Supergene non-sulfide deposits comprise rocks with elevated concentrations of Zn, Cu, Pb and, to a lesser extent, Ag and V. These are formed by the oxidation and mobilization of metals from sulfide mineralization, mobilized in solution and precipitated laterally or above the primary sulfide deposit. In most cases, there is no associated gossan or residual iron cap. Traditionally, Zn-rich non-sulfide deposits were termed “calamine”, a common name for an association of smithsonite and hemimorphite, with local cerussite and anglesite. In some cases, calamine deposits are genetically associated with nearby hydrothermal sulfide mineralization, even though their mineralogy and textures are similar to supergene calamine-style deposits. A relatively recently identified class of non-sulfide Zn deposits are those hosted in siliciclastic rocks, e.g. Yanque in Peru and Skorpion in Namibia. Other metals can also be dominant, e.g. Pb (Magellan/Paroo Station Mine, Australia); Cu (Carlotta, Arizona; Kunene, Namibia); Ag (Sierra Mojada, Mexico; Wonawinta, Australia) or V (Otavi Mountainland, Namibia). Carbon, oxygen, Zn, Pb and Cu stable isotope studies allow distinction between supergene and hypogene non-sulfide deposits. Periods of paleoclimatic switchovers from seasonally humid/arid to hyperarid climates have been considered the most favourable conditions for the formation and preservation of supergene non-sulfide deposits, even though many of these deposits are currently located in warm humid-weathering climatic zones.