Pelvic tenderness is not limited to the prostate in chronic prostatitis/chronic pelvic pain syndrome (CPPS) type IIIA and IIIB: comparison of men with and without CP/CPPS

Background: We wished to determine if there were differences in pelvic and non-pelvic tenderness between men with chronic prostatitis/chronic pelvic pain syndrome (CP/CPPS) Type III and men without pelvic pain. Methods: We performed the Manual Tender Point Survey (MTPS) as described by the American College of Rheumatology on 62 men with CP/CPPS Type IIIA and IIIB and 98 men without pelvic pain. We also assessed tenderness of 10 external pelvic tender points (EPTP) and of 7 internal pelvic tender points (IPTP). All study participants completed the National Institutes of Health Chronic Prostatitis Symptom Inventory (NIH CPSI). Results: We found that men with CPPS were significantly more tender in the MTPS, the EPTPS and the IPTPS. CPSI scores correlated with EPTP scale but not with IPTP scale or prostate tenderness. Prostatic tenderness was present in 75% of men with CPPS and in 50% of men without CPPS. Expressed prostatic fluid leukocytosis was not associated with prostatic tenderness. Conclusion: Men with CP/CPPS have more tenderness compared to men without CPPS. Tenderness in men with CPPS is distributed throughout the pelvis and not specific to the prostate

Geology of the Tanami Gold Mine, Northern Territory

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Geology of the Tanami gold mine, Northern Territory

The Tanami Gold Mine (TGM) is situated 600km NW of Alice Springs in the Paleoproterozoic 'Granites-Tanami Inlier' of Northern Australia. The deposit, which was discovered in 1904 and has been mined intermittently since, is one of several gold-only deposits that occur in the inlier. The host rocks to gold mineralisation at the TGM are a sequence of northwest-dipping, interbedded tholeiitic pillow-basalts and volcaniclastic-sedimentary rocks. The sediments were deposited by mass-flow mechanisms in a below wave-base subaqueous environment. The wholerock geochemistry of the basalts is similar to that of rift tholeiites, consistent with an intracontinental tectonic setting at the time of basalt eruption. The presence of hematite and high-grade metamorphic detritus in the sedimentary lithologies is also consistent with an intracontinental tectonic setting. The deformational history of the Tanami area involved two sub-orthogonal episodes of folding that generated northeast-trending Fl folds and northwest-trending F2 folds. Interference between the two fold generations has created dome and basin interference patterns. Illite-crystallinity measurements of sandstones and siltstones from the TGM indic~te diagenetic temperatures, probably less than 250¬¨‚àûC. The metamorphic grade, intensity and number of deformations at the TGM are less than at the 'Granites Gold Mine and elsewhere in the inlier. The host rocks to the mineralisation at the TGM (Black Peak Formation) are therefore interpreted to be younger than at the Granites (Ditjiedoonkuna Suite). Intracontinental rifting during the Palaeoproterozoic Leichardt rifting event (1810-1740Ma) created a small rift basin into which the Black Peak Formation was unconformably deposited onto a Archaean/Paleoproterozoic metamorphic basement. The Granites-Tanami Inlier is intruded by at least two distinct granite suites; the Mt Winnecke Suite (1830-1815Ma) and the Gregory Suite (1800-1790Ma). The granites in both suites are dominantly reduced, I-type granites that are enriched in incompatible elements. Gold mineralisation at the TGM is hosted within a complex sinistral wrench-fault array and associated veins and alteration halos. The main mineralised faults trend approximately NS and dip steeply east. Subsidiary structures trend at 030¬¨‚àû and 070¬¨‚àû and dip southeast. Economic gold mineralisation occurs within quartz-carbonate veins and in the surrounding sericite + quartz +pyrite¬¨¬± carbonate alteration halos. High-grade southeast-plunging, oreshoots are present where the mineralised fault trends intersect. Detailed structural studies indicate that the main mineralising event post-dated the bulk of F1 shortening, and was synchronous with the emplacement of felsic dykes into the mine sequence. Stress inversion calculations, based on fault striation populations, have revealed that at the time of the Au mineralising event, ˜ìvâ1 was sub-horizontal and SE-NW directed with ˜ìvâ2 subvertical. This contrasts with the pre-mineralisation deformation which occurred under a similarly directed ˜ìvâ1, but with ˜ìvâ3 sub-vertical. Flipping of the stress axes has allowed for the formation of steeply-dipping faults that were effective fluid focussing zones during the mineralisation event. A range of internally deformed vein textures and the presence of crack-seal and extension veins are evidence for cyclic fault rupturing caused by variations in the fluid pressure, shear stress and permeability of the fault zone. Mass balance calculations undertaken on the sericitic alteration assemblages that are spatially associated with Au mineralisation indicate addition of K, and volatiles (mainly C02 and S), and leaching of Si and Na, which caused minor volume loss during the metasomatic event. Fluid inclusion studies have revealed the presence of high-temperature (300¬¨‚àûC), low-salinity (5 wt.%) fluids with low C02 contents. Sulfur and oxygen isotope data are consistent with a hybrid magmatic/contact-metamorphic origin for the ore-forming solutions, which are inferred to be related to granite emplacement. During migration through the footwall the fluids, partly re-equilibrated with wallrocks to acquire their characteristic isotopic and geochemical compositions of ˜í¬•34S‚Äöv¢v†12‚ÄövÑ‚àû, ˜í¬•18˜ívº‚Äöv¢v†10‚ÄövÑ‚àû, K/Rb ‚Äöv¢v† 330. Mineralising solutions were weakly.acidic (pH ‚Äöv¢v† 5), reduced (S04‚Äöv¢v†/H2S ‚Äöv¢v† 0.001) and had a high ˜í¬£S content (0.006 molal); Gold was predominantly transported as AuHSO, although Au(HS)2 may have also been important, particularly if the pH or ˜í¬£S was higher than estimated. Gold deposition most likely occurred due to H1S loss associated with sulfidation reactions as magnetite and hematite, present in the wall rocks, were altered to pyrite. Phase separation occurring due to fluid pressure drops in dilational fault zones may have also been locally important for gold deposition. The ultimate source of gold at the TGM remains unclear. Two possibilities are suggested: i) gold was magmatically sourced, and was partitioned into an exsolved magmatic-hydrothermal fluid during magma crystallisation, or ii) gold was present as detrital gold in the contact aureole of the granite and was scavenged and remobilised by magmatic and/or contact metamorphic hydrothermal fluids. In the second scenario, Au mineralisation in the underlying metamorphic basement may have provided a source of detrital gold in the sedimentary lithologies of the Black Peak Formation

Gold deposits of the Tanami corridor

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Geological and structural controls on gold mineralization in the Tanami District, Northern Territory

Gold mineralization in the Tanami district is hosted within moderately northwest dipping turbiditic sedimentary and basaltic volcanic rocks of the Paleoproterozoic Mt. Charles Formation. The gold occurs within a complex sinistral wrench-fault array and associated veins and alteration haloes. The main mineralized faults have a northerly trend and dip steeply east. Subsidiary structures trend at 030° and 070° and dip towards the southeast. Paleostress calculations based on fault striation populations and geometry (strike and dip) of faults indicate that at the time of the mineralizing event, δ1 was sub-horizontal and SE-NW directed with δ1 subvertical. Structural studies indicate that the mineralization occurred after the regional folding event and synchronous with the emplacement of felsic dykes into the mine sequence. Gold veins in the Tanami district are interpreted to be part of an outer thermal aureole gold system that formed during the emplacement of granitoids in the nearby ∼1,815 to ∼1,799 Ma Frankenia and/or Coomarie domes. Economic gold mineralization occurred late in the paragenetic history of the district. Gold is hosted by quartz-carbonate veins within shear zones, and also in the surrounding sericite-quartz-pyrite ± carbonate-altered wallrocks. Gold-mineralized veins precipitated at depths of 3 to 6 km from high temperature (∼300°C), low salinity (∼5 wt% NaCl equivalent) fluids with low COδ2 contents. Barren quartz, dolomite and calcite veins that occur in pre- and post-mineralization thrust faults formed from high salinity (∼20 wt% NaCl equivalent), low temperature (∼120-150°C) basinal brines. Pyrite in the gold mineralized veins and alteration halos has lower δ34S values (6.8 to 12.5‰) than local diagenetic pyrite (17.8 to 19.2‰) or pyrite in pre-mineralization thrust faults (31.7 to 37.‰). The mineralizing fluids are inferred to have contained a well-homogenized mixture of magmatic and sedimentary-derived sulfur. © Springer-Verlag 2006

Vein mineralization at the Damang Gold Mine, Ghana: controls on mineralization

Two distinct styles of Au mineralization occur at the Damang Gold Mine; Palaeoproterozoic sediments of the Tarkwaian Group host both. One style of mineralization is stratabound within quartz-lithic conglomerates of the Banket Series. The second style of mineralization is associated with an extensive low-displacement, fault-fracture mesh that formed in a compressional stress regime late in the deformational history and after the peak metamorphism. Regional deformation within the Tarkwaian involved initial NW-SE directed shortening (D 1). A major NNE-trending F 1 anticline hosts the Damang orebody. Broadly N-S shortening during D 2 resulted in the formation of E-W-trending thrusts with small displacements. The D 3 shortening direction was similar to that of D 1. Steep D 1 faults were reactivated and a new set of low angle thrusts and associated flat-lying extension veins were formed. The bulk of the mineralization observed at Damang is associated with the low displacement D 3 fault fracture mesh. The presence of flat-lying extensional veins and the reactivation of some misoriented D 1 structures is indicative of periodic episodes of supralithostatic fluid pressures, low differential stress and fault-valve behavior towards the end of the deformation history. © 2004 Elsevier Ltd. All rights reserved