Banded iron formations (BIFs) have attracted several geologists for their economic potentiality and are regarded as the foremost profitable sources of iron. Entirely nine BIF occurrences in the central Eastern Desert of Egypt (CED) are recorded that represent the northwestern part of the Arabian–Nubian Shield and comprise Neoproterozoic basement rocks. Other localities that were previously described as BIF but missing the necessities to fit the proper BIF ore type (e.g., Abu Rakib, El Hundusi, Um Lassaf, Fatira, Um Ghamis El Hamra, Sitra, and Abu Diwan localities) are included under the volcanogenic jasper and chert deposits and attributed to low–T hydrothermal deposits related to the underlying volcanic rocks. The BIFs are encountered as defined stratigraphic units intimately related to the Pan-African island-arc volcano–sedimentary association. They are typically confined to the andesitic fine-grained volcaniclastics where it is nearly absent within the more acidic varieties. There are several lines of evidences indicating that the volcanic rocks are associated with subduction-type magmatism and additionally tholeiitic and calc–alkaline volcanics are co-genetic. Consequently, the time span between volcanic activity and subsequent BIF basin development is believed to be short. Very poor clastic input declares that chemical precipitation of the BIFs took place in periods of tectonic quiescence and volcanic indolence. REEs are utilized to provide necessary clues regarding the genesis of these BIFs whether they are of hydrothermal origin or precipitated from seawater. Based on field relations, petrography, and additionally REE features, the depositional age of these BIFs seems to be Neoproterozoic. BIFs are suffering from regional metamorphism together with the hosting country rocks. The grade of regional metamorphism was basically greenschist facies. Some BIF occurrences suffered additional thermal metamorphism and could reach the upper amphibolite-facies. Oxide, carbonate, silicate, and sulfide BIF facies in the Egyptian BIFs are recorded. Distribution of these facies, their chemical properties, and deposition mechanisms are mentioned. These facies are also as a result of the sea-level fluctuations and physicochemical variations. Field, microscopic, and geochemical data indicated, definitely, the sedimentary origin of these BIFs. A definitive interpretation of genesis of BIFs has long been sought. The explanation presented in the present chapter involves the interpretation of an island-arc as the depositional setting of the BIFs. A model to hide the deposition of BIFs in this setting is proposed. BIFs are thought to have crystallized from in situ low-temperature fluids presumably from direct seafloor precipitation with restricted hydrothermal input. BIF ingredients seems a normal Al-poor, Fe-rich pelagic mud (probably smectite) and soluble Fe and Si ions produced from alteration of the nearly andesitic and basaltic hinterland. This contribution declares that bedded cherts are deposited in a continuously acid to weakly alkaline environment, where BIFs were precipitated under alternation of acid and alkaline conditions. Precious metals concentrations of the BIFs were evaluated. Type of gold is considered as stratabound deposits related to Algoma-type BIF. The respective BIF occurrences are broadly equated to those of Algoma-type BIFs on account of the volcaniclastic association and also the island-arc setting. Primitive microorganisms like bacteria and alga are detected in the Egyptian Neoproterozoic BIFs. The role of microorganisms in precipitation of the BIFs is mentioned. Replacement and reaction textures between the organic remains and Fe-minerals and silica are represented. The preserved fossils include different types with spheroidal, filamentous, and spore-like forms. They lived at the time of transition from an anoxygenic to an oxygenic atmosphere through the activity of photosynthesizing microorganisms.