Epithermal ore deposits form at shallow depth. This conclusion was initially based on geologic reconstructions, ore mineralogy and related textures (Lindgren, 1933). It has subsequently been refined withfluid inclusion data to indicate that epithermal ores form over the temperature range of <150o C to ~300o C, from the surface to as deep as 1 to 2 km. Here we highlight the general characteristics of the two principal styles of epithermal mineralization in which gold is the dominant economic metal. We base our generalizations on observations of many deposits and prospects in the circum-Pacific region. Distinguishing between the two styles is crucial for effective exploration. Although they show similar alteration mineralogies, the distribution of the alteration zones is different, and the economic mineralization is associated with different parts of the system. The alteration zoning can be used as a pointer towards the most prospective part of the system, but only when the style has been correctly recognized. In addition, the two styles of mineralization have differences in their geochemical associations. <...>

Numerous detailed studies of stratiform  copper deposits reported in recent years have rejected the classic igneous-hydrothermal epithermal/telethermal origin for such mineralization, and have instead suggested that an origin intimately related to the processes of sedimentation would be much more suited to the observed character of these deposits. Overwhelming features, such as the widespread continuity of mineralization within a sedimentary basin and the distribution of mineralization within narrow stratigraphic limits, are commonly cited as evidence of sedimentary origins. However, such features do not exclude the possibility of diagenetic additions of ore metals to particularly favorable stratigraphic horizons, and in fact recent studies indicate repeatedly that one or more diagenetic events preceded the deposition of ore metals. For example, the deposition of iron sulfides, and in some cases sulfate-bearing minerals, is commonly observed to have occurred before the introduction of ore-stage metals. <...>

Increasingly explorationists are seeking to find new ore deposits in poorly prospected areas, be they geographically remote, such as in the Arctic, or geologically remote, such as those under sedimentary cover. Modern prospecting techniques, including low-detection-level geochemistry and the use of advanced geophysical instrumentation have greatly assisted explorers but fundamental to any soundly based exploration program remains an understanding of the geological framework of ore deposits. This allows the development of deposit models on macroscopic and mesoscopic scales.

At its 6th Biennial SGA Meeting in Krakow, Poland, August 2001, the Council of the Society for Geology Applied to Mineral Deposits (SGA) decided to offer the organization of the 7th Biennial Meeting to Athens, Greece. “Mineral Exploration and Sustainable Development” was chosen as the general theme of the meeting, in the expectation that would attract economic geologists from academia, government, and industry to discuss current issues regarding exploration for mineral deposits and their sustainable development by the minerals industry.

Geological Structure and History of Exploration of the Anikhov Graben (Southern Urals, Russia) 

Alexandra V. Panteleeva, Aleksandr V. Snachev, P. V. Pankratev,
R. S. Kisil, and V. P. Petrishchev
Geological Structure of the Kumak Ore Field (Southern Urals, Russia)     
Alexandra V. Panteleeva, Aleksandr V. Snachev, P. V. Pankratev,
V. S. Panteleev, and R. S. Kisil
Petrographic Features and Carbonaceous Matter of the Black Shales of the Kumak Deposit (Southern Urals, Russia)  
Alexandra V. Panteleeva, Aleksandr V. Snachev, А. М. Tyurin,
Mikhail A. Rassomakhin, and Irina V. Smoleva

The discovery of uranium is attributed to Klaproth, a German chemist who, in 1789, precipitated a yellow compound by dissolving pitchblende in nitric acid, neutralizing it with sodium hydroxide, and heating it with charcoal to obtain a black powder that was uranium oxide. He named the newly discovered element after the planet Uranus. In 1841, Pe´ligot, a French chemist working at the Baccarat crystal factory in Lorraine, isolated the first sample of uranium metal by heating uranium tetrachloride with potassium. Uranium was used during the nineteenth century to color pottery and glass until the discovery of radioactivity by Becquerel in 1896 (Becquerel, 1896), when he accidentally exposed a photographic plate to uranium. A team led by Enrico Fermi in 1934 observed that bombarding uranium with neutrons produces the emission of beta rays, and this led to the discovery of fission of uranium by the Fermi group on 2 December 1942 – the era of the power of the atom began <...>

The results of mineralogical–technological studies of PGM mineralization in zonal mafic–ultra mafic complexes of the Ural–Alaskan type are given. All studied massifs in the Urals and Kamchatka are characterized by similar evolution of mineral assemblages. The chromite (platinum–chromitite–dunite) and dunite (platinum–pegmatoid dunite) geological–economic types of small platinum deposits and occur rences are separate enriched sites (ore shoots) of largevolume platinum ore deposits. These are rather thick and extended zones of recrystallized dunites with attributes of hightemperature structural deformations and intense fluid reworking.

This chapter contains abbreviated descriptions of selected major uranium deposits or districts including metallogenetic concepts proposed by geoscientists who have worked on these deposits. The given deposits and districts are considered representative examples for the types of uranium deposits of established or potential future economic value. To provide an idea of the magnitude of the deposit or district described in the respective section, some figures on the resources and grades have been included in the introduction to this section. Related details on dimensions are provided under section Mineralogy in the deposit descriptions. For additional comments see Paragraph Remarks, Definitions, Units.  <...>

The stratiform deposits make up a special group of lead-zinc deposits possessing many common features in which they differ from the similar deposits of other industrial-genetic types.
They are characterized by ores confined to strata of carbonate rocks, most frequently dolomites, by ore bodies of predominantly stratal form represented by impregnation ores of simple mineral composition, within which galena usually predominates over sphalerite (rarely the reverse), by the absence of magmatic rocks of similar age to the ore in the vicinity of the deposits,