Tectono-thermal evolution of Oman's Mesozoic passive continental margin under the obducting Semail Ophiolite: a case study of Jebel Akhdar, Oman
We present a study of pressure and temperature evolution in the passive continental margin under the Oman Ophiolite using numerical basin models calibrated with thermal maturity data, fluid-inclusion thermometry, and low-temperature thermochronometry and building on the results of recent work on the tectonic evolution. Because the Oman mountains experienced only weak post-obduction overprint, they offer a unique natural laboratory for this study.
Thermal maturity data from the Adam Foothills constrain burial in the basin in front of the advancing nappes to at least 4 km. Peak temperature evolution in the carbonate platform under the ophiolite depends on the burial depth and only weakly on the temperature of the overriding nappes, which have cooled during transport from the oceanic subduction zone to emplacement. Fluid-inclusion thermometry yields pressure-corrected homogenization temperatures of 225 to 266 ∘C for veins formed during progressive burial, 296–364 ∘C for veins related to peak burial, and 184 to 213 ∘C for veins associated with late-stage strike-slip faulting. In contrast, the overlying Hawasina nappes have not been heated above 130–170 ∘C, as witnessed by only partial resetting of the zircon thermochronometer.
In combination with independently determined temperatures from solid bitumen reflectance, we infer that the fluid inclusions of peak-burial-related veins formed at minimum pressures of 225–285 MPa. This implies that the rocks of the future Jebel Akhdar Dome were buried under 8–10 km of ophiolite on top of 2 km of sedimentary nappes, in agreement with thermal maturity data from solid bitumen reflectance and Raman spectroscopy.
Rapid burial of the passive margin under the ophiolite results in sub-lithostatic pore pressures, as indicated by veins formed in dilatant fractures in the carbonates. We infer that overpressure is induced by rapid burial under the ophiolite. Tilting of the carbonate platform in combination with overpressure in the passive margin caused fluid migration towards the south in front of the advancing nappes.
Exhumation of the Jebel Akhdar, as indicated by our zircon data and in agreement with existing work on the tectonic evolution, started as early as the Late Cretaceous to early Cenozoic, linked with extension above a major listric shear zone with top-to-NNE shear sense. In a second exhumation phase the carbonate platform and obducted nappes of the Jebel Akhdar Dome cooled together below ca. 170 ∘C between 50 and 40 Ma before the final stage of anticline formation.
The Permian–Mesozoic platform sediments of north Oman (Fig. 1; e.g., Beurrier et al., 1986; Glennie et al., 1974; Lippard et al., 1982) with hydrocarbon accumulations in the southern foreland of the Jebel Akhdar Dome (Figs. 1 and 2) are overlain by the Semail Ophiolite nappe complex, the largest and best-preserved ophiolite on Earth. Limited tectonic extension after obduction, followed by uplift, folding, and deep erosion, and the present-day arid climate formed exceptional exposures in three tectonic windows and in the foreland fold-and-thrust belt of the Oman mountains (Fig. 1). The structural and tectonic evolution of the Oman mountains has been one main focus of our group in the last 15 years (e.g., Arndt et al., 2014; Gomez-Rivas et al., 2014; Grobe et al., 2016, 2018; Hilgers et al., 2006; Holland et al., 2009b; Virgo et al., 2013a, b) and was investigated in many other studies focusing on tectonic history (Breton et al., 2004; Cooper et al., 2014; Glennie et al., 1973, 1974; Grobe et al., 2018; Loosveld et al., 1996; Searle, 2007), stratigraphic sequences (Van Buchem et al., 2002; Grelaud et al., 2006; Homewood et al., 2008), geodynamic modeling (Duretz et al., 2015), hydrocarbon source rocks (Van Buchem et al., 1996; Philip et al., 1995; Scott, 1990), and reservoir rocks (Arndt et al., 2014; De Keijzer et al., 2007; Koehrer et al., 2011; Virgo et al., 2013b). Less well known is the temperature and pressure evolution of the sub-ophiolite passive margin units and the subsequent cooling history of the Jebel Akhdar (Aldega et al., 2017; Grobe et al., 2018; Hansman et al., 2017; Poupeau et al., 1998; Saddiqi et al., 2006). This information is vital for our understanding of the time–temperature history of overthrusted margins and would allow us to further constrain obduction dynamics and forebulge migration. Combining peak temperature evolution with cooling ages links the burial history with phases of orogeny.
In other orogens, peak temperatures related to nappe emplacement were reconstructed by analyzing the thermal maturity of finely dispersed organic material (e.g., Teichmüller and Teichmüller, 1986; Zagros: Mashhadi et al., 2015; Holy Cross Mountain: Schito et al., 2017; eastern Alps: Lünsdorf et al., 2012; southern Alps: Rantitsch and Rainer, 2003; Apennines: Reutter et al., 1988). However, the number of studies of thermal and pressure effects on overthrust sedimentary basins is limited and modeling approaches to reconstruct such large-scale overthrusts are increasing but still few (e.g., Aldega et al., 2018; Deville and Sassi, 2006; Ferreiro Mählmann, 2001; Jirman et al., 2018; Oxburgh and Turcotte, 1974; Roure et al., 2010; Schito et al., 2018; Wygrala, 1989). In these studies, a main difficulty is to differentiate between the temperature history of overthrusting and overprinting by later phases of orogeny. In the Oman mountains, peak temperatures reached by obduction have not been overprinted. The whole Permian–Mesozoic sequence of the carbonate platform below the ophiolite is well exposed, providing outcrop to study the pressure and temperature history of this rapidly buried passive margin sequence.
In this paper we present new thermal maturity, thermochronology, and fluid-inclusion data and integrate them into a numerical basin model of the pressure–temperature evolution along a transect extending from the undeformed passive margin sequence in the south to the Batinah coast in the north (Fig. 2). This helps to constrain temperature and pressure conditions of maximum burial and the time of dome formation and exhumation linked to the structural and tectonic evolution of the area (Grobe et al., 2018). Our results for the Oman mountains can be used to understand more deformed orogens and shed light on fluid migration in the early stages of orogeny and exhumation related to orogenic collapse.
2.1 Tectonic setting
Along the northeastern coast of Arabia, the NW–SE-oriented Oman mountains form a more than 400 km long anticlinal orogen (Fig. 1). The mountain belt consists of allochthonous sedimentary and ophiolitic nappes thrust onto a Permian–Mesozoic passive continental margin (Breton et al., 2004; Glennie et al., 1973; Loosveld et al., 1996; Searle and Cox, 2002).
This continental margin was formed during opening of the Neotethyan Ocean (Loosveld et al., 1996) and the formation of the Permian–Mesozoic Hawasina basin (Béchennec et al., 1988; Bernoulli et al., 1990). The initiation of subsea thrusting of the future Semail Ophiolite onto the Arabian plate at 97-92 Ma is recorded by U–Pb geochronology (Rioux et al., 2013, 2016; Warren et al., 2005) and 40Ar∕39Ar dating of the metamorphic sole (Hacker et al., 1996). The advancing ophiolite caused a flexural forebulge that moved southwestwards through the passive margin during the Upper Cretaceous (Robertson, 1987). Forebulge migration induced up to 1100 m of uplift of the Permian–Mesozoic Arabian platform and erosion of the Cretaceous platform sediments (Searle, 2007), causing the Wasia–Aruma break (Robertson, 1987).
During this convergence, parts of the Hawasina ocean sediments and volcanic units became detached and accreted in front of and beneath the ophiolite nappe (Béchennec et al., 1988, 1990; Glennie et al., 1974; Searle et al., 2003; Warburton et al., 1990). Palinspastic reconstructions of the Hawasina nappes locate the position of the initial ophiolite thrusting 300-400 km offshore of the Arabian coast (Béchennec et al., 1988; Glennie et al., 1974).
In the carbonate platform, burial under the advancing nappes led to the generation of overpressure cells and the formation of three crack–seal calcite vein generations (Gomez-Rivas et al., 2014; Grobe et al., 2018; Hilgers et al., 2006; Holland et al., 2009b; Virgo, 2015). The highest grades of metamorphism are recorded by eclogites exposed in As Sifah (Fig. 1a) at ca. 79 Ma (Warren et al., 2003).
The sedimentary record on the Batinah coast and the foreland, as well as laterite formation on top of the ophiolite, suggests subaerial exposure and a slowdown or stopped obduction before lower marine conditions were restored in the Maastrichtian (Coleman, 1981; Forbes et al., 2010; Nolan et al., 1990). This slowdown might relate to the formation of the Makran subduction zone (Agard et al., 2005; Grobe et al., 2018; Hassanzadeh and Wernicke, 2016; Jacobs et al., 2015; Mouthereau, 2011) preserving the early stage of the obduction orogen in Oman.
In the Jebel Akhdar, post-obduction extension took place along ductile top-to-NNE shear zones at 64±4 Ma (Grobe et al., 2018; Hansman et al., 2018), followed by NW–SE-striking normal fault systems (Al-Wardi and Butler, 2007; Fournier et al., 2006; Grobe et al., 2018; Hanna, 1990; Hilgers et al., 2006; Holland et al., 2009a, b; Loosveld et al., 1996; Mattern and Scharf, 2018; Virgo, 2015).
Renewed Arabia–Eurasia convergence during the Cenozoic formed the three dome structures. The timing of the formation and exhumation of the Jebel Akhdar Dome is still debated. Stratigraphic arguments for a Late Cretaceous doming are Maastrichtian rocks unconformably deposited on Hawasina (Bernoulli et al., 1990; Fournier et al., 2006; Hanna, 1990; Nolan et al., 1990), while inclined Miocene strata at the northern fringes of the dome point to a Miocene doming (Glennie et al., 1973). Consequently, some models suggest a two-phased exhumation in the Cretaceous and Miocene (Grobe et al., 2018; Searle, 1985, 2007), in agreement with thermochronological constraints and an interpreted two-stage cooling with possible reheating in the late Miocene (Poupeau et al., 1998; Saddiqi et al., 2006). More recent studies, however, have shown that the data can also be explained by a cooling-only scenario with exhumation in the Eocene (Hansman et al., 2017). This is in agreement with recent structural observations suggesting early dome formation and later amplification of the structure (Grobe et al., 2018).
2.2 Stratigraphic sequence
Sediments in the Jebel Akhdar consist of a pre-Permian sequence (Autochthon A, Fig. 3) unconformably overlain by a Permian–Mesozoic sequence (Autochthon B, Fig. 3; Beurrier et al., 1986; Breton et al., 2004; Glennie et al., 1974; Rabu et al., 1990). During the Late Cretaceous, Hawasina nappes and the Semail Ophiolite were emplaced onto the passive margin, and neo-autochthonous rocks of Cenozoic age were deposited on top of the ophiolite after obduction (Béchennec et al., 1988; Forbes et al., 2010; Loosveld et al., 1996).
Autochthon A deposits are exposed in the Jebel Akhdar window down to the Mistal Fm. (Beurrier et al., 1986). Black limestones of the Hajir Fm., mudstone-rich carbonate beds of the Mu'aydin Fm., and limestone and dolostones of the Kharus Fm. conformably overlie the Mistal Fm. (Beurrier et al., 1986; Glennie et al., 1974). Platform breakup is recorded by laminated cherts and volcanoclastics of the Fara Fm. (Beurrier et al., 1986) followed by an unconformity representing a gap from Cambrian to Permian times (Loosveld et al., 1996). After the establishment of the Neotethyan Ocean during the Permian, northern Oman returned to stable passive margin conditions and the carbonate platform of the Autochthon B developed, with the Akhdar Group at its base (Koehrer et al., 2010; Pöppelreiter et al., 2011). This is unconformably overlain by limestones with clastic interlayers of the Jurassic Sahtan Group (Beurrier et al., 1986; Pratt et al., 1990). Limestones with marly, frequently organic-rich intercalations of the Cretaceous Kahmah (Al Habsi et al., 2014; Vahrenkamp, 2010) and Wasia groups (Grelaud et al., 2006; Homewood et al., 2008; Philip et al., 1995) form the youngest platform sediments (Robertson, 1987; Warburton et al., 1990).
The obduction-related moving forebulge and associated uplift ended passive margin deposition and eroded the topmost Wasia Group (Natih Fm.) in the Jebel Akdhar (Fig. 3) and deeper in the Saih Hatat region. Deposition in the foredeep basins in front of and behind the forebulge was dominated by the syn- and post-orogenic, conglomerate-rich sediments of the Muti Fm. and Aruma Group (Beurrier et al., 1986; Robertson, 1987). Towards the south, in the Adam Foothills, this laterally grades to calcareous foreland sediments of the Fiqa Fm. (Forbes et al., 2010; Robertson, 1987; Warburton et al., 1990).
Hawasina sediments accreted in front of and beneath the ophiolite represent marine slope and basin facies time equivalent to the Autochthon B (Béchennec et al., 1990). They are defined as four age-equivalent groups (Hamrat Duru, Al Aridh, Kawr, and Umar) representing carbonatic turbidite deposits (Hamrat Duru Group), radiolarian cherts and platform carbonates (Al Aridh Group), platform carbonates (Kawr Group), and interbedded carbonates and volcanics (Umar Group, Béchennec et al., 1990). After obduction of oceanic crust onto the passive margin, neo-autochthonous evaporites and carbonates of the Paleocene to Eocene Hadhramaut Gp. and bivalve-rich dolomites and limestones of the Oligo- to Pliocene Fars Group were deposited south of the mountains (Béchennec et al., 1990; Forbes et al., 2010). Paleogeographic reconstructions show that the Oman mountains had high relief after obduction, followed by a low-relief landscape until the early Eocene (Nolan et al., 1990). In the middle Eocene marine transgression caused widespread deposition of limestones, as witnessed by the Seeb and Ruwaydah formations (Nolan et al., 1990). Post-Eocene times show renewed relief development and continued uplift until recent times (Glennie et al., 1974; Searle, 2007).
2.3 Previous paleothermal data of the autochthon
Only limited paleotemperature data are available from the carbonate platform (Fink et al., 2015; Grobe et al., 2016; Holland et al., 2009b; Stenhouse, 2014). Peak burial temperatures of 226–239 ∘C for the top of the platform were measured using solid bitumen reflectance (also referred to as pyrobitumen reflectance) and Raman spectroscopy of carbonaceous material (RSCM) in the Jebel Akhdar indicate peak burial temperatures of 266 to 300 ∘C for the entire platform (Grobe et al., 2016; Table 1). Temperature estimates based on RSCM and solid bitumen reflectance (Grobe et al., 2016) yielded similar temperatures for the southern flank of 248–280 ∘C for the Nahr Umr, 226–239 ∘C for the Natih B, and 172–206 ∘C for the Muti (Table 1, Fig. 3).
Vein crystallization temperatures of 166–205 ∘C at the top of the Natih A (near Al Hamra) were measured by quartz–calcite thermometry in veins formed during ophiolite-induced burial (Gen. III of Grobe et al., 2018) and approximately 255 ∘C for veins associated with a later normal fault network (Gen. V of Grobe et al., 2018; Stenhouse, 2014). Fluid inclusions (FIs) of bedding-parallel pinch-and-swell veins (top-to-NNE shear after peak burial, Gen. IV of Grobe et al., 2018) show uncorrected minimum trapping temperatures of 134–221 ∘C in the lower beds of the Sahtan Group at Wadi Nakhr (Holland et al., 2009b). Reflectance measurements of solid-bitumen-containing veins in the Wadi Ghul (Gen. I of Grobe et al., 2018), which are interpreted to be associated with fluid mobilization during forebulge migration, show maximum temperatures of 230 ∘C (Fink et al., 2015).
Vitrinite reflectance data from Mozafari et al. (2015) show temperatures of ca. 140 ∘C for the Natih B in the Jebel Qusaybah, Adam Foothills, an area not overthrust by the ophiolite complex.
2.4 Temperature evolution of the Semail Ophiolite nappe–allochthon
Initial intra-oceanic ophiolite thrusting and associated metamorphism at its sole took place at peak temperatures of 840±70 ∘C at 97–92 Ma measured at several locations in the Oman mountains (Gnos and Peters, 1993; Hacker and Mosenfelder, 1996; Rioux et al., 2013; Searle and Cox, 2002; Warren et al., 2003). At 90–85 Ma the base of the ophiolite cooled to 350±50 ∘C (white mica Ar∕Ar dating; Gnos and Peters, 1993). At around 80 Ma the deepest burial of the Oman margin beneath the ophiolite was reached (Hacker and Mosenfelder, 1996; Warren et al., 2005) with temperatures in the metamorphic sole below 300 ∘C (Le Metour et al., 1990; Saddiqi et al., 2006). A lithospheric-scale thermo-mechanical model of the thrusting in northwestern Oman includes a thermal anomaly ca. 100 km northwest offshore of the Arabian margin to initiate subsea thrusting (Duretz et al., 2015).
2.5 Petroleum system elements
Several petroleum systems developed in the carbonate platform of northern Oman with important source rock horizons in the Natih Fm. (Members B and E). Both members contain Type I–II kerogen with total organic carbon contents up to 15 % in the Natih B and up to 5 % in the Natih E (Terken, 1999). Source rock maturity is restored based on biomarker analysis to ca. 0.7 % VR within the Fahud reservoir and ca. 0.9 % VR in the Natih reservoir (Terken, 1999). In the southern mountain foreland Natih oil generation started in the middle Cretaceous and continues until the present (Terken, 1999). Ophiolite obduction in the Jebel Akhdar area of northern Oman led to overmature Natih source rocks (Grobe et al., 2016). The Natih is classified as a supercharged, laterally drained, foreland petroleum system (Terken et al., 2001). However, the thermal impact of the moving forebulge and the importance of tectonic processes for fluid migration below and in front of the obduction orogen are not clear. At least three different generations of solid bitumen particles in veins and source rocks on the southern slope of the Jebel Akhdar suggest pulses of hydrocarbon generation and migration in front of the Oman mountains (Fink et al., 2015; Grobe et al., 2016). In central Oman, Shu'aiba and Tuwaiq oils are produced from the Kahmah and Sahtan Group reservoirs, sealed by argillaceous shales of the Nahr Umr Fm. (Terken et al., 2001). All these units are well exposed in the Oman mountains.
3.1 Raman spectroscopy of carbonaceous material
To determine levels of thermal maturity, over 100 dark, unweathered, and organic-rich samples were taken from different stratigraphic units in the Jebel Akhdar (Sahtan Group, Kharaib Fm., Shu'aiba Fm., Nahr Umr Fm., Natih Fm., Muti Fm.; Fig. 3). Based on total organic carbon (TOC) content as determined by Grobe et al. (2016), 13 samples were selected for thermal maturity analysis on surfaces cut perpendicular to bedding. Results were used to calibrate the peak burial temperatures of the numerical basin models. The organic particles lack sufficient size or surface quality for reflectance measurements and are therefore investigated by confocal Raman spectroscopy of carbonaceous material. The technique measures vibrational energies of chemical bonds, which change during temperature-induced reorganization of amorphous carbonaceous material (kerogen) to graphite (e.g., Aoya et al., 2010; Beyssac et al., 2002; Kouketsu et al., 2014; Mair et al., 2018). Measurements were conducted at the Geoscience Center, Göttingen, on a Horiba Jobin Yvon HR800 UV spectrometer attached to an Olympus BX-41 microscope and a 100× objective. A high-power diode laser with a wavelength of 488 nm and an output power of 50 mW was installed and a D1 filter avoided sample alteration by heating. Each spectral window (center at 1399.82 cm−1, grid of 600 lines per mm) was measured 5 to 10 times for 2 to 10 s with a Peltier CCD detector at activated intensity correction. For quality control, the 520.4 cm−1 line of a Si wafer was measured every 30 min without observable drift of the measurements. To transform the measured data into VRr values, the scaled total area (STA) approach of Lünsdorf (2016) was applied with the equation of Grobe et al. (2016):
Absolute errors of the applied calibration are of the order of ±40 ∘C. Based on comparing neighboring samples (Grobe et al., 2016), we can resolve the relative differences down to ±30 ∘C, which also represents the residual error interpreted to relate to within-sample heterogeneity (Lünsdorf et al., 2017; Nibourel et al., 2018).
3.2 Fluid-inclusion thermometry
Doubly polished wafers (ca. 200 µm thick) of four vein samples (FI-N1, FI-N2, FI-M1, FI-M2) have been prepared according to the procedure described by Muchez et al. (1994). Fluid-inclusion (FI) petrography and microthermometry were performed to analyze the temperature–pressure conditions and fluid salinity. FIs represent paleofluids accidentally trapped in a crystalline or amorphous solid during crystallization, lithification, or both (Diamond, 2003). If unaffected by later changes, trapping pressure and temperature are given by the homogenization temperature (Barker and Goldstein, 1990). Based on the time of trapping primary (mineral growth), secondary (fracture-related) and pseudosecondary inclusions are distinguished (Barker and Goldstein, 1990; Diamond, 2003; Goldstein, 2001; Van Den Kerkhof and Hein, 2001).
Two calcite vein samples of the Natih Fm. (FI-N1 and 2, locations in Fig. 4) represent conditions related to early burial (FI-N2, structural generation I of Grobe et al., 2018) and burial beneath the ophiolite (FI-N1, structural generation III of Grobe et al., 2018). Two quartz-rich calcite veins of the Muti Fm. (FI-M1 and 2, locations Fig. 4) are related to late NE–SW-striking strike-slip faults (generation IX of Grobe et al., 2018). FI assemblages were defined and fluid inclusions measured with a Linkam THMSG600 thermostage (accuracy ±0.1 ∘C) attached to an Olympus BX60 microscope at the KU Leuven, Belgium. Calibration was performed using CO2, H2O–NaCl, H2O–KCl, and H2O standards. Homogenization temperatures (Th) were measured prior to temperatures of complete freezing (Tf), first melt (Tfm), and complete melting of ice (Tm(ice)) to avoid stretching or leakage due to the volume increase during ice formation. All measured temperatures were recorded during heating, except for the freezing temperature (Tf). Pressure corrections of Th were conducted with the program FLINCOR (Brown, 1989) for 280 and 340 MPa, assuming 8 to 10 km of ophiolite overburden (see model results, ρ=ca. 3070 kg m−3) and 2 km of Hawasina nappes (ρ=ca. 2450 kg m−3), and for 45 MPa, assuming 2 km of sedimentary overburden (Al-Lazki et al., 2002; Grobe et al., 2016). Fluid salinities were calculated from the Tm(ice) values considering an H2O–NaCl composition (Bodnar, 1993), which is based on the Tfm values.
Zircon (ZHe) dating allows us to reconstruct the thermal history of the topmost few kilometers of the Earth's crust. Helium retention in less metamict zircon crystals is sensitive in the temperature range between ca. 130 and 170 ∘C, i.e., the zircon partial retention zone (PRZ; Reiners, 2005). A total of 11 rocks sampled above (Muti Fm., Matbat Fm. of the Hamrat Duru Group, and Trondjemite of the Semail nappes), below (Mistal Fm., Muaydin Fm., Fara Fm.), and within (Sahtan Gp.) the carbonate platform were selected for ZHe dating. Zircon crystals were released using high-voltage pulse crushing (http://www.selfrag.com) and concentrated by standard mineral separation processes (drying, dry-sieving, magnetic and heavy liquid separation). Three to eight clear, intact, euhedral single crystals were selected per sample and transferred into platinum microcapsules. They were degassed under high vacuum by heating with an infrared diode and extracted-gas-purified using a SAES Ti–Zr getter at 450 ∘C. Helium was analyzed with a Hiden triple-filter quadrupole mass spectrometer. Degassed zircons were subsequently dissolved in pressurized teflon bombs and spiked, and then U, Th, and Sm were measured with a Perkin Elmer Elan DRC II ICP-MS equipped with an APEX micro-flow nebulizer.
Time–temperature histories were reconstructed using the HeFTy 1.8.3 software package (Ketcham, 2005) applying the kinetic zircon properties of Guenther et al. (2013). For samples with reset zircons the only constraint used was a minimum temperature above 200 ∘C between deposition and the calculated ZHe age. Thermal modeling was conducted until 100 statistically good time–temperature paths were achieved (goodness of fit: 0.5, value for acceptable fit: 0.05). In cases in which this was not possible, at least 10 000 independent paths were calculated.
3.4 Numerical basin modeling
Structural evolution was palinspastically reconstructed starting from the present-day profile using Move 2D (2016.1, Midland Valley Exploration). Geometries and relative ages of the structures were supplemented with subsurface data (Al-Lazki et al., 2002; Filbrandt et al., 2006; Searle et al., 2004; Warburton et al., 1990). The reconstruction workflow is based on restoring the pre-deformation layer continuity as follows: (1) faulted layers in the southern foreland were restored, and (2) doming was retro-deformed by vertical simple shear before (3) normal faults in the Jebel Akhdar were restored. This sequence is based on our tectonic model (Grobe et al., 2018). The resulting geometries were used as pre-thrusting input geometries for 2-D PetroMod 2014.1 (Schlumberger) basin modeling, enabling thermal maturity reconstruction for vitrinite reflectance values of 0.3 % to 4.7 % by the use of the EASY % Ro approach (Sweeney and Burnham, 1990). The numerical basin model is based on a conceptional definition of events. Based on this sequence of events (sedimentation, erosion, hiatus) a forward, event-stepping modeling was performed, starting with the deposition of the oldest layer. Subsequent deposition and burial is leading to differential compaction of the single rock units. For each event, lithologies and related petrophysical rock properties were assigned (Figs. S1, S2 in the Supplement).
For our conceptual model the following sequence of events was implemented (Fig. 3): (1) passive margin carbonate sedimentation from Permian until late Cenomanian times (Forbes et al., 2010; Loosveld et al., 1996) interrupted by a short erosional period at the Triassic–Jurassic boundary (Koehrer et al., 2010; Loosveld et al., 1996); (2) a moving forebulge associated with a paleo-water depth increase in its foredeep and erosion of the top of the carbonate platform in the north of the transect (Robertson, 1987); (3) the emplacement of allochthonous sedimentary nappes; and (4) subsequent stepwise obduction of the ophiolite with deepest burial reached at ca. 79 Ma (Warren et al., 2005). Modeling ophiolite obduction as rapid emplacement accounts for burial-related heat effects in the carbonate platform underneath but does not allow us to fully restore the temperatures within the ophiolitic or sedimentary nappes. The area of the Adam Foothills, represented in the transect by Jebel Qusaybah, is a relic of the moving forebulge not overthrust by allochthonous units – this was used to calibrate the burial depth of the foredeep at this point in the transect. The area to the south of the Adam Foothills is unaffected by foredeep sedimentation, but also lacks thermal calibration data. Absolute ages, thicknesses, lithologies, and related petrophysical properties as well as source rock properties were associated according to the results of our own field mapping and the compiled data from Forbes et al. (2010; Fig. S1).
Thermal boundary conditions of the model have been defined for each time step by the basal heat flow (HF) and the sediment–water interface temperature (SWIT), representing the upper thermal boundary (Fig. S3). To account for active margin tectonics and uplift and exhumation of the Jebel Akhdar, we assume an increase in basal heat flow since the Late Cretaceous. The resulting heat flow trend (Fig. S3, Terken et al., 2001; Visser, 1991) has been assigned to the entire transect and was tested in the sensitivity analysis. Paleo-surface temperatures were estimated based on Oman's paleo-latitude (after Wygrala, 1989) corrected by the effect of the paleo-water depth (PWD) derived from the facies record (Van Buchem et al., 2002; Immenhauser et al., 1999; Immenhauser and Scott, 2002; Koehrer et al., 2010; Pratt et al., 1990; Robertson, 1987). This assumes that a possible heat source from the ophiolite itself does not significantly affect the temperature evolution of the top of the carbonate platform (see Discussion section).
This setup has been iterated until modeling results fit the thermal calibration data (Table 1). From VRr calculations peak burial temperatures were determined following the approach of Barker and Pawlewicz (1994). For calibration of the numerical basin models, data were supplemented by thermal maturity and peak burial temperature data from 63 Natih B source rock samples taken around the Jebel Akhdar Dome (Grobe et al., 2016) and data from the Adam Foothills on Jebel Qusaybah (Mozafari et al., 2015).
Main modeling uncertainties derive from uncertainty in the thickness of the paleo-overburden (Muti Fm., Ophiolite, Hawasina nappes) and uncertainty of the paleo-basal heat flow. Present-day heat flow was calibrated by data and borehole temperatures from Visser (1991) and Rolandone et al. (2013), and peak burial temperatures were determined by Raman spectroscopy and solid bitumen reflectance data (Table 1). From surface samples and their position in the stratigraphic column, various pseudo-wells were created (e.g., Nöth et al., 2001) and used as control points for the 2-D model (Fig. 2). The model was used for sensitivity analyses of different input parameters.
4.1 Thermal maturity and host rock burial temperatures
New Raman spectroscopy data on the northern flank are shown in Table 1 and give scaled total areas of 78–172. This corresponds to peak temperatures of 270–300 ∘C in the Shu'aiba Fm., 268–305 ∘C in the Kahmah Group, 283–286 ∘C in the Sahtan Group, 270–288 ∘C in the Nahr Umr Fm., and ca. 266 ∘C at the base of the Natih Fm. Based on the calculation to VRr and temperature an absolute error of ±30 ∘C has to be considered for the single values. Thermal maturity data on the Natih Fm. show solid bitumen reflectances of 2.95 %–3.72 % for the southern flank of the Jebel Akhdar (Fink et al., 2015; Grobe et al., 2016), 3.32 % BR for the northern flank (Grobe et al., 2016), and a single measurement of 1.1 % VR for the Jebel Qusaybah (Mozafari et al., 2015).
Calculated peak temperatures for the autochthonous Cretaceous deposits in the Jebel Akhdar range between 225 and 305 ∘C (±30 ∘C, error of the calibration), with two Jurassic samples at 283 and 286 ∘C (±30 ∘C). Temperatures are generally higher on the northern flank (gray boxes, Fig. 3) of the Jebel Akhdar and slightly increase with stratigraphy in the autochthons. Samples from the Muti Fm. (178–208±30 ∘C) and the Hawasina nappes (193–213±30 ∘C) show lower temperatures compared to the autochthons. A single sample from the Jebel Qusaybah reflects peak temperatures of ca. 140 ∘C (Table 1) in an area that was not overthrusted by nappes but buried in the related moving forebulge.
Results of the ZHe dating are shown in Figs. 3 and 4; time–temperature paths modeled with HeFTy are included in the Supplement (Figs. S4 and S5). Samples from the carbonate platform (stratigraphically older than the Muti Fm.) have been entirely reset after deposition, as witnessed by Neogene apparent ages. Similarly, cooling ages from the center of the Jebel Akhdar Dome fall in the range of 48.7±1.8 to 39.8±3.0 Ma (Table 2, Fig. 4). Sample T4, collected in the Muti Fm., yields an apparent mean age of 93.8±6.9 Ma and samples T5 and T7 of the Hawasina nappes collected at the northern and the southern slope of the dome show two grain age clusters of Ma and Ma, respectively. In sample T5, an additional single grain age of 172.9±14.9 Ma was obtained.
These ages indicate a large-scale cooling signal that affects the entire Jebel Akhdar area; the ZHe age pattern and 1-D thermal models indicate a phase of rapid cooling below 170 ∘C in the early Cenozoic (58.9±7.0 and 39.8±3.0 Ma). The range of modeled cooling paths outline maximum cooling rates of 2–8 . This is followed by slower cooling until the present day.
Data from the Muti Fm. and the Hawasina units differ partly from this trend: the apparent ZHe ages of clasts in the Muti sample T4 (mean: 93.8±6.9 Ma) are as old as its respective stratigraphic age (Robertson, 1987). Even though all ages reproduce within error, this indicates partial reset of the ZHe system, as post-depositional reheating above closure temperature would result in younger ages. Samples from the lower Hawasina nappes contain two grain age clusters. Older ages coincide with higher uranium concentrations, suggesting that only the younger ages represent thermally reset zircons. We note that the older ZHe ages of 110–95 Ma coincide with the timing of forebulge migration through the area, as independently determined in the stratigraphic record by the Wasia–Aruma break (Fig. 3). This may be either pure coincidence due to partial resetting of an older grain age population, or it may be a grain age population with higher closure temperature witnessing exhumation. We discuss the reasons for different resetting temperatures below. However, partial reset of ZHe ages suggests that the Hawasina samples have not experienced temperatures exceeding the partial retention zone (PRZ) of 130–170 ∘C.
A sample from an intrusive body of the Semail Ophiolite yields ZHe ages of 53.7±1.2 Ma (T6) with a modeled cooling path gradually decreasing into the PRZ until ca. 55 Ma. This time interval of passing the PRZ is comparable to the Hawasina nappe samples beneath the ophiolite but occurs slightly earlier than cooling of the autochthons. Nevertheless, Semail Ophiolite, Hawasina nappes, and the autochthonous margin sequence were affected by the same cooling event that was possibly initiated by exhumation of the Jebel Akhdar Dome.
4.3 Fluid inclusions
The Muti vein samples FI-M1 and M2 of the southern Jebel Akhdar show evidence of crack and seal processes (youngest parts in the center of the vein; Ma-2010-11b and 14a of Arndt, 2015) with blocky quartz grains that contain two kinds of roundish primary FIs with sizes of 3–20 µm. They are mainly aligned along dark zones and are interpreted as growth zones or form bright clusters in the central part of the crystals. A third set of fluid inclusions (FIs) appears in large, grain-crosscutting trails interpreted to be of secondary origin. Calcite crystals within the Natih veins contain bright FIs with sizes of 2–20 µm and are edgy, often rectangular, or trapezoidal in shape. Identified primary FIs are aligned parallel to crystal growth zones.
All measured FIs are two-phase liquid–vapor inclusions with ice as the last phase to melt. The Muti samples show Tfm(ice) between and ∘C and Tm(ice) at to ∘C, and the Natih sample has Tfm of to ∘C and Tm(ice) of to ∘C (Table 3). The first melting temperatures of all inclusions correspond to an H2O–NaCl system, and complete melting temperatures of ice indicate salinities similar to seawater (3.0±0.5 wt. % to 3.5±0.3 wt. % NaCl eq., Muti Fm.; Fig. S6) or 3 times higher (10.3±0.3 wt. % to 12.5±2.0 wt. % NaCl eq., Natih Fm.; Fig. S6).
Primary inclusions in quartz crystals from the Muti Fm. show minimum trapping temperatures of 161±3 to 166±7 ∘C (Table 3; FI-M2 and middle of FI-M1) with a second primary population of 189±3 ∘C (sides of vein FI-M1). Th values of secondary inclusions in FI-M1 are above 200 ∘C. In sample FI-M2, two generations of secondary inclusions were observed, both reflecting lower Th than the primary inclusions. No hints of necking down, leakage, or stretching were observed at the measured inclusions and over 90 % of the measured FIs in one assemblage are in the range of 10–15 ∘C, representing a good quality of the measurements (Goldstein, 2001).
Samples FI-N1 and N2 from the Natih Fm. in the southern Jebel Akhdar (Fig. 4) contain primary inclusions hosted by calcite crystals giving Th of 80±4, 90±5 and 114±7 ∘C (Table 3). The latter population is often characterized by elongated, possibly stretched FI and is not considered for further interpretations. Assuming vein formation during burial (Grobe et al., 2018; Hilgers et al., 2006; Holland et al., 2009b; Virgo, 2015) under 8 to 10 km of ophiolite, including partially serpentinized peridotite and 2 km of Hawasina nappes, results were pressure-corrected for 280 and 340 MPa, leading to corrected homogenization temperatures of 235±5 and 266±5 ∘C (FI-N1) and 225±4 and 256±4 ∘C (FI-N2; Table 3). Signs of strong deformation such as twinning or cleavage were not observed in the measured inclusions; secondary inclusions were present but not measured.
These temperatures represent minimum trapping conditions of a paleofluid and do not necessarily represent burial temperatures of the host rock. It should be noted that the analyzed Natih veins formed bedding confined (Grobe et al., 2018; Holland et al., 2009b; Virgo, 2015) and show host-rock-buffered carbonate isotope signatures (Arndt et al., 2014; Hilgers et al., 2006). This corroborates the idea that the analyzed veins were in thermal equilibrium with their host rocks.
FI microthermometry of late strike-slip veins in the Muti Fm. are interpreted to have formed after dome formation (Grobe et al., 2018; Virgo, 2015) at an assumed minimum depth of 2 km (preserved allochthonous thickness). A pressure correction for the related 45 MPa corresponds to minimum fluid trapping temperatures of 184±3 ∘C (FI-M2) and 213±3 ∘C (FI-M1) with a later phase of primary inclusions outlining 189±7 ∘C and even cooler secondary inclusions of 138±12 to 172±2 ∘C (FI-M1 and M2; Table 3). These cooler fluid temperatures can be explained by further exhumation of the Jebel Akhdar and hence cooling of the fluid reservoir during crack–seal vein formation. Isotope studies on the vein calcite do not support an open system with fluid exchange (Stenhouse, 2014; Virgo and Arndt, 2010); hence, we interpret the formation of strike-slip-related veins as having formed during exhumation following peak burial.
Based on the assumption that fluid and host rock were in thermal equilibrium, we can use maturity data in combination with fluid-inclusion data to estimate the pressure at vein formation. Peak temperatures of the Sahtan Group revealed by RSCM reached 283±9 to 286±6 ∘C (Table 1, Fig. 5 red line) and enable us to solve the pressure–temperature couples of FIs measured in Sahtan veins formed at deepest burial by Holland et al. (2009b, black line). This results in minimum trapping pressures of 254±30 MPa at times of vein formation (Fig. 5 blue line), which correspond to times close to or at deepest burial of the carbonate platform.
4.4 Basin modeling
Numerical basin modeling integrates all data and tests the individual interpretations in the thermal and geodynamic framework. Deepest burial was constrained with thermal maturity data and exhumation with thermochronological data. In the following we present our best-fit model, considering a mixed ophiolite lithology (Searle and Cox, 2002) consisting of strongly serpentinized peridotites. Then, the sensitivity of important results to changes in relevant input parameters are discussed.
Modeled evolution of the transect over time is given in Figs. 6 and 7, showing (a) final deposition of the Autochthon B, (b) erosion of the Natih Fm. in the north by a moving foredeep (no erosion in S, full erosion in N), (c) emplacement of 1400 m of the Hawasina nappes, and (d)–(e) ophiolite obduction reconstructed by rapid, stepwise sedimentation. After maximum burial beneath the ophiolite complex at ca. 80 Ma (Warren et al., 2005) exhumation is assumed to start slightly prior to 55 Ma (Saddiqi et al., 2006) with a rapid phase of cooling below ca. 200 ∘C at 55 Ma, leading to lower temperatures in the Jebel Akhdar region. 1-D burial plots of two pseudo-wells created from point data in Wadi Nakhr and Wadi Yiqah are shown in Fig. 8.
As a model setup only presents one possible solution out of several, sensitivity analyses with varying paleo-overburden thicknesses (Figs. 9 and 10), changing degrees of serpentinization of the ophiolite, and varying basal heat flow during deepest burial (Fig. 11) are presented and discussed below.
Thermal maturity data on the Natih B at Jebel Qusaybah (1.1 % VRr), Adam Foothills, require peak temperatures of ca. 140 ∘C (Table 1). Sensitivity analyses of the overburden above the Natih Fm. show that a maximum of 4 km of sedimentary overburden (Figs. 9a and 10a) is needed to match the calibration data (Figs. 9a and 10a).
To restore the former minimum thickness of the Semail Ophiolite, the thickness of the Hawasina nappes along the transect was fixed to 2 km, as suggested by the maximum present-day thickness of the Jebel Misht exotics. To reach the required thermal conditions measured at the entrance of the Wadi Nakhr (Natih B: 2.83–3.72 % VRr, 225–260 ∘C; Grobe et al., 2016), 8–10 km of the original total thickness of strongly serpentinized ophiolite sequence are needed in addition to the 2 km of Hawasina nappes (Figs. 9b and 10b). These thicknesses are also sufficient to reach peak temperatures calculated for older stratigraphy at the northern flank of the Jebel Akhdar Dome (Shu'aiba Fm. at Wadi Yiqah: 270–295 ∘C by RSCM; Figs. 9c and 10c). Modeling results show an earlier heating and more rapid increase in maturity in the north. We associate this with the 2 Myr earlier onset of obduction and hence a longer burial of the northern carbonate platform (Wadi Yiqah) under the active ophiolite obduction compared to its southern counterpart (Béchennec et al., 1990; Cowan et al., 2014).
Another factor influencing the modeling results is related to the lithology of the overburden and its compaction. In the special case of burial under an ophiolite, serpentinization of peridotite and its impact on ophiolite density and thermal conductivity must be considered. Sensitivity analysis of ophiolite serpentinization shows the temperature and thermal maturity effects on our model (Fig. 11). A model case of ophiolite without any serpentinized peridotite (0 % case, ρophio=3133 kg m−3) would represent the largest deviation compared to our best-case model assuming complete ophiolite serpentinization (100 %-case, ρophio=3069 kg m−3). This density is based on Al-Lazki et al. (2002). Even if the upper part of the ophiolite was missing in the Jebel Akhdar area (Nicolas and Boudier, 2015), this and the field data from Searle and Cox (2002) in the Saih Hatat support strong serpentinization. A less serpentinized ophiolite means higher densities and related higher thermal conductivities of the overburden and thus lower peak temperatures in the sediments below. In the case of no serpentinization, the peak temperature of Natih B in the Wadi Nakhr would decrease by ca. 60 ∘C, resulting in a maximum thermal maturity decrease of 1.5 % VR. The best-fit model with an ophiolite thickness of 8–10 km would need an additional 3 km of overburden at 0 % serpentinization to equally match the measured thermal maturities. Additional thicknesses of 0.75 km (75 % serpentinization), 1.5 km (50 % serpentinization), and 2.25 km (25 % serpentinization) apply for lower degrees of serpentinization (compare to Fig. 9).
Results depend strongly on basal heat flow (Fig. S3). The best-fit model of 40 mW m−2 at maximum burial is typical for a passive continental margin setting. If this heat flow at peak burial were lowered to 30 mW m−2 an additional 1.2 km of ophiolitic overburden would be required to achieve a match with thermal calibration data (Fig. 11). Increased heat flow values to 50, 60, or 70 mW m−2 would result in lowering of overburden by 1.3, 2.4, and 3.5 km, respectively (Fig. 11).
Evaluating uncertainties in basin and petroleum system models is especially important for complex areas such as the Jebel Akhdar, where sedimentary rocks reached high temperatures and maturities due to deep and rapid burial. In the following, we discuss these uncertainties with respect to temperature and burial history, overpressure buildup, and induced fluid flow. For all presented basin models of the study area, the following assumptions apply: (1) decompacting the present-day lithologies does not consider rock volume lost by pressure solution. This is probably of minor importance in our study area as host-rock-buffered isotope ratios of the veins were interpreted as local sinks for nearby dissolved calcite (Arndt et al., 2014; Hilgers et al., 2006), so the overall rock volume remains approximately constant. (2) Decompaction only accounts for burial, whereas a possible tectonic compaction is neglected (Neumaier, 2015). (3) Calculated overpressure does not include a rock volume decrease due to pressure solution.
5.1 Burial history
Little is known about the very early phase of burial before 91 Ma (Figs. 6 and 7; Grobe et al., 2018). The assumptions for this period are based on hypotheses on the tectonic evolution of the passive continental margin as well as data on the thickness of sedimentary units but are not strongly constrained by geological data.
In Turonian times (Robertson, 1987) a southwestward-moving forebulge, related to plate convergence, affected northern Oman. It eroded the northeastern platform edge and migrated southwestward to the present-day position of the Adam Foothills (Robertson, 1987). Measured thermal maturities of 1.1 % VRr were used to reconstruct peak temperatures during burial in Jebel Qusaybah, Adam Foothills, to ca. 140 ∘C. Numerical basin modeling results reveal that an additional paleo-overburden of a maximum 4 km (Natih B, Qusaybah, Fig. 10) is required to reach these temperatures. The exhumation history of the Adam Foothills is not well known; our model is based on an interpreted late exhumation during the Miocene (Claringbould et al., 2013). Earlier exhumation would shorten the time span of the rock at higher temperatures (Fig. 7), leading to decreased thermal maturity and hence requiring an additional overburden to match the measured thermal maturity data. Therefore, the resulting burial of 4 to 4.5 km has to be regarded as a minimum value. South of the Adam Foothills basin geometries do not show tilting and are interpreted as not affected by the moving foredeep. Here peak burial was reached under ca. 3 km of the Fiqa, Hadhramaut, and Fars formations. This is based on the assumption that present-day burial equals deepest burial as no thermal calibration data for the area south of Jebel Qusaybah are available, which is in agreement with the interpretations of Terken (1999) and Warburton et al. (1990).
In the case of the Jebel Akhdar, peak temperatures were reached as a consequence of burial below the ophiolite (Loosveld et al., 1996; Searle et al., 2003; Searle, 2007; Warren et al., 2005). Here the sedimentary rocks reached high temperatures and maturities as shown by solid bitumen reflectance, RSCM, FT-IR, and Rock-Eval pyrolysis data (Fink et al., 2015; Grobe et al., 2016). Pre-obduction burial by sedimentation is not sufficient for such high thermal maturities, and it likewise cannot be explained by increased basal heat flow before 91 Ma or after 55 Ma. The influence of local hydrothermal effects cannot be excluded, but because the entire Jebel Akhdar reached high temperatures, short-term local events are unlikely to have been dominant. A regional thermal overprint on the passive margin sediments by warm ophiolite obduction can be excluded and is hence not accounted for in the model. Due to the at least 2 km thick imbricated Hawasina nappes between the ophiolite and the passive margin sequence, the thermal overprint did not affect the top of the carbonate platform. Limited thermal overprinting of the units underlying the ophiolite is supported by the fact that the sediments of the nappes directly below the ophiolite do not show signs of regional metamorphism in the Jebel Akhdar region (Searle, 1985). Moreover, the thermal imprint as observed by the metamorphic sole in northern Oman only affects tens of meters in the sub-thrust Hawasina nappes (Searle and Cox, 2002) and not the carbonate platform sediments below. This minor overprint is also observed in other areas (e.g., Wygrala, 1989).
To reach the measured maturity values in the Jebel Akhdar, a paleothickness of the ophiolite of the order of 8–10 km on top of 2 km of Hawasina nappes is required (Fig. 10); this corresponds to 280 to 340 MPa of lithostatic pressure, in rough agreement with the pressure reconstructed by combining fluid-inclusion data and independently determined thermal rock maturity temperatures (cf. FI results: 254±30 MPa).
Basin modeling indicates that highest temperatures were reached later than deepest burial under the ophiolite (Fig. 7), directly prior to exhumation. This difference is interpreted as the time advection needs to heat the rock. Deep burial under the ophiolite represents the only time in the basin's evolution when ductile limestone deformation was possible (Grobe et al., 2018). However, there is uncertainty concerning the exact timing of deepest burial in the Jebel Akhdar (we used 79 Ma according to U–Pb dating of eclogites in the Saih Hatat window; Warren et al., 2005), the related basal heat flow (Discussion section, Fig. S2), and the beginning of early exhumation (we used 55 Ma, as discussed below). A later exhumation would not be sufficient to match observed thermal maturities with thermometry data. The slightly higher temperatures of the model compared to thermometry data suggest that an even quicker exhumation might have taken place.
Our peak temperatures are in agreement with temperatures of ca. 200 ∘C suggested for the top of the carbonate platform by Breton et al. (2004), non-reset zircon fission tracks in the pre-Permian basement indicating peak temperatures up to 280 ∘C (Saddiqi et al., 2006), and ductile limestone conditions observed at the Jurassic–Cretaceous boundary (Grobe et al., 2018, Fig. 7). Moreover, thermal maturities in the same stratigraphic units show similar values along the transect and around the dome (Grobe et al., 2016). Hence, we assume a similar burial history for the entire Jebel Akhdar and were able to refine previous models (Grobe et al., 2016) with the larger dataset presented here. The temperatures used in our models are in contrast with recent results on mixed layers of illite–smectite and clay mineral assemblages from the Jebel Akhdar by Aldega et al. (2017), who argue for peak temperatures of 150–200 ∘C on the northern flank of the Jebel Akhdar and 120–150 ∘C on the southern flank. These values are incompatible with our solid bitumen and Raman spectroscopy data, as well as with the overmature Natih B source rock on the southern flank (data presented here and in Grobe et al., 2016). Independent data on temperatures from fluid inclusions confirm the higher temperature range. At present, there is no clear explanation for this discrepancy. However, it has been shown that the vitrinite reflectance system is more sensitive to rapid temperature changes than clay mineralogy (e.g., Hillier et al., 1995; Velde and Lanson, 1993). If burial was short enough, the clay minerals may not have time to recrystallize, possibly due to a lack of potassium, whereas vitrinite reflectance increases. Alternatively, we speculate that the clay minerals were transformed during top-to-NNE shearing, and thus their state does not show peak burial. Indeed, it has been shown that deformation associated with this early extension reaches deeply into the passive margin sequence and includes the Rayda and Shu'aiba formations (Grobe et al., 2018; Mattern and Scharf, 2018). Furthermore, Aldega et al. (2017) argue that the cooling history proposed by Grobe et al. (2016) indicates a temperature in the basement <70 ∘C during the Eocene–Oligocene, thus not accounting for thermochronological data in pre-Permian basement rocks. In fact, the calibration data we used for the basement indicate rapid cooling at 55±5 Ma (Poupeau et al., 1998; Saddiqi et al., 2006), in agreement with models of Grobe et al. (2016) and the exhumation presented in this work.
This exhumation might be a result of the ductile top-to-NNE shearing event (64±4 Ma; Hansman et al., 2018; Grobe et al., 2018). Its onset marks the exhumation of the carbonate platform after deepest burial. Related peak temperatures measured in the fluid inclusions of bedding-parallel veins were estimated to 186–221 ∘C by Holland et al. (2009b) assuming an ophiolitic overburden of 5 km (Sahtan Fm., Wadi Nakhr). If we adjust this pressure correction for higher values of 280 to 340 MPa, accounting for the 8 to 10 km of ophiolite and 2 km of sedimentary nappes elaborated here, trapping temperatures would increase to ca. 296–364 ∘C (Table 3), which are of the order of the maximum burial temperatures as deduced from organic matter maturity.
Figure 12 presents a summary burial graph integrating all presented data in a plot of the temperature evolution over time. Additional pressure data are obtained by fluid-inclusion thermometry: these data indicate paleo-fluid temperatures in the range of 225±4 ∘C (280 MPa) to 266±5 ∘C (340 MPa) during burial under the ophiolite (bedding-confined veins), ca. 296–364 ∘C at peak burial (top-to-NNE sheared veins), and 213±3 ∘C during exhumation with a later phase of primary inclusion outlining 184±3 to 189±7 ∘C (both strike-slip-related veins). Temperature decrease within the latter-formed parts of the strike-slip veins might relate to a change in fluid source or to exhumation during vein formation. In combination with our thermochronology data the second possibility appears more likely and would imply that strike-slip faults developed after ca. 55 Ma.
5.2 Exhumation history
Our new thermochronology data from the central part of the Jebel Akhdar Dome suggest cooling below the reset temperature of the ZHe thermochronometer (ca. 130–170 ∘C) between 48.7±1.8 and 39.8±3.0 Ma (Table 2, Fig. 4). The small variation in cooling ages for the different stratigraphic levels indicates rapid passage of the entire rock suite through the ZHe partial retention zone and consequently rapid exhumation of the Jebel Akhdar Dome. This Eocene cooling is in agreement with ZHe ages of pre-Permian strata from Hansman et al. (2017) ranging between 62±3 and 39±2 Ma. Apatite fission track (AFT) ages measured in the basement of the Jebel Akhdar range between 55±5 and 48±7 Ma (four samples; Poupeau et al., 1998) and between 51±8 and 32±4 Ma (Hansman et al., 2017). The temperature of resetting the AFT system (i.e., the depth of the base of the partial annealing zone) may vary depending on annealing kinetics. For different apatite crystals this temperature ranges between 100 and 120 ∘C (Carlson et al., 1999; Fitzgerald et al., 2006). Hence, these AFT ages reproduce within error with our ZHe results, despite the fact that both systems are sensitive to different temperature intervals (100–120 and 130–170 ∘C, respectively). This supports the interpretation of rapid exhumation of the Jebel Akhdar at ca. 55 Ma. Zircon fission track ages witness cooling of the Jebel Akhdar below ca. 260 ∘C between 96 and 70 Ma (Saddiqi et al., 2006). This implies slow cooling thereafter (ca. 100∘ between 70 and 55 Ma) until rapid exhumation at ca. 55 Ma. Earlier exhumation would not result in the required thermal maturities as the exposure of the rock to highest temperatures would be too short for thermal equilibration. A reheating event in the late Miocene is not required to explain the data.
Our ZHe data from the Muti Formation and the Hawasina nappes show a spread in ages between 173 and 43 Ma, i.e., partly much older than the ages observed in the stratigraphically lower units in the center of the dome.
A spread in ages is often observed and has been attributed to radiation damage density, uneven distribution of mother isotopes in the dated crystal, broken grains, and grain chemistry, among other causes (e.g., Flowers et al., 2009; Guenther et al., 2013). Several studies show that samples from sedimentary rocks are particularly prone to spread in ages (e.g., von Hagke et al., 2012; Ketcham et al., 2018; Levina et al., 2014). This is because transported grains are subject to abrasion, which influences age correction for grain geometry and may obscure the presence of inclusions within the crystal. Additionally, dated grains can originate from different sources and thus have a different chemical composition and a different pre-depositional temperature history. This may result in different reset temperatures, and consequently different grains (or grain age populations) represent different thermochronometers.
It is difficult to prove the existence of such multiple thermochronometers, as independent parameters indicative for different kinetics have not yet been established. Indeed, statistical analysis of different grain age populations requires dating of multiple grains (e.g., to be 95 % certain that a population representing 5 % of the grains is not missed, 117 single grain ages need to be dated; Vermeesch, 2004). In any case, reproducing ages determined in different samples indicates that the data are geologically meaningful; i.e., the observed spread is the result of partial resetting and/or different kinetics and not the result of factors independent of the time–temperature history, such as undetected inclusions or external helium implantation. We thus interpret the system as only partially reset, implying these units were not heated above the reset temperature (approximately 130–170 ∘C) after deposition. This interpretation is corroborated by unreset ZHe ages in the Hawasina window (Fig. 1; László Csontos, personal communication, 2014). The top of the Natih Formation experienced temperatures above 220 ∘C. We suggest that this apparent contradiction may be explained by juxtaposition of the colder Muti and Hawasina units against the top of the carbonate platform during extensional top-to-NNE shearing. This implies that at least 50 ∘C of the cooling is associated with post-obduction extension, i.e., before doming. A two-stage exhumation history of the Jebel Akhdar Dome has also been inferred from structural data (Grobe et al., 2018; Mattern and Scharf, 2018) and the stratigraphic record (Fournier et al., 2006; Mann et al., 1990). Top-to-NNE shearing is associated with tectonic thinning of the ophiolite (Grobe et al., 2018). This tectonic denudation will also result in cooling and may explain why so little ophiolite is found in the post-obduction sediments. Additionally, ophiolitic material may have been lost to the Gulf of Oman.
5.3 Pressure evolution
Evolution of pore pressures was modeled (Figs. S7 and S8) assuming a seal on top of the Natih Fm. ( m2). Porosity was lost during Muti deposition in the moving forebulge (top seal) and related burial and the emplacement of the Hawasina nappes and the ophiolite, which induced compaction and a remaining very low porosity of ca. 1 %. Hydrostatic pressure increased with burial under the moving forebulge at 88 Ma to 40 MPa, after Muti deposition to 60 MPa and after ophiolite emplacement to 120 MPa. There is a calculated pore pressure rise above hydrostatic pressure in response to Hawasina nappe and ophiolite emplacement.
The formation of tensile fractures, as inferred from bedding-confined mode I veins in the Natih Fm. (Arndt et al., 2014; Grobe et al., 2018; Holland et al., 2009b; Virgo, 2015), requires internal fluid pressures (Pf) exceeding the sum of the stress acting normal on the fracture surface (σ3) and the tensile stress of the rock (T): and a differential stress (σ1−σ3) below 4T (Secor Jr., 1965). Host-rock-buffered vein isotope compositions indicate that the veins were formed by local fluids (Arndt et al., 2014) and hence require local overpressure cells.
Sensitivity analyses of reduced permeabilities of the Muti, Natih, and Nahr Umr formations show that the overpressure generation necessary for rock fracturing requires a very good top seal and also a reduced horizontal permeability of the Natih Fm. of 10−23 m2 (Figs. S7 and S8). A top seal on its own is not sufficient for overpressure to initiate rock failure. This case results in pore pressures up to 300 MPa within the top Natih and localized overpressures of 195 MPa in front of the obducting ophiolite.
All results indicate that without low horizontal permeabilities of the Natih Fm. m2 the overpressure cells required for vein formation cannot be generated. The reduced permeabilities in the Natih Fm. are necessary to prevent an early, tectonically driven horizontal pressure release.
5.4 Fluid migration
Numerical basin modeling shows that rapid burial of sedimentary rocks below the ophiolite (88–80 Ma) caused under-compaction, i.e., a porosity too high with respect to burial depth, and consequent pore pressure increase. Two example model results of fluid migration in front of the obducting ophiolite are shown in the Supplement Fig. S9. If low permeabilities are assigned to the non-source-rock members of the Natih Fm., migration will mainly take place within the source rocks and at layer interfaces within the Natih Fm. If the complete Natih Fm. has low permeabilities, fluids will leave the source rock vertically first before lateral migration localizes along layer boundaries. The pressure gradient between overpressures below the allochthonous nappes and the less deeply buried southern foreland initiates tectonically driven fluid migration in front of the obducting nappes, an idea that was first introduced by Oliver (1986). Solid bitumen accumulations in black-stained calcite veins are in agreement with this interpretation (Fink et al., 2015).
Dome formation of the Jebel Akhdar anticline around 55 Ma initiated layer tilting and consequent northward migration of the generated hydrocarbons as observed by secondary low-reflective solid bitumen generations in Natih veins and host rocks at the southern flank of the Oman mountains (Fink et al., 2015; Grobe et al., 2016).
This study provides insights into temperature evolution during obduction and prior to subsequent orogenesis.
Arabia's passive continental margin was buried to at least 4 km at times of foredeep migration and afterwards under 8–10 km of Semail Ophiolite and 2 km of sedimentary Hawasina nappes. Deepest burial under the ophiolite resulted in peak temperatures of up to 300 ∘C (Shu'aiba Fm.) with sub-lithostatic pore pressures. Ophiolite obduction and overpressure cells expelled fluids towards the foreland through matrix and fracture porosity.
ZHe data show cooling associated with forebulge migration, as well as with exhumation of the Jebel Akhdar Dome.
Exhumation of the Jebel Akhdar Dome took place in two stages. A first stage is associated with top-to-NNE shearing, which is responsible for at least 50 ∘C of the cooling, as witnessed by the juxtaposition of units including partially reset ZHe ages against units that experienced more than 220 ∘C. ZHe data show that the second exhumation phase, associated with doming of the Jebel Akhdar, occurred between 49 and 39 Ma.
All generated laboratory data are shown in this paper and the provided Supplement.
The supplement related to this article is available online at: https://doi.org/10.5194/se-10-149-2019-supplement.
JLU, RL, and AG initiated and planned the study. AG planned and carried out fieldwork as well as thermal maturity measurements (VR, solid bitumen reflectance, Raman spectroscopy), structural interpretations, and basin modeling. AG, CvH, JLU, ID, and FW carried out fieldwork and structural interpretations. FW and ID conducted the thermochronological measurements with the help of CvH. PM and AG performed fluid-inclusion thermometry.
AG and CvH prepared the paper with contributions from all coauthors.
The authors declare that they have no conflict of interest.
We acknowledge the highly appreciated help of Donka Macherey (sample
preparation, RWTH Aachen), the team of the KU Leuven (fluid-inclusion
measurements), and Keno Lünsdorf (Raman spectroscopy,
Georg-August University, Göttingen). Sample crushing was realized by the
team of SELFRAG, Switzerland. Wiekert Visser and Victoria Sachse are thanked
for fruitful discussions; Gösta Hoffmann and Wilfried Bauer of GUtech
are thanked for helping with field logistics. We are grateful for comments
from Edwin Gnos, Andreas Scharf, Wolf-Christian Dullo, and Mark Handy on
earlier versions of this paper and the reviews of Massimiliano Zattin,
Luca Aldega, Bruce Levell, and Federico Rossetti.
Edited by: Federico Rossetti
Reviewed by: Luca Aldega, Massimiliano Zattin, and Bruce Levell
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