الفهرس 
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Abstract
During the Upper Cretaceous interval, a great transgression progressed covering Egypt from the north until latitude 23° N in south reaching its highest amplitude during the Late Cenomanian time (Issawi and Osman, 2000). The tectonism that affected the North African Plate and sea-level changes had a great influence on the depositional history of the Upper Cretaceous successions in Egypt, forming different topographical and structural basins. As a result, the Upper Cretaceous sequence shows a rapid facies change (Issawi et al., 1999). The Cenomanian succession is outcropped in Egypt in three main districts; the Northern and Southern Sinai, Eastern Desert (between Gebel Shabraweet and Wadi Qena) and Western Desert (Bahariya Oasis and doubtfully at Abu Roash area). These areas proved to be active areas of subsidence (Fawzi, 1963). They represent one of the major transgressive cycles during the Cretaceous Period in Egypt, that resulting in forming of very shallow seas to the lows between the elevated massif (Said, 1990). The transgression of the Cenomanian Sea has progressed generally from the north to the south of Egypt. Generally, the thickness of the exposed marine Cenomanian diminishes gradually towards the south with more clastic facies (maximum thickness is 550 m in the north of Egypt and minimum thickness is 20 m in the south). The Cenomanian rocks form a formal rock unit (Galala Formation) in the northern part of the Eastern Desert (Awad and Abdallah, 1966). The depositional basin of the Galala Formation in the northern part of the north Eastern Desert was deeper than its southern part and free from any argillaceous influx (Metwally and Abdel Azeam, 1997