Ophiolites components occur in Pan-African belt in Central Eastern Desert (CED) and South Eastern Desert (SED. The ultramafic components are severely serpentinized and in some areas occur as small fresh bodies in Serpentintes. These ultramafic bodies are characterized by the harzburgite-dunite –chromite association. The ophiolite components occur as thrust sheets along suture zone or as blocks in volcano- sedimenatry mélange or as nappe as Gebel Sol-Hamed and Gebel Gerf as largest Neoproterozoic (~750 Ma) mantle rocks in SED of Arabian Nubian Shield. The occurrences of the Neoproterozoic chromitites in Central Eastern Desert (CED), Egypt (Fig. 1) include Gabal El-Rubshi, Wadi Sodmein (Qift-Quseir road), Wadi Sephene, Wadi Beziah, Baramiya, Wadi Huitate (Idfu- Marsa Alam road), Wadi Lawi and Wadi El Zarka (South Marsa Alam). The occurrences in SED include Gebel Abu Dahar, Gebel Arais, Gebel Belmhandeit, G. Meqium, Gebel Abu Siayil, Gebel Um Thager, Gebel Gerf and Gebel Sol Hamed Chromitite deposits occur mainly as lenticular bodies of variable dimensions in ultramafic component (serpentinites) in Pan-African belt in CED and SED, Egypt. The pods appear to be concordant to sub- concordant with the host rocks as in Wadi Sephane and Gebel Gerf (Fig. 2a, b, c, d). The pods are commonly hosted by serpentinites probably derived from dunite. There are also micro-lenses, linear and planar segregations and disseminated chromite grains in meta-peridotite as shown in Wadi El Sodmin (Fig. 2e). They contact with meta-peridotite layers, where the abundance of chromite decreases upwards. Also Away from the main body of the chromitite lens, chromitite thin layers (in the order of a few centimeters thick) also occur. Podiform chromitite usually has gradational contacts with the adjacent meta- peridotite grading up to the disseminated-type chromite (Fig. 2f). The podiform chromitite deposits exhibit a wide range of compositions from high Cr to high Al varieties. The Cr of chrome spinel ranges from 0.67 to 0.88 in olivine- dunite, quite similar to that of the high-Cr chromitite, whereas it is around 0.62 in lherzolite- harzburgite (Saleh, 2006). Textural and mineralogical evidence indicates that podiform chromities were formed by crystallization of mafic magmas in the upper mantle (Lago et al., 1982). Reaction between the magmas and wall rocks is believed to have played an important role in the production of these deposits by modifying the melt composition and moving it into the field of chromite crystallization (Zhou et al., 1994, 1996). Chromite compositions are believed to be related to the degree of partial melting of host peridotites, with chrome numbers increasing as the degree of melting Mohamed Metwaly ABU ANBAR, 2016. The Chromitites Associated with the Pan-African Ophiolites in Egypt. Acta Geologica Sinica (English Edition), 90(supp. 1): 206-208. The Chromitites Associated with the Pan-African Ophiolites in Egypt Mohamed Metwaly ABU ANBAR Geology Department, Faculty of Science, Tanta University, Tanta, Egypt Vol. 90 Supp. 1 * Corresponding author. E-mail: mmanbar@yahoo.com 206 ACTA GEOLOGICA SINICA (English Edition) http://www.geojournals.cn/dzxben/ch/index.aspx http://mc.manuscriptcentral.com/ags July 2016 Fig. 1 Locations of Chromitites in SED and CED