Baryte Mineralization Research Articles

Structural and Geochemical Characterization of Baryte Mineralization in Liji Area, Northern Benue Trough, Northeastern, Nigeria

Structural and Geochemical Characterization of Baryte Mineralization in Liji Area, Northern Benue Trough, Northeastern, Nigeria

Mineralogická charakteristika barytové mineralizace z lokality Ruda-hájenka (hornoměstský rudní revír, silezikum)

The previously unknown remnants of old mining activity were recently found at the locality Ruda-hájenka in the SW part of the Horní Město Ore District (Northern Moravia, Czech Republic). Partly weathered fragments of baryte mineralization in association with acid metavolcanites of the Vrbno Group (Devonian, Silesicum) were found in the dump material. Baryte mineralization exhibits a fine-grained marble-like appearance and locally contains minor disseminated pyrite. A detailed mineralogical study also revealed the presence of trace amount of other hypogene sulphides (galena and sphalerite), whose chemical composition is similar to those reported from the Horní Město Ore District. In addition, baryte also contains individual grains or aggregates of quartz, K-feldspar, and muscovite, which are often corroded and replaced by baryte. The silicates contain negligible amount of Ba (up to 0.02 apfu), which is only slightly higher than those in the same mineral phases from the host metavolcanic rock. The isotope composition of sulphur in baryte and pyrite indicates at least two different sources of sulphur (marine sulphate and likely sulphur leached from wall rocks) and isotope disequilibrium between co-existing minerals. The texture and mineral composition of the studied mineralization resemble metamorphosed baryte mineralizations occurring in the wider area (including local stratiform baryte bodies), but the absence of elevated contents of Ba in feldspars and especially in mica contradicts with an idea of Variscan metamorphic re-crystallization of the studied mineralization together with its host rock environment under the greenschist facies conditions. Therefore, one cannot exclude the possibility that it can be a post-metamorphic vein mineralization, which experienced intense deformation and recrystallization at very low temperatures, associated with rejuvenation of fault-related tectonic activity. The supergene mineral phases are represented especially by limonite, less frequent are minerals of the hollandite group (hollandite, coronadite, cryptomelane), anglesite, cerussite, and a not very well identified Ce-mineral, most likely cerianite-(Ce). Supergene origin is also presupposed for rarely found acanthite.

Geology of the Fe-Pb-Ag "Mina Rica" deposit, Pulpí (Almería, Spain)

The “Mina Rica” (the Rich Mine), located in the district of Pilar de Jaravía, in the municipality of Pulpi (Almería province, Spain), has become internationally renowned for the great geode of selenite gypsum discovered in its interior. The ore deposit is located in a NE-SW dextral shear band, affected by a system of NNE-SSW sinistral faults. The deposit is composed of two hectometric blocks of weakly deformed rocks with a pod shape, which are constituted by a folded and faulted alternation of limestone and dolomites, and to a lesser amount, gypsum and phyllites, all with a general NNESSW orientation and strong dipping to the W. In the time sequence of the mineral phases present in the “Mina Rica” we can distinguish a first stratabound, mineralization of iron carbonates that fossilizes the Serravallian age deformation. Baryte mineralization is associated with the Tortonian movements and celestine mineralization with the Messinian ones. Gypsum, which crystallized at a temperature of below 25ºC, was the last major sulphated mineral phase to be formed, and this took place after the Pliocene vertical replays. Moreover, this study – the cartographic underpinning of which has served as the basis for the recovery and musealization of the mine – has enabled us to discover the enormous potential that the “Mina Rica” has as a centre for geological and geo-mining practical teaching, beyond the indisputable lure of its Great Geode. We foresee that the results presented in this study will be the basis for the use of the “Mina Rica” as an educational tool to help train future generations of geologists and mining engineers.

Rare earth elements and stable sulphur (δ34s) isotope of baryte mineralization in Liji Area, Northern Benue trough, northeastern Nigeria

The Liji area lithologically consists of inliers of granite and pegmatite members of the Pan-African granitoids surrounded by Cretaceous sedimentary deposits of Bima, Yolde, Pindiga and Gombe Formations. Epigenetic fracture-filling baryte mineralization hosted by granite, pegmatite and Bima Sandstone were delineated, sampled and analyzed for rare-earth elements (REEs) and stable sulphur isotope geochemistry. The REEs of the distal (unaltered) rocks indicated normal values (26.15-36.81 ppm) before mineralization was marked by enrichment of light rare-earth elements (LREEs) (27.94 ppm) relative to the heavy rare-earth elements (HREEs) (5.34 ppm) and negative Eu anomalies typical of calc-alkaline granites of Pan-African age. The baryte separates were marked by enriched LREEs and depleted HREEs with pronounced positive Eu anomalies indicating the invasion and consequent deposition of baryte-rich hydrothermal fluid under oxidizing conditions in the N-S and E-W striking fractures. Stable sulphur isotope of the baryte gives values that ranged from 18.3 - 19.8o/oo CDT indicating that the source of sulphur is from ocean water and not from magmatic, fresh water and connate water sources from the nearby granite, pegmatite and sandstone.
 Keywords: Baryte, Mineralization, Hydrothermal, Liji, REE, Sulphur-Isotope.

Barytová mineralizace v granodioritovém porfyritu z Bělovsi u Náchoda (orlicko-sněžnické krystalinikum, Česká republika)

A new occurrence of baryte mineralization at Běloves near Náchod is bound to a steep NNE-SSW trending fissure in a dyke of granodiorite porphyrite, which cut phyllites of the Nové Město Group (Orlica-Sněžník Crystalline Complex). The mineralization is composed of three generations of baryte differing in Sr contents (~0.10 apfu in the oldest generation, ~0.003 apfu in the youngest generation) and small amount of hematite. The primary fluid inclusions in baryte belong to type L and L+V; the variable phase proportions are probably caused by postdepositional damage of part of the present fluid inclusions. The wide range of temperatures of both initial melting (-40 to -1 °C) and final ice melting (-0.3 to -12.3 °C) suggests involvement of fluids with very variable salt systems and salinities. The δ34S values of baryte range between +5.5 and +7.1 ‰ CDT. The mineral composition, chemical composition of minerals and fluid inclusion data suggest that the studied mineralization is similar to Late Variscan vein baryte and mineralizations of the Bohemian Massif. The source of fluids is interpreted in evaporated fresh waters of Permian lakes, which occurred in the adjacent Krkonoše Piedmont Basin during the Permian.

Field occurrence and geochemical characteristics of the baryte mineralization in Lessel and Ihugh areas, Lower Benue Trough, Nigeria

The Lessel and Ihugh areas are underlain by Precambrian rocks comprising of banded gneiss, medium-grained muscovite granite, coarse-grained biotite muscovite granite, and Turonian arenaceous Lessel Sandstone in the Lower Benue Trough, southeastern Nigeria. Baryte mineralization occurs at Lessel-Mbagwa, Ihugh and Bunde commonly as vein and cavity type deposits within NE-SW and NW-SE trending fracture zones. Major oxides and trace element analysis of baryte and the host rocks was undertaken using Inductively Coupled Plasma Mass Spectrometry (ICP-MS), in order to establish the geochemical characteristics and to constrain the origin of the baryte mineralization. The data revealed enrichment in Ba and Sr and depletion in SiO2, TiO2, Al2O3, Fe2O3, MgO, CaO, Na2O, K2O, LILEs, HFSEs relative to background values obtained from sandstones and granitic rocks in the area. Baryte mineralization from Lessel-Mbagwa, Bunde and Ihugh is marked by positive Gd (17.1–21.4) and negative Eu (0.02–0.05) anomalies. Negative Ce anomaly (0.06) is evident in barytes from Lessel-Mbagwa and Bunde whereas baryte from Ihugh is characterized by positive Ce anomaly (1.3). The structurally controlled nature of the mineralization, depleted major and trace elements concentration in the barytes in addition to REE anomalies indicate that mixing of a strongly differentiated residual Ba-bearing fluid and sulphur-rich seawater occurred under low temperature and oxidizing-reducing conditions. The tectonic event which occurred during the Santonian to Early Campanian reactivated the NE-SW, NW-SE structural pathways in the basement gneiss and also created similar structures in the Turonian Lessel Sandstone.

English

The use of DC electrical method in baryte mineral exploration has been investigated in Buruku northeast of Markurdi, Nigeria. The objective of the study was to investigate the suitability and potential of electrical resistivity tomography (ERT) combined with vertical electrical sounding (VES) surveys in baryte mineral exploration over known deposits. Results show that the interpreted layer resistivities correlate with the 2-D observations. The study delineated averagely 28 m deep symmetrically mound-shaped resistive anomalies (1500 to 5500 Ωm) encased within low resistive sandstone formation along prospective traverses. These responses are characteristics of probable vein structures associated with baryte mineralization. Two dominant E-W and NW-SE resistivity anomaly trends were delineated. The E-W trends were more prominent and persistent than the NW-SE. They are 25 to 50 m wide and stretches to over 300 m in length. The association of mineralized veins with these trends suggests that the veins must be of early Cretaceous age. These mineralized veins correlate with locations of known baryte deposits in the prospect area which hitherto, have been exploited by artisan miners. This is an obvious indication of the utility and resolution of dc electrical method in baryte mineral exploration in the area. Key words: Electrical resistivity tomography (ERT), Vertical electrical sounding (VES), resistivity, Baryte, vein and mineralization.

The baryte-bearing beryl-phosphate pegmatite Plössberg—A missing link between pegmatitic and vein-type barium mineralization in NE Bavaria, Germany

Pegmatites and aplites enriched in P, Be, Nb, Ta and Li occur in the high-temperature metamorphic lithological units of the NE Bavarian Basement, SE Germany. They are accompanied by Ba mineralization, in vein-type deposits in the basement as well as in its foreland. Locally, Ba minerals are encountered in the late Variscan pegmatites and aplites too. The shallow discordant stock-like pegmatites (Hagendorf-type) are barren as to Ba, but in the tabular, concordant aplites and pegmatites Ba was concentrated (Plössberg-type). These concordant pegmatites and aplites are supposed to be the root zone of the intrusive pegmatites. In the rare case of low sulfur fugacity, Ba forms Ba–Zr–K–Sc phosphates/silicates in the pegmatites (transition of magmatic into the hydrothermal stages I/II). Under high sulfur fugacity, Ba is accommodated within the same stages in the structure of baryte. Barium is not accommodated in the lattice of phosphates during or in the immediate aftermaths of the emplacement of these Be–P–Nb–Ta pegmatites (stage III). This element shows up again in APS minerals during supergene alteration under acidic conditions (stage IV). Considering the host rocks of baryte mineralization, the Sr contents of baryte increased from the early Paleozoic to the Late Triassic. The Sr contents of baryte are a function of the depth below ground in the vein-type deposits and in the shear-zones bounding the tabular concordant pegmatites. Beryl is not only a marker mineral for the shear-zone-hosted pegmatites but can also be used as a tool for the geodynamic positioning of these pegmatites using its oxygen isotopes. A subdivision of the pegmatites into intrusive and shear-zone hosted may be achieved by its REE and minor elements.

The Snelston Ridge: evidence for a concealed ridge of mineralized Dinantian rocks to the south of the Derbyshire Dome

SUMMARY Little is known of the southern continuation of the Lower Carboniferous (Dinantian) rocks of the Derbyshire Dome where they lie concealed beneath Triassic rocks at the margin of the Needwood Basin. Evidence from regional Bouguer gravity anomaly surveys pointed to the existence of a ridge of shallow Dinantian rocks, here called the Snelston Ridge, largely concealed by Triassic strata apart from two small inliers. The NNW–SSE trending ridge was proved by a borehole which intersected (Dinantian) Widmerpool Formation rocks at a depth of 61 m. Evidence from a seismic reflection profile indicates that the ridge, at least at Birchwoodpark (Snelston), is probably an asymmetrical, fault-controlled anticline. There is, however, no evidence for any significant changes in the thickness of Dinantian rocks hereabouts. The base metal potential of the Snelston Ridge was investigated using detailed geophysical and geochemical surveys and drilling. A borehole on the top of the mineralized mudmound that forms the Limestone Hill Inlier proved minor replacement galena–sphalerite–baryte mineralization with up to 10% Pb over an intersection of about 11 m. Two boreholes on the flanks of the feature revealed little sign of mineralization, indicating that it is restricted to the exposed dolomitized summit of the mudmound.

Mineralogy and Genesis of the Çanakçi (Ulukisla-Nigde) Baryte Vein Deposits, Central Turkey

The studied area is located around (~anakqi (Ulukisla) Village in the north of Bolkardag Unit, Central Turkey. The baryte mineralization occurs within Elmali vulcanite member belonging to UpperPalaeocene aged ~iftehan complex which overlies unconformably the Alihoca ophiolites. The complex on the basis of lithological features can be divided into four members; Kodak shale-sandstone, Elmali volcanite, Aktastepe limestone and Ugtepe monzonite-diorite. The Elmali volcanites consists of basalt, andesite and trachyte lava flows, hypabyssal rocks, pillow lava and agglomerate. The lava flows have a E W strike and are cut by hypabyssal rocks of different phases. The baryte mineralizations occur nearly 2km southeast-east and 3km southwest of ~anakgi village. The baryte mineralization in SW of ~anakgi village has nearly lm thick and 33m length. Many small veins of baryte, nearly parallel to the main ore, are also present in the surrounding areas. Baryte veins contain mainly some galena. Minerals were identified by ore microscopy, and major and trace element analyses were performed by the XRF method. Mineralogy Megascopically, baryte ore is crystall ine, white and p ink i sh white in colour . Microscopically, small amount of quartz is accompanied with baryte mineral. Baryte occurs mainly as euhedral but sometimes anhedral crystals. Baryte crystals are colourless, perpendicular sets of cleavage and greyish interference colours indicating small brefringence. Crystals are characterised by polysynthetic twinning, undulatory extinction due to mechanic terrain in common. Mechanic twinning and like moiler texture are also observed in minerals. Baryte is cut by very thin quartz, sphalerite and galena veins and some baryte inclusion formed in some quartz crystals, all of which indicates that baryte is formed early than quartz, sphalerite and galena. The baryte crystals may also show fibrous or prismatic habit with patchy extinction reflecting the presence of considerable stresses during or after the deposition of baryte. The common opaque minerals are mainly galena, and rare sphalerite, chalcopyrite, pyrite, covellite, ilmenite and fahlore. Secondary minerals are anglesite, malachite, azurite, smitsonite, iron oxide and cerussite. The gangue minerals are represented by quartz, calcite chlorite and muscovite. Chemistry Selected 4 samples from baryte occurrences were analysed for major and trace elements (Table 1). As seen in Table 1, there is a negative correlation between the Ba and Al203. Feldspar, muscovite and possibly some clay minerals are present in order to account for the A1203 content that ranges between 3.07-12.35%. FeO is very low (0 .1-0 .5%), suggesting that baryte mineralization occurred at very low temperatures. Extremely low Na20 and CaO contents show clearly that calcium and sodium enriched fluids did not come to deposition environment during the baryte mineralization. Na20 and K20 occur principally as soluble salts mostly taking the form of chlorides, MgO does not behave as a soluble salt. The main impurity is SiO2 (mainly in the form of quartz mineral) and ranges between 2.1-17.81%. High ratio of Cu (109-161ppm) and TiO2 (0.12-1.56 %) reveals that the mineralising fluids are of hydrothermal origin and mineralising fluids came up from through volcanics and intrusive rocks. S content of the baryte minerals are between 63984 and 74306 ppm suggesting that the baryte mineralization is epithermal in origin. In addition, the high Sr values (9605-13603ppm) reflect that the origin of Sr is related with volcanic activity. The very high BaJSr ratio implies that the origin of Ba is the hydrothermal (especially epithermal) origin (Werner, 1958; Starke, 1969). Zn content ranges from 2 to 793 ppm, suggesting that the baryte occurrence is related with volcanic activity (Marchig et al., 1985). Pb

The genesis of the west shropshire orefield: Evidence from fluid inclusions, sphalerite chemistry, and sulphur isotopic ratios

AbstractThe Pb + Zn + Ba veins of West Shropshire, England, occupy fractures in Ordovician and Precambrian rocks of the Shelve Inlier. Precipitation of sphaleritic ores was succeeded by galena + baryte mineralization, with chalcopyrite also occurring late in the mineralizing episode. Three generations of sphalerite are recognized, and second being chemically zoned with distinct Fe + Cd‐rich growth zones. Associated with these iron‐rich bands are smaller (∼ 10 μm) zones rich in indium (>1.0 wt%) and copper, electron electron probe microanalyses suggesting coupled substitution of Cu+ + In+3 in the ZnS. Based on the sequence of growth zones and their chemistry a sphalerite stratigraphy can be recognized within the orefield.Fluid inclusions studies reveal the mineralizing fluids to be highly saline (18–30 wt% CaCl2 equivalent) Na + Ca‐richbrines, with mineralizing temperatures in the range 200–120°C. A trend from higher temperature‐low salinity to low temperature‐high salinity fluids with time is recognized. Sulphide sulphur isotopic ratios are consistent and suggest a ΔS34SH2S of the mineralizing fluid of 10%, while 34Sbaryte values are in the range + 14 to + 19%, indicating separate sulphate and sulphide sulphur sources. The mineralogical, fluid inclusion, and isotopic data suggest the saline fluids rose into an open plumbing system where mineral precipitation was mainly controlled by fluid cooling. The baryte however, formed due to mixing with oan overlying sulphate‐bearing reservioir.Theree possible fluid sources are considered, namely: Lower Carboniferous seawater, basinal brines, and metamorphic fluids. However, the information available does not allow the source to be positively identified.

Geochemical and geological constraints on the formation of unconformity-related vein baryte deposits of Central Europe

Baryte vein deposits confined to the unconformity between Palaeozoic or Precambrian basement and the Permian–Triassic cover are of widespread occurrence in Central Europe. Age dating carried out on pitchblende predating and postdating baryte, indicates that baryte mineralization took place between Lower Permian and Lower Jurassic times (290 to 200 Ma). 87 Sr/ 86 Sr ratios exclude any derivation of ore-bearing fluids from a mantle source and point to a crustal origin. Sulphur was derived from sulphate and sulphide contained in the host rocks folded during the Variscan orogeny (Sudetian phase) and from the Permian and Mesozoic sedimentary cover. Strontium isotopes bear witness to a mixture of granite-derived strontium and strontium from the enclosing wall rocks. The unconformity is considered to be a first-order geohydraulic surface which favoured fluid migration via convective cells. The thermal convection may be related to Variscan granites which might have provided additional heat by the decay of U, Th and K.

Isotopic evidence for UK Upper Permian mineralization by bacterial reduction of evaporites

The dolomites (Ca Mg (CO3)2) of the Lower Magnesian Limestone (or Cadeby Formation, Upper Permian age) are believed to have been formed by evaporation of seawater and include sulphate also associated with that environment. Mineralization in the formation includes baryte (BaSO4) and galena (PbS) together with other sulphides and has been ascribed to many different modes of origin. Sulphur isotope analyses have now shown that the sulphates were derived from seawater of Upper Permian age and that sulphides in sites of former anhydrite (CaSO4) nodules were formed by bacterial reduction of sulphate. This latter point is confirmed by the carbon isotope composition of the carbonates whose oxygen isotope values indicate the possibility of admixture of meteoric water to the system. Other baryte mineralization directly involves Upper Permian seawater or evaporite sulphate, whereas smaller baryte occurrences and epigenetic galena mineralization show no such direct involvement.

Copper, lead, zinc and cobalt mineralization in the English Lake District: classification, conditions of formation and genesis

The copper, lead, zinc, and minor cobalt mineralization of the English Lake District has been classified on the basis of mineralogy, spatial distribution and geological setting of the veins, and age of mineralization. The two major types of mineralization are: (1) ‘chalcopyrite-pyrite-arsenopyrite’, of Lower Devonian (Caledonian) age, and (2) ‘galena sphalerite’ of early Carboniferous age. When the former is closely associated with granite intrusions, more complex mineral assemblages are found involving tungsten or molybdenum bearing phases. Also distinguished from these two major types are later assemblages which probably result from their alteration. A later (Upper Carboniferous–Permian) baryte mineralization is also present. Minor graphite and stibnite deposits, and the major haematite mineralization found in the area, are incorporated into the classification but are not discussed, since they have been dealt with by other authors. Using data from fluid inclusions and experimental data on particular mineral assemblages occurring in the major types of mineralization, estimates have been made of the temperatures and compositions of the ore-forming fluids. The Lower Devonian veins formed at temperatures in the range of 350–200°C with typical a S 2 , values of 10 −10 –l0 −16 atm and a O 2 of ~10 −25 –10 −45 atm or even less. The solutions were probably brines of low to moderate salinity (~5–10 equiv. wt% NaCl). The Lower Carboniferous veins formed at temperatures in the region of 110–130°C from highly saline brines (~23 equiv. wt% NaCl). Theories regarding the origins of the mineralization are also discussed. The distribution of Lower Devonian veins shows a clear relationship to the underlying composite granite batholith; the Lower Carboniferous galena-sphalerite veins show no such relationship, but tensional tectonic activity in the early Carboniferous may have provided a mechanism for the opening of fissures. The source of the mineralizing fluids forming the Lower Devonian veins may have been the Borrowdale Volcanic Group, with contributions from fluids associated with the granites, which are also likely to have provided a source of heat. The high salinities of the fluids producing the Lower Carboniferous veins suggest that seawater may have been involved in leaching the metals from basement rocks.

Native antimony and bournonite intergrowths in galena from the English Lake District

AbstractThe Driggith vein is representative of the lead-zinc mineralization in the Caldbeck Fells area, with a primary mineral assemblage consisting of quartz, baryte, calcite, chalcedony, pyrite, arsenopyrite, galena, sphalerire, bournonite, argentian tetrahedrite, and native antimony. Broadly similar assemblages are found in Pb-Zn mineralization of Upper Devonian to Permian age else-where in the Lake District. The paragenetic sequence appears to have been early pyrite and minor arsenopyrite associated with quartz; with later baryte, calcite, sphalerite, and chalcopyrite enclosed by galena. Within the galena occur inclusions of tetrahedrite, bournonite, and native antimony. A later stage of baryte mineralization was followed by the alteration of primary sulphides to secondary minerals. Elsewhere in the Lake District, galena occurring in this association also contains inclusions of native antimony, bournonite, and other sulphosalts, and in this respect differs from galena associated with earlier veins composed dominantly of chalcopyrite, pyrite, and arsenopyrite. The inclusions make a major contribution to the high antimony values reported in trace element analyses of galena from the Lake District. The occurrence of these inclusions, which in some cases display preferred orientation within the host galena, is discussed in terms of phase relations involving PbS and AgSbS2.

Trace element distribution in the superficial deposits of Northern Derbyshire, England

In an area of marginal farming, trace element distribution associated with lead, fluorite and baryte mineralization is important to the farmer because of the high infertility rate of the livestock and contamination of plant produce leading to the subsequent failure of the farming economy. Therefore sampling of superficial sediments was undertaken over the mineralized Carboniferous Limestone of North Derbyshire above the medieval lead and the modern fluorite workings. Twenty-seven elements were analyzed using emission spectrophotometry and subsequently compared with the geochemistry of the underlying bedrock. Discrepancies which occur are attributed to the glacial and periglacial action during the Wolstonian and Devensian glacial episodes.