Greece Field Trip

Greece Field Trip

Deep water Turbidities & Associated Facies As Modeling for Hydrocarbon Accumulations

Sixth & Seventh Day Zakynthos Island The lower Oligocene–lower Miocene Ionian foreland deep water flysch basin of the Ionian Islands was segmented by the late Oligo Oligocene by the westward-propagating thrust and fold system. In Zakynthos, upper Miocene flysch in the west passes eastward into shelf sediments. During Messinian crisis we have the sedimentation of Messinian evaporites, (in the western part only one cycle was recognized, whereas eastwards 14 cycles were recognized with mud and gypsum).

Movement on the Ionian thrust during early Pliocene, in the eastern part of Zakynthos Island, subdivided the pre-existing Miocene basin into two independent basins: the Alikanas foreland basin in the central Zakynthos and the Geraki piggy-back basin in the south-eastern Zakynthos.

In Alikanas foreland basin the re-sedimentation of Messinian deposits produced gypsiferous and fine-grained turbidites (one cycle westwards, more than seven eastwards). Migration of tectonic activity westwards changed the tectonic regime of this region and from a foreland basin we have a piggy-back basin during late Pleistocene.

In Geraki piggy-back basin we have three sub-basins close to the Ionian thrust that filled up during early Pliocene, first stage of Ionian thrust activity. The rest basin eatwards, far from the Ionian thrust, influenced from one normal fault and is still active. In this area during Pleistocene we have two coarsening upward shallow marine cycles. Diapirs influenced sedimentary basin during the sedimentation of the lower cycle.

To Register

Geo. Mahmoud Shakshak G&G Consulting Manager Oil & Gas Skills

Tel : +202 27549240 Fax : +202 27549744 Mobile : +201065520643 mshakshak@ ogs.com.eg

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FIELD SEMINAR

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urbidities and associated sequences play a very important part in hydrocarbon accumulation in different areas in oil fields in Egypt such as in Nile Delta, Gulf of Suez and Mediterranean ‌. and There is no similar outcrops in any location in Egypt. However it is well exposed in Greece where it is consider excellent surface analog to the subsurface facies.

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hrhrhree days in Pindos foreland studying Eocene to Miocene thick Turbidites, two day in an extensional sub-basin where thick Pleistocene fan-delta deposits were formed, and two days in Zakynthos island studying the evolution from Miocene to present, as part of the Pindos foreland, during Miocene, and as a complex basin (foreland and piggy-back basin) during Pliocene.

From 4 to 12 October 2012 F e e s -------------------------------- $ 4 0 0 0

Dr. Abraham Zelilidis, PhD University Of Patras - Greece

Dr. A. ZELILIDIS has obtained his degree in Geology from the University of Patras, Greece in 1984 and Ph.D. in Sedimentology in 1989. His expertise is in sedimentary Basin Analysis and Petroleum Geology. He has carried out several projects on hydrocarbon evaluation using subsurface and surface data. Dr. Zelilidis published several papers on tectonics and sedimentation of various geological provinces in Greece.

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Greece Field Trip

Fourth & Fifth Day Who Should Attend ?

Geologists, Sedimentologists, Stratigraphers ,Petrophysicists ,Geophysicists and Reservopir Engineers.

First, Second & Third Day Pindos Foreland Basin The fill of the Pindos Foreland Basin consists of thick Turbidite sequences which were deposited during the westward migration of the external Hellinides. In plan view, the Pindos Basin is elongated NW–SE parallel to the Pindos thrust, and the stratigraphy is locally deformed by a series of thrust–related folds. Basin deposition was dominated by carbonate sedimentation during the Late Mesozoic and Paleocene–Eocene.

Depositional conditions then changed, with submarine turbidites flows being derived from the newly–formed Pindos Mountains to the east. The Pindos foredeep was filled by submarine fan deposits and the source material of the submarine fans was the pindos Mountains. Palaeocurrent data for the submarine fan development of the Pindos foreland. Near to the Pindos thrust, the turbidite deposits are coarse–grained and represent the proximal parts of submarine fans; further westwards, the turbidites are finer grained and represent the more distal parts of the fans.

During the first day, stops will focus in the northern part of the Pindos Foreland Basin and will study geological outcrops of internal (from Metsovo to Ioannina) Ionian zone. During the second day will drive south and will study geological outcrops of internal Ionian zone (proximal part).

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Fan-deltas in Egion region and Pindos foreland deposits The Egio sub–basin, developed at the southern margins of the Corinth graben, are protected WNW–trending rift basins, which are confined basinwards by an intrabasinal basement high with horst morphology. Transport of sediment was perpendicular to sub–basin elongation and from the southern margin or from the intrabasinal basement highs, and formed Trapezoidal-type fan–delta deposits. These fan–delta deposits are coarse grained, and sediment fluxes were dominated by mass flows. All outcrops consist of foreset deposits that formed on the hanging wall of steep, fault–controlled nearshore slopes. In some places, alluvial fans, topsets and marine terrace deposits are present.

Mavri Miti formation (Pindos foreland deposits in the northern part of Peloponnesus) The lower members are thin-bedded turbidites of Late Eocene. The overlying beds include chaotic deposits with olistholiths of reddish Eocene limestone, sandstone olistho stromes, slumps and flame structures. Above these members the sandstone beds show a thickening and coarsening upwards trend and locally exhibit a ball-andpillow structure into a lenticular sand body.

Moreover non-graded sandstones are bounded by even and parallel surfaces, including small scale ripple marks showing a weak current flow. In the upper members of the Mavri Miti formation the deep water flysch sedimentation is characterized by progressive coarsening-upward sequences. They are composed of Facies C2 and D1 . Conglomeratic sandstones (Facies C) predominate at the top of this unit. The upper members of the Mavri Miti formation are of Early Oligocene age.

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