The supergene Skorpion non-sulphide zinc deposit is located approximately 40 km north of the Orange River in the southernmost Namib Desert, Namibia. It comprises a non-sulphide ore body (24.6 Mt @ 10.6 % Zn) and subordinate amounts of primary hypogene base metal sulphide mineralisation, which underlies the non-sulphide ores at depth. The supergene non-sulphide ores have formed by oxidation of a base metal sulphide protore by wall rock replacement and in-situ oxidation. The non-sulphide ore minerals comprise predominantly sauconite (Zn-smectite), substantial amounts of hemimorphite and smithsonite, and subordinate amounts of hydrozincite, tarbuttite and chalcophanite. The supergene ore minerals form mainly euhedral and subhedral crystals and occur as open space fillings in inter- and intragranular voids and fractures. The supergene non-sulphide ore body is hosted mainly by Late Proterozoic meta-arkoses and -subarkoses, and subordinately by felsic metavolcanic rocks and their volcaniclastic equivalents. The non-sulphide ore body is irregularly shaped, transgressive to sedimentary layering and major tectonic features. It is laterally zoned displaying a pronounced supergene lateral metal zonation pattern, which has developed as a result of differences in solubilities of the metals iron, copper, and zinc. The immobile metals iron and copper form supergene zones that represent the leached gossaneous part of the sulphide protore. The more mobile zinc has been leached from the sulphide protore. It has been transported in meteoric fluids and has precipitated in a distance from the sulpide protore and thus in the distance from supergene copper and iron zones forming a markedly supergene zinc enrichment zone. Even if the supergene non-sulphide ore body and the associated lateral metal zonation pattern are transgressive to a major Mesozoic fault system, they are partly controlled by it. The fault system opened abundant dilatational joints and fractures, which increased the permeability of the Neoproterozoic host rocks. Thus, meteoric fluids were channeled and were able to percolate along the fault system and to oxidise the hypogene sulphide ores to several hundreds of meters depth. Palaeo-morphological features and palaeo-climatic conditions indicate that the oxidation of the hypogene sulphide ore body and thus the formation of the supergene non-sulphide ore body must have taken place from Late Cretaceous up to Early Tertiary. Subsequently, the uppermost part of the Skorpion ore body has been eroded and alluvial sediments have been deposited on top of the erosional palaeo-surface in Late Tertiary.