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Download full-text PDF. commonly 5 5 to 100 ppb Au and 10 to 200 ppm As.

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Rare organic- 5 sulfide-rich metalliferous black shales may contain up to 1 to 2 ppm Au and over 1,000 ppm As.
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In this two-stage basin-scale model, gold and arsenic are introduced early into black shale and turbidite basins during sedimentation and diagenesis stage 1 and concentrated to ore grades by later hydrothermal, structural, or magmatic processes stage 2.
In reduced ссылка на продолжение margin basin settings, organic matter, sedimented under anoxic to euxinic conditions, immobilizes and concentrates gold, arsenic, and a range of trace elements particularly V, Ni, Se, Ag, Zn, Mo, Cu, U present in marine bottom waters, into fine-grained black mudstone and siltstone of slope and basin facies.
During early diagenesis, gold and certain other trace elements Ni, Se, Te, Ag, Mo, Cu, ±PGE are preferentially partitioned into arsenian pyrite that grows in the muds.
These processes produce regionally extensive black shale and 5 sequences enriched in syngenetic gold and arsenic, commonly from 5 to 100 ppb Au and 10 to 200 ppm As.
Rare organic- and sulfide-rich metalliferous black shales may contain up to 1 to 2 ppm Au and over 1,000 ppm As, present as refractory gold in arsenian pyrite and nanoparticles of free gold.
During late diagenesis and early metamorphism stage 2 the diagenetic arsenian pyrite is recrystallized перейти form coarser grained pyrite generations, and the organic matter is cooked to bitumen.
Under higher grade metamorphism lower greenschist facies and above arsenian pyrite in carbonaceous shales is converted to pyrrhotite.
These processes release gold, arsenic, sulfur and other elements Sb, Te, Cu, Zn, Mo, Bi, Tl, and Pb from the source rocks to become concentrated by hydrothermal processes, locally to produce gold ores, in structural sites such as fold hinge zones, shear or breccia zones within or above the black shale sequence.
LA-ICP-MS analyses of diagenetic pyrite in carbonaceous sediments, both associated and not associated with gold deposits, suggests that invisible gold contents of greater than 250 ppb in diagenetic pyrite, are indicative of carbonaceous shale source rocks with the potential to produce economic gold deposits.
Application of this sedimentary source-rock model enables a systematic exploration approach for sediment-hosted gold deposits, based on the distribution, composition and structure of carbonaceous shale sequences and their contained diagenetic pyrite.
The Ertix gold belt is located on the boundary of the Kalatongke arc and the Kelan back-arc basin of D-C1.
Most scholars used to interpret the formation and distribution of the gold deposits in the Ertix tectonic belt in terms of the petrogenic and metallogenic models for active continental margins.
However, enormous data 5 isotopic dating and geologic research show that the mineralization was obviously later than the oceanic subduction, whereas exactly simultaneous with the collisional orogenesis during C2-P, especially at the transition stage from collisional compression to extension.
Based on study of metallogenic time, tectonic background, ore geology, ore fluid nature, ore material source, etc.
Accordingly, the theoretical tectonic model for collisional metallogenesis and petrogenesis is employed to explain the formation of the Ertix gold belt and to determine the gold exploration directions.
Paleomagnetic results obtained from the early Triassic Semeitau igneous series SIS yield a high-quality pole for eastern Kazakstan that is concordant with reference poles for Siberia and Europe, strongly supporting the hypothesis that Kazakstan was already joined with Eurasia at this time.
We consider this pole to be reliable.
The sampling of temporally spaced extrusives and more slowly cooled intrusives and the presence of both polarities strongly suggest that this pole averages secular variation.
This result fails to confirm hypothesized post-Permian rotation of the Siberian craton relative to its margins and provides no evidence for left-lateral motion on the east-west shear zones in which the Semeitau is located.
The similarity of ages between the SIS and the Siberian Traps supports speculation of a genetic relationship between the two.
The Giant mine is a mesothermal, greenstone-hosted gold deposit that has produced ˜250 metric tons of gold, principally from sulfide ores in altered metavolcanic rocks.
Previous нажмите чтобы узнать больше concluded that mineralizing fluids acquired metals and other ore-forming components from within the ore-hosting metavolcanic rocks and ascended a steep-dipping shear zone to the site of ore deposition.
Geochemical analyses reveal an east-dipping Na depletion zone extending from the ore zone to within the metasedimentary sequence that coincides with enrichments in Ag, As, S, and Sb and with δ180quartz values of 11.
These data indicate that wall-rock hosted gold mineralization was deposited where fluids emerging from metasedimentary rocks encountered highly reactive Ti-rich tholeiitic basalts.
From a geochemical standpoint, this ore system represents 5 metasedimentary-type gold deposit hosted in metavolcanic rocks.
A new type of gold occurrence recently discovered in the Carlin trend, north-central Nevada, is clearly distinct from classic Carlin-type gold ore.
These occurrences are interpreted to be of sedimentary exhalative sedex origin because they are stratiform and predate compaction and lithification of their unaltered Devonian host rocks.
They contain barite that exhibits δ34S and δ180 values identical to sulfate in Late Devonian seawater and sedex-type barite deposits.
Abrupt facies changes in the host rocks strongly suggest synsedimentary faulting and foundering of the carbonate shelf during mineralization, as is characteristic of sedex deposits.
Gold occurs both as native inclusions in synsedimentary base-metal sulfides and barite, and as chemical enrichments in sulfide minerals.
The absence of alteration and lack of δ13C and δ180 isotopic shift of primary carbonates in these rocks is strong evidence that this gold was not introduced with classic Carlin-type mineralization.
Collectively, these features show that the Devonian strata were significantly enriched in gold some 300 m.
These strata may have been an important, perhaps even vital, source of gold for the latter.
Although gold is typically low in most Zn-Pb-rich sedex deposits, our evidence suggests that transport of gold in basinal fluids, and its subsequent deposition in the sedex environment, can be significant.
Sediment-hosted disseminated gold deposits in NW Sichuan China have many features in common with the well-known Carlin-type deposits in the western United States.
They are hosted by Middle—Upper Triassic turbidites composed of 1300—4300 m of rhythmically interbedded, slightly metamorphosed calcareous sandstone, siltstone, and slate.
The ore bodies are typically layer- or lens-like in shape and generally extend parallel 5 the stratification of the host sedimentary rocks, with a strike length of tens to several hundreds of meters.
The immediate host rocks consist mainly of calcareous slate and siltstone characterized by high contents of organic matter and diagenetic pyrite.
The main primary ore minerals associated with gold mineralization include pyrite, arsenopyrite, realgar, and stibnite.
Gangue minerals comprise mostly Пленка для ламинирования пакетная ProfiOffice, 154 х 216 мм, 150 мкм, глянцевая, 100 шт.

(profioffic, calcite and dolomite.
Gold is extremely fine-grained, usually less than 1 μm, and cannot be seen with an 5 microscope.
In western Victoria, a widespread stratiform style of gold enrichment in 5 black mudstone and chert—clearly different from the classic mesothermal quartz vein deposits of the Victorian goldfields—has been confirmed by whole-rock geochemistry and Laser Ablation Inductively Coupled Plasma Mass Spectrometry LA-ICPMS.
This enrichment pre-dates compaction, deformation and low-grade metamorphism of the sedimentary host-rocks, and therefore possibly developed diagenetically during slow deposition of the thin carbonaceous black mudstone beds and the thinner layers of chert.
These paired strata have been documented at many locations in three regional outcrop areas of chevron-folded Cambrian and Lower Ordovician metasediments in the Stawell and Bendigo Zones, where they are interbedded по этому сообщению quartz-rich turbidites.
Gold is present in euhedral pyrite crystals in both black shale and chert.
LA-ICPMS analysis of individual pyrite crystals in the indicator beds shows that pyrite is enriched in Au, As, Sb, Se, Te and Bi.
The Au content of pyrite varies from 0.
Many pyrite crystals show enrichment of gold in their cores and depletion in their rims, confirming the likely syngenetic or syndiagenetic accumulation of gold during pyrite formation in the sediments.
Prior to regional metamorphism, folding and faulting, the many indicator strata in the outcrop areas were parts of an extensive marine sequence of Late Cambrian and Early Ordovician age.
The former primary source of this mineralisation is considered to have been one or more contemporaneously exhalative submarine hydrothermal systems.
Thus, the older Palaeozoic sediments of the western Lachlan Fold Belt were significantly enriched in syngenetic gold in the Early Palaeozoic, at least 40 million years before emplacement of the quartz — gold vein deposits of the goldfields.
We report results of metallogenic, structural, petrological, and fluid-inclusion studies that characterise the nature of gold mineralisation in the Amanda Bel Goldfield, the most significant gold producer in the Palaeozoic Broken River Province of northeastern Queensland, Australia.
Gold—antimony—arsenic and gold—arsenic deposits in the Amanda Bel Goldfield occur along distinctive northeastern trends, suggesting a strong structural control for their development during several phases of deformation in the Devonian to Carboniferous.
Field evidence, as well as petrographic, scanning electron microscope and fluid-inclusion analysis of mineralised samples, indicate the presence of two main stages of gold genesis.
These are distinguished by the coarse grained versus invisible nature of gold particles and their association with particular sulfide phases.
A third stage of gold deposition is attributed to источник статьи of antimony±gold-rich ore fluids.
Fluid-inclusion studies record minimum trapping temperatures between 140 and 380°C, and salinities of up to 6.
Our analyses further indicate that mineralising solutions for the earlier of the two main gold-forming stages were slightly more saline, and that the ore-hosting veins formed at higher temperatures.
The style of gold mineralisation in the Amanda Bel Goldfield is compatible with orogenic gold deposits that form primarily during compressional and transpressional deformation along convergent plate margins in accretionary and collisional orogens.
The increased understanding gained from our studies on the origin and nature of the deposits aids predictive mineral discovery elsewhere in the Broken River Province, and also in analogous terranes throughout the Tasman Fold Belt System of eastern Australia.
The late Paleozoic-early Mesozoic tectonic evolution of Xinjiang Autonomous Region, northwestern China provided a favorable geological 5 for the formation of lode gold deposits along the sutures between a number of the major Eastern Asia cratonic blocks.
These sutures are now represented by the Altay Shan, Tian Shan, and Kunlun Shan ranges, with the former two separated by the Junggar basin and the latter two by the immense Tarim basin.
In northernmost Xinjiang, final growth of the Altaid orogen, southward from the Angara craton, is now recorded in the remote mid- to late Paleozoic Altay Shan.
Accreted Early to Middle Devonian oceanic rock sequences contain typically small, precious-metal bearing Fe-Cu-Zn VMS deposits e.
Orogenic gold deposits are widespread along the major Irtysh e.
Duyolanasayi, Saidi, Taerde, Kabenbulake, Akexike, Shaerbulake and Tuergen-Hongshanzui e.
Hongshanzui fault systems, as well as in structurally displaced terrane slivers of the western Junggar e.
Hatu and eastern Junggar areas.
Geological and geochronological constraints indicate a generally Late Carboniferous to Early Permian episode of gold deposition, which was coeval with the final stages of Altaid magmatism and large-scale, right-lateral translation along older terrane-bounding faults.
The Tian Shan, an exceptionally gold-rich mountain range to the west in the Central Asian republics, is only beginning to be recognized for its gold potential in Xinjiang.
The more significant resulting deposits in the terranes of the southern Tian Shan include the Sawayaerdun orogenic deposit along the Kyrgyzstan border and the epithermal and replacement deposits of the Kanggurtag belt to the east in the Chol Tagh range.
Gold-rich porphyry copper deposits e.
Tuwu define important new exploration targets in the northern Tian Shan of Xinjiang.
The northern foothills of the Kunlun Shan of southern Xinjiang host scattered, small placer gold deposits.
Sources for the gold have not been identified, but are hypothesized to be orogenic gold veins beneath the icefields to the south.
They are predicted to по этой ссылке formed in the Tianshuihai terrane during its early Mesozoic accretion to the amalgamated Tarim-Qaidam-Kunlun cratonic block.
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Mineralization is controlled by the NE-trending Suzdal Fault.
In the north, the deposit borders on the Early Triassic Semeytau volcanic-plutonic structure.
Mineralization is superposed on the Late Paleozoic complex of metadolerite and quartz porphyry dikes.
Ore deposition was a long-term process comprising four stages.
The first stage was related https://megapixels.ru/100/plenki-zagotovki-dlya-laminirovaniyaya-brauberg-komplekt-100-sht-dlya-formata-a6-100-mkm-531785.html deposition of slightly auriferous pyrite syngenetic to host rocks.
The second stage is characterized by formation of the first productive with invisible gold fine-acicular arsenopyrite mineralization accompanied by sericitization and localized in the tectonic zone.
The stockwork ore with pocket-disseminated base-metal mineralization and free microscopic gold of the third stage is hosted in silicified rocks.
The ore formation has been completed by quartz-stibnite veins superposed on all preceding types of mineralization.
The deposit is an example of polygenetic and multistage mineralization.
In Eastern Kazakhstan, Sb mineralization is the most widespread in the Irtysh and Bakyrchik ore districts of the West Kalba gold-bearing belt.
It is spatially related to disseminated gold-sulfide ores at some deposits and is structurally and spatially isolated at others.
Disseminated gold-sulfide mineralization is localized in Carboniferous carbonaceous-terrigenous carbonate rocks.
It is marked off by zones of dynamic metamorphism and foliation and is characterized by the ribbon-like-lenticular morphology of ore deposits.
In combination with gold-sulfide ores, Sb mineralization is more diverse.
Also, Sb-containing minerals such as arsenopyrite and pyrite are observed.
Two temperature regimes of mineralization are established here: 418-300 °C for gold-polysulfide mineralization and 280-200 °C for later Sb mineralization.
No visible gold is found in the antimonite of the quartz-antimonite veins, 5 atomic-absorption analysis reveals few ppm or more gold.
The late antimonite stage of mineralization is separated from the gold-polysulfide stage by 7 Myr long intramineralization tectonic shifts.

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