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By H. A. Buehler

LOCATION THE Ozark region occupies a large part of the southern half, of Missouri, the northern portion of Arkansas and comparatively small areas in northeast Oklahoma, southwest Kansas, and southern Illinois. . It is a roughly elliptical plateau which has been deeply dissected by stream erosion, and which slopes imperceptibly into the prairie regions to the north, east, and west, but which terminates rather abruptly along the Arkansas River on the south and Tertiary lowland to the southeast. The-Boston Mountains extending for a distance of some 200 miles (321 -km.) along the Arkansas River rise to an elevation of 2000 ft. (609 m.), forming the most prominent topographic feature of the region. The so-called St. Francois Mountains in St. Francois, Madison, and adjoining counties in southeast Missouri, form a prominent but more restricted topographic feature, the highest point rising to an elevation of 1800 ft. (548 m.).. The remainder of the region is largely a plateau area varying from 800 to 1500 ft. (243 to 457 m.) in elevation. STRATIGRAPHY The region is underlain chiefly by sedimentary formations, which outcrop in roughly concentric bands around a comparatively restricted area of igneous rocks in the St. Francois Mountain district. Although located geographically near the eastern edge of the Ozarks, the St. Francois Mountains have apparently suffered the greatest orogenic movement and the lowest formations of the succession are exposed in their immediate vicinity. The various sedimentary formations of the region do not show any considerable metamorphism and have suffered little change since consolidation. With the exception of a few basic intrusions in Ste. Genevieve County and a pegmatite dike in Camden County, Missouri, there is no evidence of igneous-action, since the first sedimentary beds were deposited.

Jan 10, 1917

By G. W. H. Norman

INTEREST in the mineral possibilities (gold, copper) of northern Quebec, north of the Quebec-Cochrane branch of the Canadian National railway, has centred for many years in the Chibougamau district (see Figure 1). Since 1934, however, promising gold discoveries in the Rose Lake-Florence River section, 115 miles southwest of Chibougamau lake, have widened the interest, and prospectors have examined other parts of the country between Chibougamau lake and Bell river and the surrounding districts. The object of this paper is to !resent an outline of the geology, and to describe the mineral deposits, o part of this region, or, more specifically, of the part embraced by the Opawica-Chibougamau and Waswanipi map-areas(l), which include the districts about Chibougamau lake and Rose lake-Florence river, where mineral deposits are now in course of development either by surface or underground work. Early discoveries, developments, and explorations in the Chibougamau district are well summarized in the report of the Chibougamau Commission, published in 1911(2). The Commission discredited previous optimistic accounts of mineral discoveries in the area, made initially in 1903, but at the same time they expressed the opinion that, from a geological standpoint, the district promised a reward to diligent and intelligent prospecting. Their general conclusion-that prospecting in the area was not then (1911) commercially advisable in view of its inaccessibility and other handicaps shifted interest from the district until, some years later, valuable discoveries were made in the Rouyn area, and aircraft widened the field of successful exploration. During the past ten years or so, considerable energy has been spent in promoting the development of the district. The net result has been the discovery of a number of prospects, the majority of which have been explored only by trenching and, in most cases, diamond drilling.

Jan 1, 1936

By J. F. Wright

Gold-bearing quartz veins and replacement chalcopyrite deposits are the two important types of metallic mineral deposits of the east central Manitoba mining district. The gold-bearing veins occur along Manigotagan valley, northwest for 25 miles from Beresford lake, and the copper deposits along Oiseau valley, between Oiseau lake and the east end of Lac du Bonnet. Lithium-bearing minerals of possible commercial value have recently been discovered in pegmatite along Winnipeg river about 10 miles east of Point du Bois. There are also prospect pits with showings of galena, sphalerite, cobaltite, pentlandite, nickeliferous pyrrhotite, arsenopyrite, pyrite, molybdenite, cassiterite, and other minerals, but the various occurrences of these minerals, as exposed, are small. The bedrock and mineral deposits of this mining district are Precambrian and resemble in many respects the formations and mip.eral occurrences of western and northern Ontario. Although prospectors visited eastern Manitoba at intervals during the last fifty years, effective prospecting did not begin until 1913 or 1914, and not until 1923 were skilfully directed, systematic explorations undertaken. It is true, that between 1913 and 1923 considerable sums were expended in a number of attempts at mining and milling the gold-quartz ore, but these enterprises failed partly through poor management or attempts to develop veins that were too small or too low-grade to be worked at a profit under the existing conditions of transportation and power supply.

Jan 1, 1925

By Virginia T. McLemore

The Gallinas Mountains are in northern Lincoln County and southern Torrance County, New Mexico, USA where a series of alkaline igneous bodies, including porphyritic latite, trachyte/syenite, andesite, and rhyolite laccoliths, flows, dikes, and plugs, have intruded Permian sedimentary rocks belonging to the Permian Abo, Yeso, and Glorieta Formations. A small amount of bastnaesite, a REE mineral, was recovered during processing for fluorite from the Gallinas Mountains. Four types of deposits are found in the Gallinas Mountains: epithermal REE-F veins, Cu-REE-F veins, REE-F breccia pipes and iron skarn deposits; all are associated with Tertiary alkaline to alkalic-calcic igneous rocks. Alteration includes brecciation, silicification, chloritization, and fenitization. District zonation is defined by Cu-REE-F (±Pb, Zn, Ag) veins that form center of the district, surrounded by REE-F veins. Carbonatites are inferred at depth by the presence of fenitization, carbonatization of the breccias, presence of REE and similarity of the intrusive rocks and mineralization to areas with known carbonatites.

May 1, 2011

By Stanley W. Ivosevic

The South-Central area of the Osa Peninsula, Puntarenas Province, on the Pacific coast of southern Costa Rica, may have produced on the order of 30,000 kg (100,000 troy oz) of gold since prehistoric times. The Peninsula lies along an 800- to 900-km-long belt of late Mesozoic eugeosynclinal rock deposition, hydrothermal activity, and deformation (Campanian). The oldest rocks exposed in the area are basalt and tuffaceous mudstone of the Late Jurassic or Cretaceous Nicoya ophiolite complex. The Nicoya Complex is overlain by weakly lithified Pleistocene Older Sediments, predominantly conglomeratic sandstone and derived from erosion of the Nicoya Complex. Erosion reduced the Complex to a surface of high relief, so that the detrital source was in the area originally; the source retreated with subsidence. Stratigraphically, the Older Sediments are followed by surficial deposits of intermediate age, consolidated Younger Sediments reworked from Older Sediments, and unconsolidated Holocene surficial deposits reworked from Younger Sediments. The most prominent structures are a northeast-trending anticline and northeast and northwest fault sets. Some deformation was Cretaceous, but folding and much faulting occurred after deposition of the Older Sediments. Remnants of plainlike features and destructional terraces on the Older Sediments attest to stepwise downcutting of the terrain during successive stages of uplift. Near the end of this process, the present valley floors and coastal headlands developed. During a probable epeirogenic rise in sea level, Younger Sediments filled the valley bottoms and an aggradational coastal plain developed. Sea level dropped by stages and with some reversals to its present position; this caused stepwise incision of the valley fill, stepwise beveling of the coastal plain, and development of the present wave-cut platform. Spilitization around the time of the Campanian orogeny caused some parts of the Nicoya complex to be calcitized and others to be silicified. Gold, pyrite, and probably additional silica were introduced during subsequent hydrothermal activity. Native gold was eroded from Nicoya Complex lodes and reconcentrated through three generations of placer gold deposits. First, the gold was deposited as a detrital.

Jan 1, 1977

By W. E. Cockfield

THE object of this paper is to review recent geological work in the Cariboo district and to present notes on the recent development of mineral properties. The Geological Survey has done considerable work in the Cariboo district, extending over a period of years. In 1885 and 1886, Bowman (1) mapped the geology of a large area. In 1922 and 1923, Johnston and Uglow (2) mapped Barkerville area in some detail and prepared a report on the placer and lode gold deposits. In 1931 and 1932, Cockfield and Walker (3) mapped the Quesnel Forks area. In 1933, Hanson reported on Willow River area ( 4), and in 1934 made a detailed examination of part of the Barkerville area (5). In 1935, Lang commenced work on the Keithley area, lying to the southeast of the Barkerville area, and in 1936 published a preliminary re-port (6). The work on Keithley area was continued in 1936 by both authors of the present paper. As the results of the earlier work have been published, this paper will be concerned largely with Keithley area, that is, the part of the region lyinp between longitudes 121° 00' and 121° 30', and latitudes 52° 45' and 53° 00 . This area lies astride Cariboo (Swamp) river and extends north some 17 miles from Keithley, which is situated near the southern border of the map-area (see sketch-map). Points in the western part of the map-area are fairly accessible. A road extends from Barkerville to upper Cunningham creek, and from this a trail crosses Snowshoe plateau to Keithley. A second trail from this road leads to the lower falls on Cariboo river. From this road, a branch road leads to upper Antler creek, with a trail leading from this branch road to Keithley. Part of this western half of the area is made up of the Snowshoe plateau, which constitutes a gently rolling surface, at or above timber line, where trails are largely unnecessary.

Jan 1, 1937

By Howard W. Tipper, Richard B. Campbell

"The Quesnel Trough is underlain by a thick sequence of mainly Upper Triassic and Lower Jurassic volcanic-clastic and sedimentary rocks that lie between the highly deformed Proterozoic and Paleozoic rocks in the Omineca Geanticline to the east and the Upper Paleozoic Cache Creek Group in the Pinchi Geanticline to the west. Broad areas of the Trough between Kamloops and Williams Lake are covered by Eocene volcanics and sediments and by Miocene-Pliocene plateau lava. Granitic intrusions were apparently mainly confined to two major episodes; one about 200 m.y. ago (coeval with the Guichon batholith) and one about 100 m.y. ago. In addition, the region includes small granitic and syenitic intrusions, some porphyritic, that may be all or partly still younger. Exposures in the region are generally small and scattered, obscured by widespread, not necessarily thick glacial deposits. This, together with the extensive Tertiary cover, makes prospecting difficult. The part of the Quesnel Trough discussed here is the direct northwest-ward extension of the copper-rich Kamloops-Merritt-Princeton region. It contains the Boss Mountain molybdenum mine, related to a breccia zone induced in a batholith of the oldest group by a younger intrusion, and the Cariboo Bell copper deposit in Lower Jurassic volcanic-elastic rocks and syenitic intrusions. The Gibraltar deposit, in a 200-m.y. intrusion, is within the Pinchi Geanticline close to the margin of the Trough. Molybdenum prospects are mainly restricted within or near the 100-m.y. granitic rocks. Copper prospects, on the other hand, are most prominent in the volcanic-elastic rocks and in the 200-m.y.-old granitic rocks, although they can also be spatially related to younger intrusions. Copper thus has a wide potential distribution.The writers believe that the region is deserving of careful and comprehensive exploration by directly applying the knowledge and techniques developed in the important producing areas to the south. All of the major pre-Tertiary geological elements seem to have potential for mineral deposits; none should be ignored. A thorough knowledge of the thickness and distribution of the Tertiary rocks and the development of geophysical methods to ""see through"" them is of particular importance."

Jan 1, 1970

By Jean-Louis Robert

Field work inaugurated in 1962 in the townships of Lemieux and Lesseps, in the Gaspe Peninsula of Quebec, has permitted the author to delineate the lithologic units of the area, to elucidate a few stratigraphic problems and to outline several zones of alteration. Certain features of these zones and the numerous mineralized showings in the area merit the attention of prospectors and exploration companies.

Jan 1, 1966

By R. W. Wittkopp

The Relief Canyon gold deposit is located approximately twenty- four kilometers east of the town of Lovelock in Northwestern Nevada. At Relief Canyon, the Late Triassic Grass Valley Formation has been thrust over the Late Triassic Natchez Pass Formation. The lower plate Natchez Pass Formation is composed of massive gray dolomitic limestone which is locally silty and sandy. The upper plate Grass Valley Formation is composed of shale, siltstone, argillite and quartzite. Gold mineralization at Relief Canyon occurs along the highly brecciated thrust contact between these two formations. Weak gold mineralization often occurs above the thrust in the Grass Valley Formation, however, most of the ore grade mineralization is present below the thrust in the brecciated Natchez Pass Formation or where the two formations are mixed as a result of movement along the thrust. Several types of gold mineralization have been recognized at Relief Canyon. A large amount of the ore is present as a jasperoid breccia, however, significant amounts of ore occur as a mixed breccia composed of upper plate rock, fresh limestone, clay and jasperoid breccia. Gold ore also occurs in a fresh limestone breccia which contains a large amount of clay. Below masses of jasperoid, jasperoid stringers containing gold extend into the fresh limestone. Gold mineralization at Relief Canyon appears to be truly disseminated and has the typically associated trace elements of arsenic, antimony, mercury and fluorine. The Relief Canyon deposit can be classified as a structurally controlled disseminated gold deposit. Other deposits that fit this classification are the Pinson and Dee gold mines.

Jan 1, 1984

By M. D. Johnson

The San Andres mine, located in the western mountain region of Honduras, Central America, contains epithermal gold mineralization as disseminations, in quartz-chalcedonic veins and stockworks. Host rocks include a thick sequence of Cretaceous to Tertiary conglomerates, sandstones, rhyodacite tuffs and andesites. Mineralization is controlled by northwest and northeast striking, normal faults and fractures which dip steeply east and west. Currently, 500 STPD of 1. 93 Grams/MT gold ore is being open-pit mined from the conglomerate and andesite. The mine is at the west end of a mineralized zone that can be traced over an area of approximately 1.5 square kilometers.

Jan 1, 1993

By L. R. Chimimba

"The Trojan nickel deposit occurs within a pile of ultramafic lavas subjected to a lower amphibolite grade of metamorphism. The lavas form part of the Upper Greenstones (Bulawayan Group) of the Mazoe greenstone belt. The nickel mineralization occurs as disseminated, massive and near-massive sulphides. The massive and near-massive ore occurs along the basal contact of the serpentinite units and is overlain by the more abundant disseminated ore, which occurs within the serpentinite. The main sulphide minerals are pyrrhotite. pentlandite and chalcopvrite. Minor amounts of millerite and pvrite are present. The Ni : Cu ratio in all three types of ore averages 15:1.The intercumulus nature of sulphides in the near-massive ore and similar textures occasionally seen in the disseminated ore indicates a magmatic origin of the mineralization. The basal position of the near-massive and massive ore suggests that the sul­ phides settled out under gravity during the emplacement and crystallization of a peridotitic magma. The deposit has been deformed and some of the primary massive ore has been remobilized into veins and breccias. The disseminated mineralization now occurs mainly as blebs of sulphides intergrown with silicate minerals or as stringers of sulphides between foliation planes in the serpentinite."

Jan 1, 1984

By Paul Kents

The Canadian Javelin Limited Cerro Colorado copper-porphyry deposit in Panama, possibly the largest known copper-porphyry, contains between 1350 and 450 meter elevations, drill proven and probable ore in excess of 3.0 billion tons averaging 0.65% of copper equivalent. The deposit is located in the Central Cordillera Range, straddling the Continental Divide at 1500 meter elevation. Local topography is very steep. Accessibility is difficult, all logistics made by helicopter, and only recently a 52 km. road from the Pan-American highway was completed into the area. The deposit was discovered in 1969, and since then 75 shallow exploratory holes and 98 deep holes, the deepest 1340 meters, totalling 45,000 meters have been drilled. Deep holes were drilled at the corners of a regular rectangular 150 meter grid.

Jan 1, 1975

By Ward Sumner

The Jones Hill prospect is a Proterozoic age, volcanogenic, semi-massive to massive sulfide deposit. The deposit is located on the western edge of the Pecos greenstone belt in the southern Sangre de Cristo Mountains of northern New Mexico. The prospect is found in a block (West Block) of meta- igneous rocks, primarily diabase, metavolcanic rocks, and metasedimentary rocks (fig. 1). This assemblage is typical of lithologies found in the greenstone belt. Metamorphic grade is greenschist to lower amphibolite. The West Block is bound- ed on the west by Proterozoic age (1.7-1.4 b.y. by Rb/Sr), granitic plutons collectively called the Embudo granite, and on the east by Paleozoic sedimentary rocks, primarily sandstones, shales, and limestones of Mississippian and Pennsylvanian age. The mineralization occurs in a single horizon which has been overturned and cut into two blocks by a high-angle reverse fault (fig. 2). The mineralized horizon is found at the contact of felsic metavolcanic and rnetavolcaniclastic rocks with overlying intermediate metasedimentary rocks. The local stratigraphic sec- tion from bottom to top is as follows: 1) porphyroblastic quartz- sericite schist (originally a rhyolitic, subvolcanic intrusive); 2) quartz-sericite-chlorite-biotite schist (felsic metavolcanic and metavolcaniclastic rocks); 3) chlorite-talc-biotite-sulfide schist (altered felsic metavolcanic rocks); 4) carbonate-quartz-sulfide [ ] chlorite-tremolite-talc schist (mineralized exhalite); 5) quartz- chlorite schist (silicified tuff); and 6) amphibole-chlorite-feldspar- biotite schist (occasional mafic to intermediate metavolcanic flows).

Jan 1, 2013

By James F. Allan

"Abstract -The Kipawa yttrium-zirconium prospect is located about 150 km south of Noranda, Quebec . Yttrium-zirconium mineralization occurs in an elongate, regionally metamorphosed and deformed peralkaline complex in the Grenville terrain. The mineralized zone, as defined by ? 0.10% Y203, is 1300 m long and 10 m to 30 m wide. Zirconium content typically ranges from 0.50 to 1.20% Zr02. The mineralized zone strikes northwest and dips 20 degrees to 35 degrees to the southwest. It occurs at the structural base of the peralkaline complex in syenite gneiss and cale-silicate rocks and is conformable with both the footwall contact of the complex, and the layering and gneissosity in the enclosing rocks. Minerals of economic interest are eudialyte (sodium-zirconium silicate), mosandrite (sodium-titanium silicate), britholite (calcium-silica phosphate), and a few other uncommon zirconium and titanium silicate minerals.The highest and most continuous yttrium grades occur in the upper part of the syenite gneiss unit in areas containing eudialyte, mosandrite and rninor britholite. Yttrium also occurs in britholite in cale-silicate rocks and in mosandrite in syenitic rocks in the lower part of the syenite gneiss unit. Both the yttrium-bearing minerals and yttrium grades are erratic in the lower part of the unit. Zirconium is generally more uniformly distributed than yttrium. A peralkaline granite gneiss phase of the complex intrudes the syenite gneiss and possibly truncates it, and the mineralization, near the southern boundary of the mineralized zone.The mineralized zone is coincident with a radiometric anomaly and discontinuous yttrium and zirconium soil anomalies.More drilling and metallurgical studies will be required to determine the economic viability of the yttrium and zirconium mineralization at Kipawa."

Jan 1, 1992

By Kah Lert

"The Red Mountain porphyry molybdenum deposit is situated in the Big Salmon Range, approximately 80 km east-northeast of Whitehorse, Yukon.Red Mountain is underlain by Paleozoic, argillaceous sedimentary rocks of the Yukon Cataclastic Complex, which have been intruded by a multi-phase mid-Cretaceous stock.Mineraliwtion, quartz stockwork, metal zonation, and an alteration assemblage characteristic of a porphyry molybdenum system have been superimposed on quartz monzonite porphyry and adjacent homfelsed sedimentary rocks. A later, barren and pyritic quartzeye diorite porphyry body and related dikes have dissected the quartz monzonite porphyry, homfelsed sedimentary rocks and associated molybdenite mineralization.Drill-indicated geological reserves of molybdenum mineralization outlined consist of 187 270 000 tonnes grading 0.167% MoS2.IntroductionLocationThe Red Mountain porphyry molybdenum deposit is located at 60°59'N, 133°44'W (NTS 105 C), approximately 80 km east-northeast of Whitehorse, Yukon. The property is situated within the rugged Big Salmon Range, 15 km east of the north-northwest-trending Teslin River. Red Mountain, at an elevation of 1702 m, consists of relatively steep, talus covered slopes with prominent gossanous bluffs marking the southeast flank. Relief on the property is 700 m, with tree-line at an elevation of 1450 m to 1500 m (Fig. 1)."

Jan 1, 1995

By W. D. Hausel

The Wyoming Province is an Archean craton which underlies portions of Idaho, Montana, Nevada, Utah, and much of Wyoming. The cratonic block consists of Archean age granite-gneiss with interspersed greenstone belts and related supracrustal terranes exposed in the cores of several Laramide uplifts. Resources found in the Province and in the adjacent accreted Proterozoic terrane include banded iron formation, Au, Pt, Pd, W, Sn, Cr, Ni, Zn, Cu, and diamonds. The Province shows many similarities to the mineral-rich cratons of the Canadian shield, the Rhodesian and Transvaal cratons of southern Africa, and the Pilbara and Yilgarn blocks of Western Australia, where much of the world's precious and strategic metal and gemstone resources are located.

Jan 1, 1991

By Dean G. Heitt

"The Rain and SMZ mines from 1987 to 1994 produced a total of22.0 t of gold from a pre-mine reserve of 14.24 Mt of ore grading 2.13 g/t Au.Gold at Rain is hosted within the basal portion of the Mississippian Webb Formation. ·Mineralization is closely tied to the Rain Fault which is interpreted to be the main feeder for the deposit. Multiple collapse and hydrothermal breccia events provided permeability for the mineralizing fluids in the otherwise unreactive siltstones. Major alteration events include: decalcification and dolomitization of the Devils Gate Limestone; and silicification, baritization, argillization and oxidation of the Webb Fm. Six ore types based on XRD and visual rock chip Jogging have been identified: siliceous ore containing >40% quartz and <30% barite; siliceous-baritic ore containing mostly silica but >30% barite; baritic ore containing >40% barite; argillaceous ore containing >40% total clays (including alunite); calcareous ore containing mostly calcite and dolomite; and carbonaceous ore which has significant pyrite and organic carbon. Metallurgical testing of the oxide leach grade ores found that recoveries, on -1.3 cm crushed material, were greater than 70%. Results also found that Rain ore has strong grind dependency due to silica encapsulation.The Rain leach pad was commissioned in 1988, and to date 9.3·Mt at an average grade of0.65 g/t Au have been placed. Life to date recovery, through December 1995, is approximately 51 %, for a total of3.87 t of gold produced. Two major factors have contributed to the low leach recoveries at Rain when compared with the metallurgical testing: 1) More argillaceous ore than expected was placed on the pad especially late in the mine life and 2) approximately 50% of the tons placed were run-of-mine with no agglomeration."

Jan 1, 1997

By V. N. Kolesnikov

The Sikhote-Alin part of the Circum-Pacific Ore Belt is characterized by wide distribution of Sn, Pb, Zn, W; Au, Ag, and other mineralization. This mineralization is regionally associated with the Late Cretaceous-Tertiary East Sikhote-Alin volcanic belt where it overlaps the Taukha accretiollary-wedge terrane of the Early Cretaceous age. The Pb-Zn deposits of the Dalnegorsk ore district may be grouped into the skarn (about 80%) and vein types. The skarn deposits are of major commercial value. Their geological position is controlled by the carbonate units located within tectonic melange of the Taukha terrane. Some other lithological and tectonic factors also play a significant role ill distribution of the mineralization. The ore bodies are traced to the depth of 1000-1500 m below the surface, having a pipe-lens shape and vertical zonation. Major minerals of the ores are galena, sphalerite, pyrrhotine, chalkopyrite, hedenbergite, quartz, and calcite. The minor elements of the Pb-Zn mineralization are cadmium, silver, bismuth, and copper. The paper describes relationships between mineral suites and minor element contents in the ores, as well as their significance for processing the ores. The metallurgy applied allows high recovering of the major components (Pb -93.9%; Zn -91.4%). However the tails contain some minor components that may be of commercial interest.

Jan 1, 1998

By E. Marcoux, F. Lotfi, A. Belkabir, L. Maacha, A. C. Brown, S. Brunet

"Koudiat Aïcha is a small Zn-Pb-Cu deposit, enclosed in the Visean Sarhlef volcano-sedimentary series of the Moroccan Hercynian Jebilet massif. Base metal mineralization is located between a basal unit consisting of black argillite with arenite intercalations, and an upper unit composed of black argillite with locally fossiliferous calcareous units towards the top. Paraconcordant gabbro sills are present in both the upper and basal units, and the enclosing strata. Three successive phases of deformation linked to regional deformation overprint the volcano-sedimentary rocks and gabbros, as well as the sulfide mineralization.The mineral deposit includes several lenses of massive to semimassive pyrrhotite, 1 to 20 m thick, with a large halo of disseminated sulfide veinlets and sulfide nodules within a zone of intense chlorite alteration in the footwall. The ore mineralogy consists of massive to semimassive pyrrhotite with lesser amounts of sphalerite, chalcopyrite, arsenopyrite, galena, pyrite, and stannite.Lead isotope results (206Pb/204Pb averaging 18.27) suggest that the metals of the Koudiat Aïcha deposit are derived from the volcano-sedimentary host rocks. Sulfur isotopes also indicate a volcano-sedimentary origin, with bacterial reduction of sulfate (d34SCDT = -7.5‰ to -10.5‰). The conditions for sulfide meta-morphic equilibration range from 250° to 330°C (sphalerite and chlorite geothermometers). The gabbroic sills could have been a local heat source for hydrothermal circulation. Based on these geological and mineralogical features, a Besshi-type model seems appropriate for the genesis of the Koudiat Aïcha mineralization.Koudiat Aïcha est un petit dépôt de Zn-Pb-Cu, encaissé dans la série volcano-sédimentaire Viséenne de Sarhlef dans le massif Hercynien de Jebilet au Maroc. La minéralisation en métaux usuels se situe entre une unité basale d’argilite noire interlitée d’arénite et une unité supérieure composée d’argilite noire comprenant localement des calcaires fossilifères près de son sommet. Des sills de gabbro paraconcordants sont présent à la fois dans les unités basale et supérieure, ainsi que dans les strates environnantes. Trois phases de déformation successives associées a la déformation régionale superposent leurs effets sur les roches volcano-sédimentaires, les gabbros, ainsi que la minéralisation sulfurée. Ce gîte comprend plusieurs lentilles de pyrrhotite massive a semimassive de 1 a 20 m d’épaisseur au sein d’un large halo de veinules de sulfures disséminés et en nodules au sein d’une zone intensément chloritisée dans le mur du gisement. Le minerai consiste en pyrrhotite massive à semimassive avec des quantités subordonnées de sphalérite, de chalcopyrite, d’arsénopyrite, de galène, de pyrite, et de stannite. Les résultats de l’analyse des isotopes du plomb (206Pb/204Pb moyen de 18.27) suggèrent que les métaux du gîte Koudiat Aïcha proviennent des roches volcano-sédimentaires encaissantes. Les isotopes du souf¬fre indiquent eux-aussi une origine volcano-sédimentaire, impliquant la réduction bactérienne des sulfates (d34SCDT = -7.5‰ et -10.5‰). L’équilibration métamorphique des sulfures s’est produite entre 250° et 330°C (géothermomètres à sphalérite et chlorite). Les sills de gabbro pourraient avoir été la source de chaleur locale responsable de la circulation hydrothermale. Sur la base de ces caractéristiques géologiques et minéralogiques, il semble approprié d’invoquer un modèle de type pour Besshi pour expliquer la genèse de la minéralisation de Koudiat Aïcha."

Jan 1, 2008

By J J. Wilkinson, C J. Ha, R J. Herrington

The Pic de Fon iron oxide deposit is a potential major new source of iron ore, located at the southern end of the Simandou range in eastern Guinea on the West African Craton. The deposit is hosted by banded iron formations (BIFs) within a supracrustal sequence, which lies unconformably upon a crystalline basement. The host BIFs and shales have been metamorphosed up to staurolite-grade itabirite and phyllite respectively. Stratigraphic relationships are obscured by polyphase deformation, although the sequence appears to comprise a lower phyllite(-minor quartzite) unit and transitional phyllite-iron formation overlain by three itabirite units. It is the itabirite units, selectively enriched to iron grades in excess of 65 per cent Fe (with low deleterious elements), that constitute the Pic de Fon deposit. Samples acquired from exploration diamond drill holes and outcrop across the deposit have been collected to investigate the Pic de Fon lithologies and iron-rich material types. Initial research techniques have included geological mapping, reflected light microscopy, x-ray diffraction (XRD) studies and ICP-AES geochemistry. The aim is to develop a model for deposit genesis that may assist future exploration and deposit exploitation planning. Results to date have identified a variety of hematite textures, which include recrystallised trellis, interlobate and granoblastic hematite after magnetite. In addition, fine-grained bladed to acicular microplaty hematite appears to both replace itabirite banding and infill porosity. Field relationships indicate a structural control of microplaty hematite development. Geochemistry and XRD results suggest a loss of silica with negligible iron addition during the conversion of itabirite to ore grade mineralisation. The enrichment process(es) is also accompanied by a gradual increase in K, Mg, Na, (Ca and Al).

Jan 1, 2005