Multi-Phase Inversion Tectonics Related to the Hendijan-Nowrooz-Khafji

Journal of African Earth Sciences 111 (2015) 399e408

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Journal of African Earth Sciences

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Multi-phase inversion tectonics related to the HendijaneNowroozeKhafji Fault activity, Zagros Mountains, SW Iran

* Sadjad Kazem Shiroodi a, Mohammad Ghafoori a, Ali Faghih b, , Mostafa Ghanadian b, Gholamreza Lashkaripour a, Naser Hafezi Moghadas a a Department of Geology, Faculty of Sciences, Ferdowsi University of Mashhad, Mashhad, Iran b Departments of Earth Sciences, College of Sciences, Shiraz University, Shiraz, Iran article info abstract

Article history: Distinctive characteristics of inverted structures make them important criteria for the identiﬁcation of Received 13 March 2015 certain structural styles of folded belts. The interpretation of 3D seismic reﬂection and well data sheds Received in revised form new light on the structural evolution and age of inverted structures associated to the HendijaneNowrooz 19 August 2015 eKhafji Fault within the Persian Gulf Basin and northeastern margin of Afro-Arabian plate. Analysis of Accepted 22 August 2015 thickness variations of growth strata using “T-Z plot” (thickness versus throw plot) method revealed the Available online 28 August 2015 kinematics of the fault. Obtained results show that the fault has experienced a multi-phase evolutionary history over six different extension and compression deformation events (i.e. positive and negative Keywords: Inversion tectonics inversion) between 252.2 and 11.62 Ma. This cyclic activity of the growth fault was resulted from 3D seismic section alteration of sedimentary processes during continuous fault slip. The structural development of the study Zagros area both during positive and negative inversion geometry styles was ultimately controlled by the Persian Gulf relative motion between the Afro-Arabian and Central-Iranian plates. Iran © 2015 Elsevier Ltd. All rights reserved.

1. Introduction secondary porosity, c) modify the attitude of the sedimentary package, allowing different directions of fluid migration with time, Inversion tectonics was introduced by several authors (e.g. d)reactivate older faults, changing their sealing properties and e) Glennie and Boegner, 1981; Cooper and Williams, 1989) to describe form complex structures at depth and care needs to be taken to changes of tectonic regime from extension to compression, and vice differentiate these from single event compressive thin-skinned versa. After introducing different type of inverted structures (i.e. thrust structures (Coward, 1994). positive and negative types) by Williams et al. (1989), several ex- Constraining reactivation processes has practical implications amples of these structures were recognized and described world- for improving the evaluation of seismic hazards (Lisle and wide (e.g. Biji, 2006 and references cited therein). Positive and Srivastava, 2004) and assessing the impact of reactivation on fault negative inverted structures are created in response to change of seal quality and fluid migration (Holdsworth et al., 1997). The main tectonic regime following the contractional reactivation of inheri- gaol of this study is to describe and quantify the style of inversion ted normal faults or extensional reactivation of inherited reverse tectonics adjacent to the HendijaneNowroozeKhafji Fault from the faults, respectively (Fig. 1). Distinctive characteristics of inversion- Persian Gulf Basin and northeastern margin of the Afro-Arabian related structural geometries consist of anomalous variations of plate (Fig. 2). Due to the occurrence of large oil and gas resources fault-throw with depth, thicker strata on the hanging wall of of Iran and Saudi Arabia (Fig. 3) in the vicinity of this fault, it has thrusts faults and footwall shortcut thrusts (Cooper and Williams, tremendous geological and industrial importance. The Hendijan 1989). The recognition of inverted structures is important in the high and the BurganeAzadegan high with NEeSW and NeS trends oil industry because inversion can: a) modify the burial history of a are the most prominent structural features in the Persian Gulf Ba- sedimentary basin, b) uplift sediments above sea level generating sin. The Hendijan and BurganeAzadegan high are structural trends were named based on elongated topographical feature in north part of Persian Gulf (the geological map of National Iranian Oil Company in SW Iran at scale 1:10,00,000). The Hendijan high in SW * Corresponding author. fi E-mail address: [email protected] (A. Faghih). Iran hosts several Iranian and Saudi Arabian oil elds (Abdollahie http://dx.doi.org/10.1016/j.jafrearsci.2015.08.015 1464-343X/© 2015 Elsevier Ltd. All rights reserved. 400 S. Kazem Shiroodi et al. / Journal of African Earth Sciences 111 (2015) 399e408

Fig. 1. Two Schematic diagrams of a classical inversion structure, interaction between pre-tectonic, syn-tectonic and post-tectonic is important. (a) The early normal fault is reactivated as reverse (positive inversion structure). (b) The early reverse fault is reactivated as normal (negative inversion structure).

Fard et al., 2006). The Hendijan Fault is one of the Important Lin- the Arabian basement have been repeatedly reactivated during the eaments that have Arabian tectonic trend and refer of a syncline Permo-Triassic opening of the Neo-Tethys and have exerted a structure in Arabian plate (Bahroudi and Talbot, 2003). These strong control over the structure, thickness and facies of the cover structures extend to the N within the Zagros Mountains (Fig. 2). rocks (Zeigler, 2001). In the foreland part of the Zagros, north- Hence, we discuss the kinematic evolution of the Hendijan Fault esouth trends are attributed to the reactivation of Pan-African based on the quantitative interpretation of 3D seismic reflection basement faults (Edgell, 1991, 1996) during the Permo-Triassic and well data. In this paper, we present new tectono-sedimentary (Alsharhan and Nairn, 1997) till Late Cretaceous (Abdollahie Fard data based on the geological interpretation of seismic sections to et al., 2006 and references cited therein). The ductile deep seated support the occurrence of a multi-phase inversion tectonics related Precambrian Hormuz salt series, basement rocks movement and to the HendijaneNowroozeeKhafji Fault activity within the Zagros the late Tertiary Zagros orogeny, are main factors that have influ- Mountains, SW Iran. Based on the interpretation of growth strata enced the formation of the structural anomalies in the Persian Gulf and seismic stratigraphy, this paper describes the geometry styles (Saadatinejad et al., 2012). The study area is located in the Persian of inverted structures and reliably approximates the age of the Gulf Basin along the northeastern margin of the Afro-Arabian plate beginning of the positive and negative inversions in the Persian adjacent to the HendijaneNowroozeKhafji Fault. The names, li- Gulf Basin. thologies and ages of the stratigraphic formations and groups used here (Fig. 4) are based on the classical stratigraphic chart for this region established by James and Wynd (1965), correspond to those 2. Geological and tectonic settings employed by the National Iranian Oil Company in their regular exploration tasks synthesized in unpublished and confidential The Zagros Mountains is one of the most active collisional oro- annual reports. The ages of the various stratigraphic units were gens within the AlpineeHimalayan orogenic belt. Closure of the established by determining foraminifera biozones and employing Neotethys Ocean which resulted from oblique convergence be- fossils such as sponge spicules, algae, echinoids, rudists, radiolarids, tween the Afro-Arabian plate and Central Iranian plate during the ostracods, gastropods, foraminifers, bryozoans, corals, stromatop- Cenozoic led to formation of this belt (Mouthereau et al., 2012 and oroids, crinoids, tintinnids, Favreina, annelids and palynomorphs references cited therein). Both the Zagros Range and its foreland collected in confidential exploration wells. The Hendi- belong to the northeastern part of the Afro-Arabian Plate. The janeNowroozeKhafji Fault with few tens of kilometers is located in Persian Gulf Basin, a rich region of hydrocarbon resources, is a part the southeastern-east part of Zagros range in Iran and the west of of this lithospheric plate. This basin is surrounded by the Arabian Persian Gulf (Fig. 1). Shield in the west, Taurus range in the north and the Zagros range in the east and northeast. The regional geology of the Persian Gulf Basin has been described and analyzed in detail because of the high 3. Methods hydrocarbon potential of this region (e.g. Stern, 1985; Beydoun, 1991; Edgell, 1996; Alsharhan and Nairn, 1997; Bahroudi and In active tectonic settings, growing structures often control the Talbot, 2003). The Persian Gulf Basin was the site of ancient pas- deposition process at different scales (Verges et al., 2002). Growth sive margin sedimentation on the margin of Gondwana during fault activity led to change in the sediment thickness across the most of the Phanerozoic, which faced toward the Neotethys in the fault (i.e. synsedimentary fault). This event causes the differences in Mesozoic and toward the Paleotethys Ocean in the Paleozoic (Alavi, thickness of sediments both on the footwall and hanging wall 1994; Bahroudi and Talbot, 2003; Abdollahie Fard et al., 2006). during time of fault activity. Fault throws subsequent to the sedi- Main faults and folds in the northeast margin of Afro-Arabian plate mentation of each horizon and the fault movement history can be have different trends such as NeS, NNWeSSE or NNEeSSW determined using these thickness changes. Analysis of these (Abdollahie Fard et al., 2006). Northesouth-trending faults within thickness changes along a fault is now feasible using high quality S. Kazem Shiroodi et al. / Journal of African Earth Sciences 111 (2015) 399e408 401

Fig. 2. Map of basement lineaments and oil- and gas ﬁelds in the Zagros Basin (compiled from Beydoun, 1991; Alsharhan and Nairn, 1997; Weijermars, 1998).

3D seismic data (Childs et al., 2003). Displacement and the growth which is considered that sedimentation always fills-up fault- history of individual fault surfaces can be determined through this generated topography. In faulted settings, lithological variations analysis. The analysis of syn-tectonic sedimentation is widely used due to fault activity can be predicted on seismic profile using this to determine the kinematics of growth-faults. (e.g. Castelltort et al., method. (Castelltort et al., 2004a,b and references cited therein). 2004a,b). In order to highlight the activation interval of the Hen- Among the n stratigraphic horizons across a growth fault, the dijaneNowroozeKhafji Fault, we used the ‘T-Z plot’ method younger horizon at i ¼ 0 is considered as the first stratigraphic introduced by Pochat et al. (2004). Using this method one can surface without fault generated topography while the older i ¼ nis constrain the slip history of growth faults. The application of this the youngest pre-faulting horizon (Fig. 5). The obtained data from method is based on the “fill-to-the-top” sedimentation assumption analysis of thickness variations of growth strata may provide 402 S. Kazem Shiroodi et al. / Journal of African Earth Sciences 111 (2015) 399e408

Fig. 3. Prominent basement-rooted lineaments in the Arabian continental crust. As can be seen in Map, HendijaneNowroozeKhafji fault has Pan-African trend (Alavi, 2007). information about fault kinematics even in the absence of palaeo- and associated sedimentological patterns can affect quantitatively bathymetry and the age of each horizon. slope variations on a TeZ plot. Therefore, this type of analysis be- Generally, throw variations represent a combination of comes a powerful tool to unravel main lithological alterations on displacement and topography across the growth fault (Fig. 6). seismic sections in faulted domains. This research carried out based Therefore, the throw ti on the first increment of sedimentation on the mapping and interpretation of a net of high quality seismic (interval [i; i-1]) after time i (Fig. 6) is expressed as: sections acquired in two orthogonal sets: one set strikes NNEeSSW (referred to as NeS below) and the other strikes WNWeESE ¼ þ ti di ei (referred to as WeE below). The Schlumberger Petrel software was used for most of interpretation. Sixteen different horizons were in which the vertical displacement on the fault between i and i-1 is picked and interpreted in each seismic section. Sixteen different di, and the topography at time i is ei. It is assumed that fault horizons were picked and interpreted in each seismic section displacement variations can cause thickness variations in the (Fig. 8). sedimentary layer in two sides of fault. Alteration in this type of plot indicating positive, null and negative slopes reflects variations of thickening of the sedimentary strata towards the hanging wall 4. Results (Baudon and Cartwright, 2008 and references cited therein). Thickening of strata towards the hanging wall resulted from fault 4.1. Analysis of throw versus time activity, whereas during periods of fault quiescence (null slopes) associated with non-thickened intervals. Negative slopes the T-Z The long-term evolution of the fault displacement rate during plots may indicate fault linkage or fault inversion (Castelltort et al., time was analyzed in order to determine the major factor which 2004b and references cited therein). Assuming fill-to-the-top controls short-term thickness variations in growth strata (i.e. fault model (Fig. 7), the T-Z plot is useful to constrain the displacement movement or sedimentation dynamics). This research focuses on history of growth faults (Pochat et al., 2004). the study of variation of the vertical throw of each timeline during To construct a T-Z plot, the vertical throw Ti related to each time (Fig. 9). These particular stratigraphic surfaces can be horizon is plotted against the depth Zi in the hanging-wall considered as representing a nearly instantaneous event at the (Castelltort et al., 2004a). The first step for constructing this type scale of a sedimentary basin or such km-scale structures (Mitchum of plot consists of picking some markers on a seismic section that and Van Wagoner, 1991). These time lines are also not usually are correlatable around a fault. Then, the thickness of intervals related to erosive events which may preclude the mapping of the between successive markers and the associated vertical throw true displacement of fault (Childs et al., 1993). Therefore, the across the fault related to each horizon are measured and plotted. measured vertical throw related to time line associated the footwall Starting from the shallowest unfaulted interval, the throw related and the hanging wall is correlatable with the true fault to each horizon (Y-axis) and their depth (X-axis) down the fault are displacement. plotted against each other. In this case, evolution of fault growth Changing slope of the curve is interpreted as reflecting a change S. Kazem Shiroodi et al. / Journal of African Earth Sciences 111 (2015) 399e408 403

Fig. 4. Simplified stratigraphy of the area depicting the major lithological successions and main tectonic events in the Persian Gulf. The stratigraphic column is modified from Abdollahie Fard et al. (2006), Alavi (2007) and Soleimany et al. (2011), based on well data. Mechano-stratigraphy, detachments and influence on the hydrocarbon system are outlined.

Fig. 5. Principle of TeZ plot construction. (A) Example of correlated stratigraphic markers across a normal growth fault. (B) Corresponding TeZ plot (Castelltort et al., 2004a).

of fault mechanism during the time (Pochat and Van Den Driessche, negative slope shows thicker deposits in the footwall and a normal 2007 and references cited therein). Unthickened layers on both dip slip mechanism. sides of the fault are shown by zero-slope interval, thus the fault The analysis of our data reveals that the vertical throw of the has been inactive and a positive slope corresponds to a thinner fault encompasses a long-term, progressive diminution with time layer and reverses dip slip mechanism of the fault and ﬁnally, of the fault scarp from 607 m to 30 m, over 240 million years 404 S. Kazem Shiroodi et al. / Journal of African Earth Sciences 111 (2015) 399e408

4.2. Thickness versus throw analysis

The main feature can be seen on the TeZ plot is a long-term quasi linear decrease of the vertical throw from 358.1e479.72 m, over a sediment thickness of 2771 m on both sides of the HendijaneNowroozeKhafji Fault (Fig. 10). Based on the seismic interpretation, the width of the Hendi- janeNowroozeKhafji Fault is about 1 km including many sub-faults with normal and reverse dip-slip movements during the period of our data (more than 240 million years). These long-term relation- Fig. 6. General relationships between vertical throw (Ti), displacement (di), strati- ship of thickness versus time is characteristic of syndepositional graphic thicknesses (Shi and Sfi) and fault topography (eiandei- 1) during one step of fault growth (Castelltort et al., 2004a). faults. Based on the results, the fault activity can be divided into 6 phases (Fig. 10): a first phase from 11.62 to 15.97 Ma (4.35 Ma) with displacement rate of 2.60 m/Ma and in second phase from 15.97 to 20.44Ma (6.47Ma) with displacement rate of 5.88 m/Ma and in third longer phase from 20.44 to 145 Ma (122.56 Ma) with displacement rate of 2.73 m/Ma and in fourth phase from 145 to 152 Ma (7Ma) with displacement rate of 22.24 m/Ma and in fifth phase from 152 to 208.5Ma (56.5Ma) with displacement rate of 6.97 m/Ma and in Latest phase from 208.5 to 252.17 Ma (43.67Ma) with displacement rate of 8.12 m/Ma. As show in Table 1, maximum of activity rate of HendijaneNowroozeKhafji Fault during 11.62 to 252.17 Ma has been on normal mechanism from 145 to 152 and minimum fi e ‘‘ Fig. 7. Signi cance of T Z plot slope variation (Castelltort et al., 2004a,b). a) Fill-to- e e the-top’’ model: Each slope variation characterizes the ratio between fault displace- activity rate of Hendijan Nowrooz Khafji Fault has experienced a ment rate and sedimentation rate. A zero-slope interval is symptomatic of fault inac- reverse mechanism from 11.62 to 15.97. In addition, the longest tivity. A positive-slope interval is symptomatic of fault activity (Pochat et al., 2009). active phase along the HendijaneNowroozeKhafji Fault was in the 3rd phase lasting 124.56 Ma and shortest phase was the 1st lasting (Fig. 9). According to the Fig. 6, two major inclinations are distin- only 4.35 Ma. guished (Fig. 9) as follows: The slope of the T-Z curve shows the same trend in three time intervals; Tatarian to Norian, Kimmer- idgian to Portlandian and Aquitanian to Burdigalianin. Throws in 5. Discussion four steps are different from each other, Norian to Kimmeridgian, Portlandian to Aquitanian and Burdigalian to Serravallian that 5.1. Tectonic inversion adjacent to the HendijaneNowroozeKhafji represents the changing of tectonic conditions or the stress regime Fault which caused deposition of growth strata in the basin and reverse dip-slip movement. Based on the above mentioned results, the fault Reactivation of faults activity during different deformation movement can be divided into 6 phases (Fig. 9 and Table 1). phases has been reported for several tectonic regimes worldwide

Fig. 8. Cross section through HendijaneKhafji fault with growth structure in the Persian Gulf basin, based on wells and seismic data. The thickness of strata on fault zone or both sides of its changed during of fault activity. S. Kazem Shiroodi et al. / Journal of African Earth Sciences 111 (2015) 399e408 405

Fig. 9. Signiﬁcance of T-Z plot slope variation according Fill-to-the-top model of Castelltort et al. (2004a,b). Each slope variation characterizes the ratio between fault displacement rate and sedimentation rate, a zero-slope interval is symptomatic of fault inactivity, a positive-slope or negative once interval are symptomatic of fault activity (Pochat et al., 2009).

Table 1 Different phase of fault activity determined based on quantitative interpretation of seismic data along the HendijaneNowroozeKhafji Fault.

Phase Start of the phase (Ma) End of the phase (Ma) Duration time (Ma) Rate (M/Ma) Function Thickness (TWT)

1st 11.62 15.97 4.35 2.60 Reverse 216.78 2nd 15.97 20.44 4.47 5.88 Normal 57.08 3rd 20.44 145 124.56 2.73 Reverse 1148.22 4th 145 152 7 22.24 Normal 77.58 5th 152 208.5 56.5 6.97 Reverse 717.22 6th 208.5 252.17 43.67 8.12 Normal 707.56

(Cooper and Williams, 1989). The stresses acting along the plate HendijaneNowroozeKhafji Fault) on basin architecture and on margins can be transmitted far into the foreland resulting in the lateral changes of facies and formation thickness in the Izeh zone reactivation of pre-existing normal faults (Ziegler et al., 1995). and Dezful embayment. The HendijaneNowroozeKhafji Fault is Moreover, changes from early extension to later contraction in the collection of a number of vertical strike-slip faults with dip-slip foreland domains which previously affected by normal faulting components that were reactivated under regional tectonic condi- have promoted positive tectonic inversion (Butler et al., 2006 and tions during different time periods. Observing seismic cross line of references cited therein). Resulting changes from early contraction HendijaneNowroozeKhafji Fault in Persian Gulf reveals changes in to later extension have promoted negative tectonic inversion thickness of syn-tectonic deposition above fault zones and on both (Pasculli et al., 2008). sides of the fault zone. Observation of stratal on-lap and/or off-lap Sherkati and Letouzey (2004) presented evidence for the effects pattern in seismic reﬂector in some strata with different ages in the of reactivation of NeS basement faults (e.g. the study area reveal that this thickness change is not related to the

Fig. 10. Results of T-Z plot measurements along the 16 layers. Throw is reported on the Y-axis in milliseconds, thickness of each horizon (Z) is reported on the X-axis in milliseconds. Evolution of the vertical throw of timeline surfaces at during time. When the slop of graph change, means that altered in fault mechanism. 406 S. Kazem Shiroodi et al. / Journal of African Earth Sciences 111 (2015) 399e408 primary basin floor roughness. This represents a change in the dip- In the Norian stage, slopes of graphs in the TeZ plot change to slip component of fault zone due to a changing tectonic regime in positive and thickness of sediment above the fault zone is less than the study area as follows. its two sides which indicates a reverse component and uplift 1- When we carefully scrutinized sedimentary layers deposited movement along the fault. In this time, the Hercynian Ocean was to during the Scythian to Tatarian (Fig. 11a), Pliensbachian to Kim- the north of Iran and the northward subduction and closure of the meridgian (Fig. 11c) and Priabonian to Burdigalian (Fig. 11e); we this Ocean happened at about 220 Ma in the Triassic period found that the fault had a normal dip-slip component. The thick- (Berberian and King, 1981). We suggest that as a result of closing ness of sediment in the west side of the fault is greater than that of the Hercynian Ocean at this time suddenly the kinematics of the east side. On-lap features in the strata explain that the sedimentary HendijaneNowroozeKhafji Fault changed. Prior to the middle basin developed on the fault zone had subsidence both toward the Triassic orogenic event(210 Ma), late Paleozoic ophiolite complexes east and west resulting in a normal fault component of dip-slip were emplaced in the north, presumably at the time of the collision activity. of the continental fragments with Asia (Shafaii Moghadam et al., 2- From Norian to Pliensbachian (Fig. 11b) and Kimmeridgian to 2014; Shafaii Moghadam and Stern, 2015). In the Kimmeridgian Priabonian (Fig. 11d) and Burdigalian to Serravallian (Fig. 11f), the stage, the fault zone changed in its function, as a result, an exten- deposition level of the fault zone was significantly reduced sional tectonic regime caused pelagic sedimentation of upper Tri- compared to the east and west sides due to reverse dip-slip assiceJurassic period along the active central Iranian and the movement along the fault. Therefore, the fault zone was seated passive Zagros continental margins, providing the first sedimentary higher than its sides. This has resulted in a lower rate of sedi- evidence for the appearance of a true oceanic environment (Shafaii mentation in the fault zone or the sediments have been exposed to Moghadam et al., 2015). Therefore, we notice an increase in the erosion as a result of fault uplifting. This is visible on high- thickness of the sediments in the fault zone at this time which resolution seismic images and it can be seen in the large scale of reflects tension function and normal dip-slip component of the growth strata on both sides of the fault zone. Due to the normal fault zone at this time. motion during Scythian to Tatarian and reverse motion during A compressional event occurred in Late Jurassic-Early Creta- Norian to Kimmeridgian, negative inversion structures formed on ceous (140 Ma). At the middle of the period when the High-Zagros the fault zone during these times. During orogenic evolution of Alpine Ocean supposed to have been closing (Alavi, 2007) as shown collided passive continental margins of the Afro-Arabian continent, in T-Z plot from Portlandian to Albian curve, the slope is almost basement faults are reactivated. The Zagros Mountains resulted uniform and the fault zone had a reverse dip-slip component from the ongoing collision of the Afro-Arabian plate with the consistent with a contractional tectonic regime in the region during Central Iranian continental blocks (e.g. Stocklin, 1968; Jackson and that time. In the Turonian, the thickness of sediments was sharply Mckenzie, 1984). reduced along the fault zone(Fig. 8). During the latest Turonian (~90 In order to determine the geometric and kinematic evolution of Ma) stacked thrust sheets, composed of oceanic crust and upper the Zagros basin and the trapping of hydrocarbons, it is necessary to mantle rocks (ophiolites), were obducted onto the northeastern distinguish its pre and post-collisional structures. The Arabian Afro-Arabian passive continental margin (Alavi, 2004, 2007). Thus, Shield displays two sets of Pan-African tectonic fabrics (Stern, 1985; the result of an extremely functional reverse dip-slip of the fault Kusky and Matsah, 2003; Jackson et al., 2013) formed between 900 zone was result of Alpine Ocean (Neo-Tethys) ophiolite obduction Ma and 600 Ma ago (Stacey et al., 1984): one set dips steeply with a during Turonian. The latest Turonian regional unconformity, which NeS trend and the other has a NWeSE trend and shows left-lateral marks a drastic change from a continental shelf tectono- strike-slip displacement (Stern, 1985). The Phanerozoic cover of the sedimentary setting to a relatively narrow and elongated profore- Arabian Platform is affected by broad anticlines and narrower land basin, records the initiation of this “obduction” event (Alavi, synclines (Beydoun, 1991) mostly trending NeS. A number of terms 2004). So function of the erosion phase and ophiolite obduction have been used for such structures (Bahroudi and Talbot, 2003), cause a sudden change in the slope of T-Z plot in Turonian. including lineaments and blind basement faults (Berberian, 1995). The Middle Alpine orogenic events ended at about 20 Ma These structures are attributed to the reactivation of one of the two (Berberian and King, 1981; Alavi, 2004, 2007). Thus the fault zone sets of Pan-African basement structures (Edgell, 1991). Most have acted with a reverse dip-slip component from Turonian to Pria- been active since the Late Paleozoic (Alsharhan and Nairn, 1997; bonian (Fig. 8). After the collision, a relative calm prevailed in the http://www.hindawi.com/68351920/Abdeen et al., 2008; Tairou region as reflected by normal dip-slip displacements representing a et al., 2012). Old NeS basement faults have been repeatedly reac- period of tectonic relaxation after beginning of collision from the tivated since the Permo-Triassic opening of Neo-Tethys which has Aquitanian to Burdigalian. As a result with opening of the Red Sea exerted a strong control over the thickness and facies of Mesozoic and pushing the Arabian plate toward Asia, compressional regime sediment (Zeigler, 2001; Bahroudi and Talbot, 2003). The reac- again dominated in the region and the fault zone has reverse dip- tivation of NeS basement fault (e.g.HendijaneNowroozeKhafji slip in Serravallian(Fig. 8). Fault) affected basin architecture and created lateral changes in the facies and thickness of formations in the Izeh zone and Dezful 6. Conclusion Embayment as observed on seismic sections (Tavakoli Shirazi, 2012; Sherkati and Letouzey., 2004; Abdollahie Fard et al., 2006; Kinematic Analysis of the HendijaneNowrooz_Khafji Fault Soleimany and Sabat., 2010). According to Fig. 2, the T-Z plot in based on T-Z plot method provided a long-term evolution charac- Tatarian to Norian has a positive slope that represents normal dip- terized by altered rate of the fault continuous slip during 240.55 slip along the fault at this time. This behavior of the fault is millions of years. Based on the detailed interpretation of a high consistent with the regional tectonic regimes. The opening of the quality 3D seismic reflection sections, the throw versus times NWeSE trending Neo-Tethys Ocean in the Permo-Trias separated measurements reveal six phases of the fault activity with different the Arabian plate to the southwest from the Iranian plate to the rate of throw in each phase. Two distinct mode of reactivation (i.e. northeast and the sedimentary cover rocks which were later to positive and negative inversion) are recognized which give insights become part of the Zagros deformation belt (Berberian and King, into the mechanism and kinematics of the fault reactivation. The 1981; Sengor, 1990). Thus, when the Neo-Tethys Ocean has being structural style of the study area during inversion realm was ulti- opened, the fault acted with a normal dip-slip component. mately controlled by the motion of the Afro-Arabian plate relative S. Kazem Shiroodi et al. / Journal of African Earth Sciences 111 (2015) 399e408 407

Fig. 11. High-resolution record of tectonic and sedimentary processes in growth strata based of HendijaneKhafji fault activity. In (a), (c) and (e) we can see increase of strata thickness in fault zone related to one or both sites its and on lap toward those, in these stages fault had normal dip-slip component and in (b), (d) and (f) we see decrease of strata thickness in fault zone related to one or both sites its and on lap toward fault zone That because of reverse dip-slip component in these stages. 408 S. Kazem Shiroodi et al. / Journal of African Earth Sciences 111 (2015) 399e408 to the Iranian plate. James, G.A., Wynd, J.G., 1965. Stratigraphic nomenclature of Iranian oil consortium agreement area. AAPG Bull. 49, 2162e2245. Kusky, T.M., Matsah, M.I., 2003. Neoproterozoic Dextral Faulting on the Najd Fault Acknowledgments System, Saudi Arabia, Preceded Sinistral Faulting and Escape Tectonics Relative to Closure of the Mozambique Ocean. Geological Society of London, Special e The authors would like to thank the editor Professor Eriksson for Publication, pp. 327 361, 206. Lisle, R.J., Srivastava, D.C., 2004. Test of the frictional reactivation theory for faults his editorial authority. We gratefully acknowledge constructive and validity of fault-slip analysis. Geology 32 (7), 569e572. reviews by an anonymous reviewer, which helped to considerably Mitchum, R.M., Van Wagoner, J.C., 1991. High-frequency sequences and their improve the scientific content and presentation of the manuscript. stacking patterns sequence stratigraphic evidence of high-frequency eustatic cycles. Sediment. Geol. 70 (2e4), 131e160. Important comments by Professor Timothy Kusky improved the Mouthereau, F., Lacombe, O., Verges, J., 2012. Building the Zagros collisional orogen: presentation of the paper. 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