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Examples of low angle reverse faults, Chenareh anticline. (a) 3D model based on QuickBird imagery and 25 m satellite DEM with selected bedding measurements and traces of the hinge zones. Location of LiDAR derived 3D photorealistic models (Chenareh Gorge) is represented by red curves. (b) Untextured 3D photorealistic model of the Chenareh Gorge, reconstructed main stratigraphic surfaces and locations of the close up examples of low-angle thrusts (red boxes). (c) Close up: field photograph (shooting direction along fold axis) of low angle thrust (red lines) located in the gently dipping backlimb. Stereographic projections of backtilted low-angle thrust measurements from RSD and fieldwork. Fault plane: black great circles; kinematic indicators: red circles. Detail (upper right) for comparison between outcrop structures and 3D photorealistic models signature. (d) Close up: LiDAR derived 3D photorealistic model of the steeply dipping forelimb. Red lines represent interpreted thrusts.
Source publication
The Simply Folded Belt of the Zagros Mountains, Iran, is a spectacularly well-exposed example of a foreland fold and thrust belt. A regional analysis of the Cenomanian–Coniacian Sarvak and Ilam Formations, exposed in the southern Lurestan Province, is presented as a case study for sub-seismic fracture development in this type of compressive setting...
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Context 1
... in gently dipping and sub-vertical domains of fold limbs. The angular relationship between thrusts and bedding is maintained regardless of structural position and bedding dip domain. Thrusts generally have a poorly developed damage zone and limited fault core thickness. This type of structure is particularly well exposed along the Chenareh Gorge (Fig. 8). In this locality, the Ilam and Upper Sarvak formations are continuously exposed and characterized by basin, slope, mar- gin and platform top facies organized into five 3rd-order cycles. Thrusts occur preferentially in basin, slope and plat- form top ...
Context 2
... occurrence of low-angle thrusts seems to be mostly controlled by the stratigraphy rather than the structural pos- ition. Low-angle thrusts are distributed homogeneously across anticlines and they are characterized by a constant angle (c. 20() to bedding regardless of the structural domains where they occur (Fig. 8). These observations, together with lack of systematic distribution of top-to-the-SW and NE thrusts in backlimb and forelimb of the anticlines respectively rules out the hypothesis that these structures developed as a conse- quence of flexural slip during folding. Instead, it suggests that low-angle thrusts formed before folding and ...
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Citations
... Laubach et al., 2009;Hooker et al., 2013), and previous episodes of deformation (e.g. Agosta et al., 2010;Casini et al., 2011;Ferrill et al., 2021) are among some of the other factors that may influence fracture network properties. Each of the relationships outlined above may impart spatial Figure 1. ...
Subsurface datasets typically lack the resolution or coverage to adequately sample fracture networks in 3D, and fracture properties are typically extrapolated from available data (e.g. seismic data or wellbore image logs). Here we assess the applicability of extrapolating fracture properties (orientation, length, and intensity) across observation scales in deformed, mechanically layered carbonate rocks. Data derived from high-resolution field images, medium-resolution digital outcrop data, and relatively low-resolution satellite imagery at Swift Reservoir anticline, NW Montana are leveraged to (i) assess interacting structural and stratigraphic controls on fracture development, and (ii) compare estimated fracture properties derived from multiple observation scales. We show that hinge-parallel and hinge-perpendicular fractures (i) make up the majority of fractures at the site; (ii) are consistently oriented with respect to the fold hinge, despite along-strike variability in the fold hinge orientation; and (iii) exhibit systematic increases in intensity towards the anticline hinge. These fractures are interpreted as having formed during folding. Other fractures recorded at the site exhibit inconsistent orientations, show no systematic trends in fracture intensity, and are interpreted as being unrelated to fold formation. Fracture orientation data exhibit the greatest agreement across observation scales at hinge and forelimb positions, where hinge-parallel and hinge-perpendicular fracture sets are well developed, and little agreement on the anticline backlimb, where fracture orientations are less predictable and more dispersed. This indicates that the scaling of fracture properties at Swift Reservoir anticline is spatially variable and partly dependent on structural position. Our results suggest that accurate prediction and extrapolation of natural fracture properties in contractional settings requires the assessment of structural position, lithologic variability, and spatially variable fracture scaling relationships, as well as consideration of the deformation history before and after folding.
... Geological storage of CO 2 (GSC) requires an appropriate reservoir placed at a suitable depth to guarantee efficiency (Alcalde et al., 2014;Bachu, 2000;Sun et al., 2020). However, the presence of fold-related fractures, which have a critical impact on the distribution of the reservoir quality, is not always easy to characterize at depth because they are usually below the resolution of standard geophysical techniques (Brandes and Tanner, 2014;Casini et al., 2011;Gutmanis et al., 2018). Therefore, the orientation, extent and the implication of such fracture systems for reservoir potential in the subsurface can only be predicted by using geological models and outcrop analogues (Brandes and Tanner, 2014;Sun et al., 2021;Tavani et al., 2015). ...
... Therefore, the approaches used to determine the relative age of fracture development are: (i) the crosscutting relationships between different fracture and striae sets; (ii) the relation between fracture orientation and bedding attitude; and (iii) the restriction of fractures to specific preand/or syn-orogenic units. Following these assumptions, we summarize the fold evolution in four stages of deformation, which are in line with previous studies describing the evolution of folds in fold-and-thrust belts (Amrouch et al., 2010;Beaudoin et al., 2015Beaudoin et al., , 2020Casini et al., 2011;Lacombe et al., 2021;Tavani et al., 2015): ...
... Fold tightening stage: this late deformation stage is represented by fractures that are still consistent with a NNW-SSE shortening direction but are characterized by a constant orientation independently of the bedding dips, and by large faults offsetting the already folded beds of the anticline. These features are indicative of a fold tightening stage (Amrouch et al., 2010;Beaudoin et al., 2020;Casini et al., 2011;Lacombe et al., 2021;Tavani et al., 2015). At this stage, the ongoing shortening is expected to be oriented at a high angle with respect to bedding and the resulting deformation has been interpreted as accommodated by: (i) the formation of thrust faults (Bóixols thrust in the Forat de Bóixols and the Abella de la Conca localities), offsetting the steeply dipping forelimb of the anticline; and (ii) strike-slip faults exhibiting subhorizontal striae sets and recording a subhorizontal maximum principal stress regardless of the bedding dips across the anticline (Fig. 10). ...
Dating fold-related structures is critical to understand the timing, duration, and rate of fold growth as well as the sequential evolution of fold-and-thrust belts. In this contribution, we combine structural analysis of fractures with U-Pb dating of calcite veins related to the evolution of the Bóixols-Sant Corneli anticline (Southern Pyrenees) aiming to constrain the age and evolution of deformation and the duration of folding. Twenty-three U-Pb ages were obtained in the different sets of fracture-filling calcite veins, which span from Late Cretaceous to late Miocene (79.8 ± 1.2 Ma to 9 ± 4.6 Ma). These ages have been attributed to growth (71.2 to 56.9 Ma), fold tightening (55.5 to 27.4 Ma) and collapse (20.8 to 9.0 Ma) of the Bóixols-Sant Corneli anticline. This reveals a duration of 14 Myr for the folding stage and 28 Myr for the fold tightening, which translates in 42 Myr of the entire folding process and thus encompassing most of the Pyrenean compression.
For more info:
https://www.researchgate.net/publication/361272185_Spatio-temporal_variation_of_fluid_flow_behavior_along_a_fold_The_Boixols-Sant_Corneli_anticline_Southern_Pyrenees_from_U-Pb_dating_and_structural_petrographic_and_geochemical_constraints
... Deformation style and type of folds are different across the belt due to high plasticity of salt deposits that acting and basal and middle detachments and association of folds with often hidden faults in the Zagros Fold-Thrust Belt (e.g., Molinaro et al. 2005;Carruba et al. 2006;Sepehr et al. 2006;Sherkati et al. 2006;Jahani et al. 2009). This can cause seismicity variations in terms of distribution, magnitude, focal depth and mechanism of earthquakes (Talebian & Jackson 2004;Nissen et al. 2007Nissen et al. , 2011Nissen et al. , 2014Roustaei et al. 2010;Casini et al. 2011;Barnhart et al. 2018). ...
The Zagros Fold-Thrust Belt is one of the most tectonically active regions in the world. The seismicity of this belt is affected by various factors and has certain complexities. This paper provides the results of assessment of temporal and spatial seismicity variations of the central portion of the belt in Fars and Bushehr provinces and their link to regional tectonic properties. Relatively, everywhere in the belt, the geometry of the folds has been mainly affected by thrusts and basement faults. There is a meaningful link between seismic activity and folding in the belt. The most abundant types of folds are detachment folds, fault bend and fault propagation folds. They play an important role in the spatial seismicity of the area. The maximum number of seismic events have medium magnitude which ranges between 2.5 and 3. There is a decreasing trend of a and b parameters from southwest to north and northeast where the occurrence of higher magnitude earthquakes is expected. Temporal analysis of seismicity shows that earthquakes with magnitude≥ 6.5 have a ten-year return period in the region. The occurrence of several earthquake groups in the belt was in the form of swarms showing point or linear spatial distribution. Some of these possible swarms are around transverse faults, salt domes and some are related to blind faults, which indicate the complexity of the seismicity in this belt. Spatial distribution of low magnitude seismic clusters is also influenced by two other factors (1) existence of frequent salt domes many of which might be active and their spatial links to major faults and (2) human-related activities, especially hydrocarbon extraction.
... In folded successions, the stratigraphic segregation of fluids remains stable during layer-parallel shortening, whereas fluid reservoirs can be interconnected by the development of crossformational fracture systems during more advanced stages of folding as discussed in Evans and Fischer (2012) and Cruset et al. (2020a) (Fig. 16A, C and D). Fracture systems with good connectivity may cut seal units, favouring the migration of deep hydrothermal fluids and resources previously accumulated beneath non-permeable units, as observed in anticlines from the Bighorn Basin, the Paradox foreland basin and the Lurestan Zagros fold and thrust belt (Sharp et al., 2010;Casini et al., 2011;Beaudoin et al., 2014;Ogata et al., 2014). The fluid flow evolution and the relative extent of fluid-rock interaction during the growth of anticlines may be controlled by the scale and distribution of fracture networks, by the structural domain of the fold and by the folded stratigraphy, as concluded by Muñoz-López et al. (2022) in their study of the Bóixols-Sant Corneli anticline in the Southern Pyrenees. ...
We propose a review to discuss the large number of studies dealing with the fluid history in extensional and compressional sedimentary basins that evolved along the Iberian-Eurasian plate boundary during the full Mesozoic-Cenozoic Wilson Cycle in the Pyrenean fold belt and the Basque-Cantabrian Basin. We integrate classic and modern geochemical and geochronological datasets used in fluid studies with the current tectonic knowledge of the studied area.
Late Hercynian fluid systems were dominated by Carboniferous-early Permian magmatic intrusions related to large-scale lithospheric delamination at the end of the collision, which caused the accumulation of skarns at depths of 8000–10,000 m during contact metamorphism. During the Mesozoic extension, early and widespread shallow burial dolomitization of Jurassic and Early-Cretaceous carbonates occurred at burial depths of 500–1000 m due to seawater influx. From Albian to Cenomanian, along the North Pyrenean extensional fault zone, contact metamorphism processes occurred in association with mantle-derived and deep-crustal fluids at temperatures higher than 300 °C, which interacted with Triassic evaporites and formation and marine waters and depths of 2000–3000 m. Away from this fault, fluid systems were dominated by hydrothermal dolomitization and the accumulation of Znsingle bondPb mineralization along diapir walls and faults, whereas in the less extended and proximal domains of the extensional system, fluids were formation waters at temperatures up to 150 °C. The Alpine compressional fluid history registers the increasing influence of meteoric fluids as the foreland basin became overfilled and fluid flow occurred at depths of 2.5–4 km in tectonic units detached in Triassic evaporites and of >4 km in units rooted at depth with the Paleozoic basement. Along and across strike differences in the fluid evolution of the Pyrenees are attributed to changes in the structure of the cover and basement tectonic units, the westward decrease of shortening and in the oblique directions of Upper Triassic successions, which acted as very efficient seals for deep-sourced fluids.
Subvertical walls of diapirs are baffles for fluid flow, whereas fracturing and deposition of porous halokinetic successions are effective conduits. Evaporite detachments compartmentalize paleohydrological systems during tectonic deformation, although they may be breached by fluids reaching lithostatic pressures. In large evaporite-bearing provinces, fluid systems may share common patterns during successive extensional and compressional tectonic events, as documented in the Western Mediterranean Mesozoic extensional rift system. In this area, metal-bearing and deep-sourced fluids interacted with Triassic sulphates and organic matter, triggering the accumulation sulphides in rock porosity. However, more research is needed in other large-scale evaporitic provinces of different ages to identify common fluid flow patterns.
... Rock cores and borehole wall imagery provide the sources of data for characterizing directly the nature of subsurface fractures (e.g., Poppelreiter et al., 2010;Casini et al., 2011). These observations and measurements provide an opportunity to test fracture model predictions and to infer paleo and/or present-day stress states (e.g., Wu and Pollard, 2002;Barton et al., 2009). ...
In the Keshen gas field in the northern Tarim Basin, the main production interval is the ultra-deep (>6000 m), ultra-high pressure Lower Cretaceous Bashijiqike Formation. Understanding the characteristics and role of natural fractures in the reservoir is essential for efficient exploration and development. Data from borehole images (42 vertical wells) and cores (12 vertical wells) enabled a comprehensive characterization of fracture attributes, including mode, orientation, fill, density, and clustering as well as variations with respect to depth and structural position. Using image logs from 20 vertical wells and cores from 12 wells, we find that steeply dipping (>60°), E-W and N–S-striking fractures are the most common across the studied anticline. Fracture density is highest in the forelimb and near faults (2.85 fractures/m), compatible with fracture formation during folding and associated faulting. Fracture clusters 10+ m wide are also preferentially located within these structural zones and are spaced around 5–15 m apart. Fracture orientations, fill, and density varies with depth. We identify a depth transition horizon above and below which fracture characteristics, specially strike, dip, and resistivity change dramatically. We infer those changes are due to fold geometry, rheological differences associated with increasing pressure and temperature at extreme depths. We observe anhydrite-filled fractures located near the top of the formation, whose presence is associated with overlying evaporites. Vertical and lateral variations of fracture characteristics and distribution discovered in this reservoir may aid the interpretation and prediction of the fracture network in other ultra-deep sandstone reservoirs with a comparable setting or well performance.
... The Asmari Formation is one of the main reservoir rocks in the Zagros region due to its high primary porosity Hegre, 2005, 2010). The fracture network in the Asmari Formation provides secondary porosity that enhances hydrocarbon recovery and, as a result, many studies have focused on the fracture patterns in this formation (McQuillan, 1973(McQuillan, , 1974Wennberg et al., 2007;Ahmadhadi et al., 2007Ahmadhadi et al., , 2008Casini et al., 2011;Carminati et al., 2013Carminati et al., , 2014Tavani et al., 2018). Some of these studies have been conducted specifically on the Kuh-e-Asmari anticline (McQuillan, 1974;Ahmadhadi et al., 2008;Carminati et al., 2013), and have identified four main sets of fractures oriented orthogonal to bedding, striking NW-SE and NE-SW (i.e. ...
Multi-scale fracture characterisation in reservoir analogues is crucial for determining orientation clustering, length scaling laws, abundance, and topology of the fracture network, all of which are essential for modelling flow of geofluids. In this study, we examine the application of Bing Maps imagery for fracture network analysis in the Kuh-e-Asmari anticline (Zagros Mountains, Iran), a scarcely vegetated area which is a good outcropping analogue for fractured reservoirs. Image-derived fracture characterisation is conducted at three distinct scales (1:50,000, 1:5,000 and 1:500) using the NetworkGT plugin in QGIS and was compared with structural data collected in the field (i.e. scan lines). The results reveal a scale dependency, with the advantages and disadvantages of each scale summarised as follows. The 1:50,000 is the only spatially continuous dataset. The 1:5,000 dataset, potentially spatially continuous, enables the analysis of fracture and connectivity distribution in great detail, emphasising strongly fractured/connected elongated zones, which may represent damage zones of known, previously mapped fault strands. The 1:500 scale does not ensure the spatial continuity of the dataset; however, similar to scan lines, it can perform detailed analyses of the fracture network in potentially interesting areas. We conclude that structural field surveys can be combined with multi-scale mapping on aerial images to better define the length and abundance distribution of fractures.
... Rock cores and borehole wall imagery provide the sources of data for characterizing directly the nature of subsurface fractures (e.g., Poppelreiter et al., 2010;Casini et al., 2011). These observations and measurements provide an opportunity to test fracture model predictions and to infer paleo and/or present-day stress states (e.g., Wu and Pollard, 2002;Barton et al., 2009). ...
... Page 2 of 21 a positive impact on the carbonate reservoir quality (Casini et al. 2011). The Cretaceous carbonate Formations are well identified in the Southern Tunisian domain in outcrops as well as in the subsurface (Busson 1969;Abdallah 1989;Mamou 1990;Razgallah et al. 1994;Bouaziz 1995;Abdallah et al. 2000;Bouaziz et al. 2002;Zagrarni et al. 2008;Bodin et al. 2010;Grosheny et al. 2013). ...
The present study is dealing with the characterization of 67 m thick Cretaceous carbonate sequences. The study relied on petrophysical laboratory core analysis, sedimentological and fracture investigations. Four facies were recognized based on field and petrographic analysis i.e., stromatolitic limestone, fossiliferous limestone, rudist-rich dolomite, and dolomite with stromatolitic intercalations. Throughout the studied deposits, the measured data showed relatively high porosities. The stromatolitic limestone revealed the most important porosity reaching 30%. The bioclastic limestone, the rudist-rich dolomite, and the dolomite with stromatolitic intercalations showed an average porosity of 8.9%, 11.5% and 10.4%, respectively. The diagenetic processes affecting petrofabric and pore types are the main factors controlling the evolution of porosity, fluid flow and acoustic properties of the studied deposits. Several diagenetic features were identified and seem to enhance or reduce the pore space. The dissolution and micro-fracture processes are responsible for enhancing porosity, whereas, compaction, neomorphism and cementation processes contribute on its reduction. Dolomitization has a mixed-impact by improving and decreasing reservoir quality. Cemented rocks filled with calcite may have considerable influence on enhancing P-wave propagation; however, connected open micro-fractures and channel pores showed a significant decrease in velocities. The fracture analysis revealed a clear anisotropy of permeability being mostly represented by WNW-trending in the upper part of the Zebbag Formation and the lower part of the Bahloul equivalent, whereas NW–SE to NNW-trending predominate the remaining series. Consequently, the Upper Cenomanian–Turonian deposits represent a petroleum potential and hydrogeological interest where the fracture intensity is the main factor enhancing reservoir qualities.
... Earthquakes not only shake the surface of the earth and create surficial hazards but also modify the hydrogeological conditions of an area (Niwa et al., 2012). A moderate earthquake may create fractures/micro-cracks (Casini et al., 2011), liberate the old fractures, and also cause fracture widening and closing (Wang and Manga, 2010;Valigi et al., 2019). It may influence the discharge, temperature, and ± electrical conductivity of spring water (King et al., 1994;Manga and Rowland, 2003). ...
Springs and streams are essential sources of fresh water for the Himalayan population. On global and regional extents, these resources are being severely affected by climate change as well as anthropogenic activities. However, the effects of seismicity also have considerable influence on springs, but negligibly studied in that aspect. Crustal deformation, shaking and shifting of the earth's surface, due to an earthquake, can modify the stream flow and water level in wells through consolidation of surficial deposits and development of new fractures. The present study addresses the effect of an earthquake on water springs in a seismically active. On 18 September 2011, the Sikkim Himalaya experienced a strong earthquake of magnitude (Mw) 6.9. To assess the impact of this earthquake on hydrology, we studied the springs in South Sikkim district, India. Our study suggests that after the 2011 earthquake of Mw 6.9, some of the springs were dried up, whereas some springs discharged at a higher rate than earlier. We excluded the springs which were dried due to climate change in this study. Further, Our study suggests that in tectonically active mountain ranges, like Himalaya, an earthquake not only caused the surficial deformations but also influences the hydrological framework on regional scale. Therefore the seismic nature of the terrain should also be considered for spring rejuvenation policies.
... Geological storage of CO 2 (GSC) requires an appropriate reservoir placed at a suitable depth to guarantee efficiency (Alcalde et al., 2014;Bachu, 2000;Sun et al., 2020). However, the presence of fold-related fractures, which have a critical impact on the distribution of the reservoir quality, is not always easy to characterize at depth because they are usually below the resolution of standard geophysical techniques (Brandes and Tanner, 2014;Casini et al., 2011;Gutmanis et al., 2018). Therefore, the orientation, extent and the implication of such fracture systems for reservoir potential in the subsurface can only be predicted by using geological models and outcrop analogues (Brandes and Tanner, 2014;Sun et al., 2021;Tavani et al., 2015). ...
... Therefore, the approaches used to determine the relative age of fracture development are: (i) the crosscutting relationships between different fracture and striae sets; (ii) the relation between fracture orientation and bedding attitude; and (iii) the restriction of fractures to specific preand/or syn-orogenic units. Following these assumptions, we summarize the fold evolution in four stages of deformation, which are in line with previous studies describing the evolution of folds in fold-and-thrust belts (Amrouch et al., 2010;Beaudoin et al., 2015Beaudoin et al., , 2020Casini et al., 2011;Lacombe et al., 2021;Tavani et al., 2015): ...
... Fold tightening stage: this late deformation stage is represented by fractures that are still consistent with a NNW-SSE shortening direction but are characterized by a constant orientation independently of the bedding dips, and by large faults offsetting the already folded beds of the anticline. These features are indicative of a fold tightening stage (Amrouch et al., 2010;Beaudoin et al., 2020;Casini et al., 2011;Lacombe et al., 2021;Tavani et al., 2015). At this stage, the ongoing shortening is expected to be oriented at a high angle with respect to bedding and the resulting deformation has been interpreted as accommodated by: (i) the formation of thrust faults (Bóixols thrust in the Forat de Bóixols and the Abella de la Conca localities), offsetting the steeply dipping forelimb of the anticline; and (ii) strike-slip faults exhibiting subhorizontal striae sets and recording a subhorizontal maximum principal stress regardless of the bedding dips across the anticline (Fig. 10). ...
This study integrates field structural data, petrographic and geochemical (δ¹⁸O, δ¹³C, Δ47, ⁸⁷Sr/⁸⁶Sr, and elemental composition) analyses and U–Pb dating of calcite veins cutting the Bóixols-Sant Corneli anticline (Southern Pyrenees) in order to date and to investigate the spatio-temporal relationships between fluid flow and fold evolution. This E-W trending anticline grew from Late Cretaceous to Paleocene at the front of the Bóixols thrust sheet deforming pre-growth and growth sedimentary sequences. U–Pb dating reveals Late Cretaceous to late Miocene deformation ages, which agree with the age of growth strata deposition and the sequence of deformation interpreted from field and microstructural data. Dates coeval (71.2 ± 6.4 to 56.9 ± 1.4 Ma) and postdating (55.5 ± 1.2 to 27.4 ± 0.9 Ma) Upper Cretaceous to Paleocene growth strata are interpreted to record: (i) the growth of the Bóixols-Sant Corneli anticline during the Bóixols thrust emplacement, and (ii) the tightening of the anticline during the southern tectonic transport of the South-Central Pyrenean Unit. Other ages (20.8 ± 1.2 to 9.0 ± 4.6 Ma) postdate the folding event and have been associated with the collapse of the Bóixols-Sant Corneli anticline. The geochemistry of calcite veins indicates that the fluid flow behavior varied across the Bóixols-Sant Corneli anticline through its growth, showing a compartmentalized fluid system. In the hinge of the anticline and in the upper Santonian to middle Campanian syn-orogenic sequence along the footwall of the Bóixols thrust, the similar petrographic and geochemical features between all calcite cements and host rocks point towards a locally-derived or well-equilibrated fluid system. Contrarily, along large faults such as the Bóixols thrust, and in the anticline limbs, the geochemistry of vein cements indicates a different scenario. Cements in large faults yielded the lightest δ¹⁸O values, from −8 to −14 ‰VPDB, and variable enrichment in δ¹³C, ⁸⁷Sr/⁸⁶Sr, elemental composition and δ¹⁸Ofluid. This is interpreted as the migration of fluids, through fault zones, that evolved from distinct fluid origins. Cements in the fold limbs exhibit δ¹⁸O and δ¹³C between −8 and −6 ‰VPDB and between −10 and + 2 ‰VPDB, respectively, the lowest Sr contents and the lowest precipitation temperatures, suggesting that the anticline limbs recorded the infiltration and evolution of meteoric waters. The paleohydrological system in the Bóixols-Sant Corneli anticline was restricted to the Bóixols thrust sheet. The Upper Triassic evaporitic basal detachment likely acted as a lower fluid barrier, preventing the input of fluids from deeper parts of the Pyrenean crustal thrust system. This study provides a well-constrained absolute timing of fracturing and fluid flow during basin inversion and folding evolution and highlights the suitability of U–Pb geochronology to refine the age of fractures and veins and their sequential evolution in orogenic belts.
