortening value for the southern cross-section includes the Los Blancos anticline, duplex structures of the Puesto Rojas area, and the Rio Atuel anticlinorium and structures along its front. The northern cross-section involves the Rio Atuel anticlinorium and all structures along its front. Calculated shortening values are remarkably similar to those presented by Giambiagi et al. (Reference Giambiagi, Bechis, García and Clark2008) near our cross-section C–C′ and by Turienzo (Reference Turienzo2010) near our northernmost cross-section E–E′ (Fig. 5).

Two distinctive characteristics of the inverted basement structures of the MFTB are noteworthy. First, these structures all have steeply dipping forelimbs that are in the order of 4 km of structural relief (Fig. 5). This geometry is uncommon in many inversion structures, which tend to form the classic harpoon shapes (e.g. Williams, Powell & Cooper, Reference Williams, Powell, Cooper, Cooper and Williams1989; McClay, Reference McClay, Buchanan and Buchanan1995). The detailed geometry of these steeply dipping to overturned forelimbs is well constrained by outcrop and subsurface data, with several exploration wells drilled in front of basement structures that navigated along steep flanks for > 3 km. Surface structural data along these forelimbs show consistent steeply dipping to overturned panels, whereas seismic data show an abrupt lack of information restricted to a relatively narrow zone that matches with the subvertical beds constrained by wells and surface information. This deformation geometry seems to be shared by other basement anticlines not clearly related to inversion of large extensional depocentres, including the Sierra Azul-Bardas Blancas and several other structures further south (Manceda & Figueroa, Reference Manceda, Figueroa, Tankard, Suárez Soruco and Welsink1995; Giambiagi et al. Reference Giambiagi, Ghiglione, Cristallini and Bottesi2009). The mechanics behind this mode of deformation remain poorly understood, but may be influenced by the composition and anisotropies within the regional basement, the Choiyoi Group and underlying units, whose rheology is significantly different than more homogeneous crystalline basement rocks. Second, although basement structures have a structural relief of several kilometres, the topography is limited, and the frontal inverted structures have particularly subtle topographic expression. For example, the Rio Atuel anticlinorium records ~ 4–5 km of structural inversion (as constrained by restoration of the top of Choiyoi basement to its original post-rift position) yet shows only a modest shift in topography (Fig. 5). This apparent contradiction may be resolved through assessments of the relative timing between inversion, erosion and flexural subsidence in the adjacent foreland, with the possibility that poorly consolidated sedimentary rocks on top of growing basement structures were easily eroded and deposited in foreland depocentres along the eastern front of these structures.

A further interesting point of the MFTB is the potential presence of Cenozoic extensional faults, closely post-dating Andean contractional deformation (cross-sections A–A′ and B–B′ of Fig. 5). The W-dipping El Infiernillo fault (Gerth, Reference Gerth1931) west of Puesto Rojas has been interpreted as a Neogene extensional fault of post-orogenic origin by Kozlowski et al. (Reference Kozlowski, Cruz, Manceda and Condat1990). Evidence for Quaternary activity on this fault comes from basaltic lavas that have erupted along the fault (Ramos & Kay, Reference Ramos, Kay, Kay and Ramos2006). In our reconstructions, this fault is developed along a local structural culmination composed of stacked Mesozoic units, and links westward with the former basement thrust fault related to the Los Blancos anticline. Late-stage extensional collapse along similar structural culminations is well documented in the North America Cordillera (e.g. Constenius, Reference Constenius1996). North of Arroyo El Durazno, geological maps (Mombrú & Bettini, Reference Mombru and Bettini1975) show clear extensional faulting map relationships, with younger Neuquén Group hanging-wall strata in fault contact with older Vaca Muerta footwall deposits, further supporting an extensional origin for the El Infiernillo fault.

5. Kinematic evolution and synorogenic sedimentation

Several recent studies have provided information on the timing of thrust belt deformation in this region (Giambiagi et al. Reference Giambiagi, Bechis, García and Clark2008; Turienzo, Reference Turienzo2010; Kraemer et al. Reference Kraemer, Silvestro, Achilli, Brinkworth, McClay, Shaw and Suppe2011; Turienzo et al. Reference Turienzo, Dimieri, Frisicale, Araujo and Sánchez2012; Boll et al. Reference Boll, Alonso, Fuentes, Vergara, Laffitte and Villar2014). The general consensus is that inversion of the eastern frontal structures of the basement-involved Malargüe anticline and Rio Atuel anticlinorium occurred since middle Miocene time (Giambiagi et al. Reference Giambiagi, Bechis, García and Clark2008; Kraemer et al. Reference Kraemer, Silvestro, Achilli, Brinkworth, McClay, Shaw and Suppe2011), although 3D seismic data in the eastern foreland platform show minor movement along basement faults since Late Cretaceous and Palaeogene time (Boll et al. Reference Boll, Alonso, Fuentes, Vergara, Laffitte and Villar2014), coeval with early shortening along more-hinterland structures in the west (Kozlowski, Cruz & Sylwan, Reference Kozlowski, Cruz and Sylwan1997; Mescua, Giambiagi & Ramos, Reference Mescua, Giambiagi and Ramos2013; Boll et al. Reference Boll, Alonso, Fuentes, Vergara, Laffitte and Villar2014). Based on several cross-cutting relationships, Giambiagi et al. (Reference Giambiagi, Bechis, García and Clark2008) bracketed basement fault reactivation and basin inversion between 15 and 1 Ma, with maximum displacement before 8 Ma. On the basis of deformation timing from growth strata associated with the Malargüe anticline, Kraemer et al. (Reference Kraemer, Silvestro, Achilli, Brinkworth, McClay, Shaw and Suppe2011) postulated limited shortening before 7 Ma, when basement deformation accelerated along this structure. To the north, uplift of the basement-involved Carrizalito range may have initiated later, at about 5 Ma (Combina, Nullo & Stephens, Reference Combina, Nullo and Stephens1993).

Whereas the broad age of deformation along the frontal part of the MFTB is relatively well documented, the relative timing and geometric linkages between thick- and thin-skinned structures is not. Previous work focused on the interactions between basement structures and the frontal thrust systems in the foreland, including the Mesón and Sosneado thrusts (Giambiagi et al. Reference Giambiagi, Bechis, García and Clark2008; Turienzo, Reference Turienzo2010; Turienzo et al. Reference Turienzo, Dimieri, Frisicale, Araujo and Sánchez2012), but less attention has been paid to the relationships with thin-skinned thrust systems developed atop the Rio Atuel basement structure. Our structural reconstructions based on map, well and seismic data provide further constraints. The emerging pattern results in a model that does not differ from the typical behaviour of most thrust belts, with deep-seated thrusts that ramp up and transfer slip to shallower stratigraphic levels, followed by foreland propagation of new deep-seated thrust sheets that lift and carry, in piggyback fashion, the original shallow thrust systems.

The kinematic evolution can be deduced from structural relationships in cross-sections A–A′ and B–B′ of Figure 5, and can be extrapolated to the north. The sequence of deformation can be divided into several steps. The first phase involved basement thrusting below the Los Blancos anticline, which fed slip into Mesozoic units, creating relatively simple contractional geometries in the Jurassic section and a complexly deformed duplex system once thrusts climbed to levels above the Vaca Muerta shales. The emplacement of these later structures occurred at depth, on top of a still non-inverted Rio Atuel extensional depocentre. The eastern extent of the shallow duplex system was conditioned by both the lateral change from organic-rich shale to coarser, less organic facies in Vaca Muerta, and the eastern extent of evaporites in the Huitrín Formation, which provided favourable conditions for floor and roof thrust development. The second phase involved reverse reactivation of a basement extensional fault and hanging-wall folding in the Rio Atuel structure. This passively lifted the older, thin-skinned Puesto Rojas structures, and also fed slip to the present frontal thrust system of Mesón, Sosneado and related faults. The relative timing between the Puesto Rojas structures and the Rio Atuel fault reverse motion is well constrained: well data indicate that the basal detachment of the Puesto Rojas structures now dips east, and the northern continuation of this shallow thrust system in the Loma del Medio area (Fig. 8) is presently located along the vertical to overturned frontal part of the Rio Atuel basement anticline. A relatively similar situation has been described by Kraemer et al. (Reference Kraemer, Silvestro, Achilli, Brinkworth, McClay, Shaw and Suppe2011) further south at 35.5°S, with the shallow La Brea triangle zone developing in front of the Torrecillas and La Valenciana anticlines, before being passively deformed during development of the broader Malargüe anticline and its hanging-wall shortcut splay.

The timing of these two phases in the structural evolution of the MFTB can be assessed through analysis of surface and subsurface growth stratal successions expressed in the foreland basin fill. The younger phase of basement reactivation and associated frontal thrusting is recorded by a growth stratal succession expressed in foreland basin fill along the eastern margin of the Rio Atuel structure, in the footwall of the mapped La Manga fault (Fig. 8). Along the Vega del Burro, a tributary drainage to the larger Arroyo La Manga, a roughly 400 m thick exposure of the Loma Fiera-Tristeza Formation shows major variations in stratal dip (Fig. 9). Whereas the lowest levels of the succession show steeply overturned, W-dipping bedding orientations, upper levels exhibit gentle (10–20°) eastward dips. Internally, individual beds show an eastward thickening, away from the bounding structure to the west. The upsection reduction in stratal dip and internal thickness variations are contained in a narrow zone within ~ 1 km of the mapped trace of the La Manga fault (Fig. 8). We interpret these geometric relationships as the product of synchronous fault displacement and synorogenic sedimentation during motion on the thick-skinned Rio Atuel basement structure.

Figure 9.

Schematic line drawing showing growth strata preserved in upper Miocene beds of the Loma Fiera-Tristeza Formation at the Vega de Burro locality, in the eastern footwall of the major E-directed thrust exposed in the Loma del Medio area (Fig. 8). The young zircon U–Pb age populations from two volcaniclastic horizons provide estimates of late Miocene depositional ages and synchronous thrusting.

The Vega del Burro growth stratal succession is dominated by disorganized, pebble to boulder conglomeratic facies with large proportions of volcaniclastic material. Nearby sources of volcanogenic materials are consistent with previously documented phases of volcanism and shallow intrusive activity (Combina & Nullo, Reference Combina and Nullo2011). New zircon U–Pb geochronological analyses of two volcaniclastic horizons from lower and upper levels of the growth stratal succession yielded youngest age populations of 10.0±0.2 Ma (n = 3 grains) and 7.7±0.3 Ma (n = 5 grains), respectively (Fig. 9). These relationships require that Rio Atuel basement reactivation was active during late Miocene time, with significant deformation during the broad 10.5 to 7.5 Ma window.

The older phase of thrusting is likely recorded in comparable growth stratal geometries imaged in seismic reflection profiles and depicted in our regional cross-sections (Fig. 5). Growth relationships in the westernmost subsurface occurrences of the Agua de la Piedra Formation, along the western limb of the Tristeza syncline (Fig. 5) show pronounced eastward thickening and progressively shallower dips for higher stratigraphic levels. Rather than representing reactivation of the Rio Atuel basement structure, we suggest that these older, roughly early to middle Miocene growth relationships are the product of early displacement along the western trailing basement structure (Rio Blanco anticline) and geometrically linked displacement within the aforementioned shallow duplex system (Puestos Rojas structures).

6. Importance for petroleum exploration

Several hydrocarbon fields have been discovered in the MFTB and adjacent basin (Giampaoli, Ramirez & Gait, Reference Giampaoli, Ramirez, Gait, Kozlowski, Vergani and Boll2005; Boll et al. Reference Boll, Alonso, Fuentes, Vergara, Laffitte and Villar2014). Potential Jurassic–Cretaceous source rocks include the Tres Esquinas, Vaca Muerta and Agrio formations, although most current results associate the existing fields with Vaca Muerta oils (Boll et al. Reference Boll, Alonso, Fuentes, Vergara, Laffitte and Villar2014). Within the foreland, the El Sosneado and contiguous Loma de la Mina fields total 19 million barrels of oil; further south, Llancanelo is a heavy oil field of 6 million barrels. In contrast, in the thrust belt, 35 million barrels of oil are contained within the Puesto Rojas, Cerro Mollar and several small oil fields. The foreland fields produce from subtle traps, possibly controlled by low-offset reactivated basement faults, stratigraphic traps and combined traps. These fields, however, are located away from the best source rock conditions in the Vaca Muerta, as they are along the thin, and coarser platformal zone with lean to mostly immature conditions. However, atop the Rio Atuel anticlinorium, the Vaca Muerta has optimal source rock conditions with systematic high TOC values, and maturity values reaching the oil window (Boll et al. Reference Boll, Alonso, Fuentes, Vergara, Laffitte and Villar2014) (Fig. 10). Therefore, the migration and hydrocarbon charge of platform traps must have occurred prior to inversion of the Rio Atuel depocentre, unless generation was produced in the buried narrow strip directly east of the Vaca Muerta footwall cutoff, beneath the eastern flank of the Rio Atuel anticlinorium (Figs 5, 10). This narrow zone has not been reached by exploration wells and may have transitional facies, perhaps with generation potential. However, exploration risks in the platform would be minimized by drilling traps that existed before inversion.

Figure 10.

Cross-section A–A′ (Fig. 5) showing vitrinite reflectance (Ro %) values for the Puesto Rojas area and foreland platform, based on outcrop and well samples. Note the overall poor maturity (low Ro values) for the synorogenic sediments, suggestive of a low geothermal gradient.

For the Puesto Rojas and contiguous Cerro Mollar fields within the MFTB, the kinematic evolution and the existing geochemical data and burial history models (Boll et al. Reference Boll, Alonso, Fuentes, Vergara, Laffitte and Villar2014) suggest that traps were likely charged prior to reverse reactivation of the Rio Atuel fault, when the shallow duplex system was deeply buried in its pre-inversion configuration. This play situation could be quite favourable, with quality source rocks and thick evaporites providing an efficient top seal for fractured reservoirs of the Chachao and Agrio formations. Subsequent exhumation due to basement uplift along the reactivated Rio Atuel fault must have been highly destructive for existing hydrocarbon accumulations, with survival of only those preserving a cover of Rayoso evaporites and sufficient closure to minimize hydrocarbon spilling. If correct, this model suggests the Puesto Rojas and Cerro Mollar fields can be considered palaeo-traps that were subsequently uplifted as part of the Rio Atuel anticlinorium during later inversion. An alternative scenario is that these thrust systems were uniformly carried close to the surface without receiving an original oil charge, but later remigration introduced fluids which converged towards the Puesto Rojas area along routes defined by the structural geometry of the large anticlinorium.