The Oligo-Miocene deepwater system of the Levant Basin

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- 5 -intrusion and stretching of the crust took place, no indications for sea-floor spreading andemplacement of new oceanic crust are found (Gardosh and Druckman, 2006).The post-rift phase is associated with cooling and subsidence that was probably more intense withinthe basin than on the eastern margin. The Late Jurassic to Middle Cretaceous section records agradual formation of a passive-margin profile and the subsequent development of a deep-marinebasin bordered by a shallow-marine shelf (Bein and Gvirtzman, 1977; Garfunkel, 1998). Thepassive-margin stage is characterized by recurring cycles of marine transgression and regressionassociated with relative sea-level changes (Flexer et al., 1986; Gardosh, 2002). These are reflectedby marine onlaps, unconformity surfaces, stacking of carbonate platforms, on the basin's margin,and mass transported deposition in the basin.The convergence phase is related to the closure of the Neotethyan Ocean system and the northwardmotion of the Afro-Arabian plate towards Eurasia (Robertson, 1998). In the Levant region thismotion is manifested by large-scale contractional deformation of the Syrian Arc fold belt (Krenkel,1924; Picard, 1959). Syrian Arc type folds are found throughout the Levant region, in an areaextending from the Western Desert of Egypt, through Israel to Lebanon and Syria. Based on surfacestudies, Walley (2001) suggested two main folding phases: Late Cretaceous and Early Tertiary. Thesubsurface study of the Levant Basin confirmed this suggestion (Gardosh and Druckman, 2006;Gardosh et al., 2006; Bar et al., 2008; Gardosh et al., 2008). The Late Cretaceous Syrian Arc phaseI is characterized by inversion of the Early Mesozoic normal faults and the development ofasymmetric, high-amplitude folds found mostly near the eastern Levant margin and further inland.The Early Tertiary Syrian Arc phase II is characterized by the formation of low-amplitude foldsthroughout the basin, uplifting and tilting of marginal blocks at the eastern part of the basin andfurther inland. The contractional activity resulted with the formation of a wide elevated fold belt inthe eastern part of Levant basin, extending 50-70 km west of the present-day coastline (Gardosh andDruckman, 2006; Gardosh et al., 2006; Gardosh et al., 2008).Tertiary tectonic activity and sea-level falls caused intense erosion and accumulation of severalkilometers thick basin-fill (Gardosh et al., 2006; Gardosh et al., 2008). Fluvial systems flowed onthe exposed shelf from elevated areas in the east, while submarine turbidity currents incised theupper slope and transported siliciclastic sediments further into the basin (Druckman et al., 1995).The Oligo-Miocene and Pliocene drainage system includes several main submarine canyons andnumerous secondary conduits (Gardosh et al., 2006; Gardosh et al., 2008). Two of the canyons in
- 6 -the southeastern part of the basin, e.g. Afiq and Ashdod, are incised several hundred meters on thecontinental slope. Other canyons were less erosive and their flow pattern was for the most partdictated by pre-existing synclines. The Tertiary drainage system was shut-off temporarily during theMessinian salinity event and was turned-on again during post-evaporite, latest Miocene to EarlyPliocene lowstands. A subsequent Plio-Pleistocene transgression was followed by the accumulationof a thick, siliciclastics prograding wedge along the Levant continental slope.2. Data sets2.1 Well and outcrop dataThe well data used in this study is based on 44 wells located in the basin or on its eastern margin(Fig. 2). Stratigraphic subdivisions of these wells were, for the most part, taken from thelithostratigraphic database of oil and gas wells drilled in Israel (Table 1) compiled by Fleischer andVarshavsky (2002). Biostratigraphic data, from part of the wells, were reexamined and theirstratigraphy was updated in the framework of this project (Siman-Tov, 2008a,b). Velocity data andtime-converted wire-line logs were used for correlation of stratigraphic tops with the seismic data(Table 1). The lithostratigraphy and biostratigraphy of selected wells were thoroughly reviewed andwere used to construct four detailed stratigraphic cross-sections extending from the coastal area tothe eastern part of the basin (Fig. 2). Additional well and outcrop data from the Levant margin wereanalyzed and were integrated into a stratigraphic table and the marine onlap curve of the Tertiarysuccession (Fig. 3).Table 1: Summary of well data used in the present study. The depth of chronostratigraphic and lithostratigraphic tops inthe wells is in meters below MSL. These depth values were used for calibration the seismic data with depth maps.Abbreviations of lithostratigraphic units are: TY - Talme Yafe Formation, Mt Sc - Mount Scopus Group, Av - AvedatGroup, BG - Bet Guvrin Formation, AshCl - Ashdod Clastics, Mav - Mavqiim Formation.Chronostrat.Base Up. Base Early Mid. BaseBoundaryCretaceous Oligocene Miocene ? MessinianBase PlioceneSeismichorizonGreen Red Cyan Purple VioletWell names: Well Abbrv.Andromeda-1 AND1 2149/Ziqim 2127/MavAshdod-1 ASH1 2208/TY 2208 1785/BG 1710/Pattish 1690/MavAsher Yam-1 ASYM1 479/Yagur 479 479 479 479Ashqelon-2 ASHQ2 2234/TY 2040/Av 1303/BG 1120/Ziqim 1063/MavAshqelon-3 ASHQ3 2098/TY 1955/Av 1245/BG 1009/Ziqim 961/MavAtlit-1 Deep ATLT1 45/Negba 45 45 45 45Bat Yam-1 BYAM1 2432/TY 2197/Av 2087/BG 1479/AshCl 1479/NPVulcBravo-1 BRV1 2939Daliyya 2197/Av 1627/BG 1380/Ziqim 1350/Mav
Page 1 and 2: The Oligo-Miocene deepwater system
Page 4 and 5: ITable of contentPageAbstract …
Page 6: IIIFigure 16: Depth map of the base
Page 9 and 10: - 2 -Oligo-Miocene sands were depos
Page 11: - 4 -The discoveries of the early 2
Page 15 and 16: - 8 -Legend2D survey A2D survey B2D
Page 17 and 18: - 10 -2.2 Seismic dataThe seismic i
Page 19 and 20: - 12 -conditions, and possibly sedi
Page 21 and 22: - 14 -3.3.2 Lower Oligocene sedimen
Page 23 and 24: - 16 -Druckman, 2006; Bertoni and C
Page 25 and 26: - 18 -aSWNETWT (ms)bSWHanaha-1NEMav
Page 27 and 28: - 20 -aNWSETWT (ms)bYam West-1Ziqim
Page 29 and 30: - 22 -WETWT (ms)aYam Yafo-1multiple
Page 31 and 32: - 24 -NW SEaYam West-2Plio-Pleistoc
Page 33 and 34: - 26 -A third incision surface, mar
Page 35 and 36: - 28 -4.2.2 Deep, central part of t
Page 37 and 38: - 30 -10812591167Figure 13: Time st
Page 39 and 40: - 32 -10812591167Figure 15: Time st
Page 41 and 42: - 34 -HaifaQishon302829AtlitCaesare
Page 43 and 44: - 36 -Figure 19: Depth map on the t
Page 45 and 46: - 38 -SW NEAfiq Canyon Ashdod Canyo
Page 47 and 48: - 40 -The Beer Sheva-Afiq Canyon lo
Page 49 and 50: - 42 -SWNE SW NE SW NEPlio-Pleistoc
Page 51 and 52: - 44 -SWHanaha-1NE SW NE SW Hof Ash
Page 53 and 54: - 46 -BMSL1400m.1500200025003000Han
Page 55 and 56: - 48 -WE W E NW SEPlio-PleistoceneC
Page 57 and 58: - 50 -W EPlio-PleistoceneMessinian
Page 59 and 60: - 52 -S NPlio-PleistoceneM.-U. Mioc
Page 61 and 62: Figure 31: Stratigraphic section al
Page 63 and 64:
- 56 -W ELower-slope and basin floo
Page 65 and 66:
- 58 -SlopeSusita + En-GevsandsShel
Page 67 and 68:
- 60 -In the Hadera Canyon the seis
Page 69 and 70:
- 62 -Additional mechanisms for tra
Page 71 and 72:
- 64 -The existence of channel fill
Page 73 and 74:
- 66 -SlopePartly Uplifted ?Hordos
Page 75 and 76:
- 68 -Oligo-Miocene sands were depo
Page 77 and 78:
- 70 -Druckman, Y., Conway, B.H., E
Page 79 and 80:
- 72 -Neev, D., 1960, A pre-Neogene
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The Oligo-Miocene deepwater system of the Levant Basin

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