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the Keskarrah Formation, comprised of conglomerate and lithic sandstone; and the Itchen Formation, composed of greywacke and mudstone beds l...

Deformation

Structures produced during D1 are rarely visible in outcrop, and are inferred from changes in facing direction or from variations in bedding and cleavage relationships. These folds are tight to isoclinal with steep axial planes and subvertical plunges. Fold wavelengths vary from a few centimetres to 100 metres. The S1 axial planar cleavage is defined by an alignment of biotite and muscovite, and locally remains as small scale alignments lying between S2 surfaces. Second phase folds are t...

Plutonism

C1 to C3 plutonic events are compositionally gabbroic to granodioritic, and are coeval with volcanism. C4 and C5 plutonic rocks emplaced during D2 show a wider compositional variation, from gabbroic to granitic. C6 plutons are granitic to syenogranitic and locally pegmatitic. The C6 rocks are post D2 to early D3. Modal compositions and textural variations are used to distinguish various phases within each plutonic event. The Contwoyto Batholith, lying to the north and west of Lupin, is thoug...

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Stratigraphy

All ore zones at Lupin are confined to a continuous amphibolitic iron formation within the Contwoyto Formation which has been followed by mapping, surface and underground drilling and underground workings for a strike length in excess of 3 kilometres and a dip length of 1.2 kilometres. The main ore hosting unit is dominated by sulfide rich amphibolitic iron formation with minor interbeds of phyllite and quartzite.

Metamorphism

From surface to about 550 meters below surface the Lupin deposit lies within biotitic rocks of upper greenschist facies. Regional metamorphism accompanying early deformation is evident in the orientation of mica flakes parallel to axes of F1 folds. The early prograde metamorphism was followed by retrograde metamorphism as indicated by the alteration of biotite and hornblende to chlorite.

Structure

The first phase of isoclinal deformation developed before the peak of regional metamorphism and resulted in tight isoclinal folds with axes oriented northeast. Wavelengths are in the order of 100 metres and an axial planar foliation is locally preserved by oriented flakes of biotite and muscovite. These folds are isoclinal in the upper levels but broaden with depth, suggesting a domal structure. The second phase of isoclinal folding, developed during, or slightly prior to peak metamorphi...

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Garnet Amphibolite

Garnet amphibolite occurs as thin horizons or lenses, less than 1 metre thick and up to 30 metres long, within or at the margins of the iron formation. It may be schistose and may grade into rare pelitic rocks within the sulfide rich iron formation. Garnet content is up to 90% of the rock but averages about 20%. The garnet content in garnet amphibolite at the margins of sulfide rich and sulfide poor iron formation decreases away from the iron formation.

Sulfide Poor Iron Formation

Well laminated, sulfide poor iron formation is dominant in the East Zone and the south nose of the Centre Zone below 650 level, but is present throughout the deposit. It may grade into the sulfide rich variety and is occasionally interbedded with it. Bedding is defined by alternating grunerite, metachert and hornblende layers, and thin laminae occasionally enriched in pyrrhotite.

Sulfide Rich Iron Formation

Gold at Lupin is finely disseminated within pyrrhotite, arsenides and silicates. Arsenopyrite occurs as large prismatic crystals up to 2cm in diameter close to quartz veins which cut the iron formation. Arsenopyrite replaces amphibole, quartz, pyrrhotite and chlorite. Metacrysts commonly have loellingite cores and much of the gold associated with the arsenides occurs at the loellingite arsenopyrite boundaries. Petrographic studies have shown that pyrrhotite replaces, and is intergrown with ho...

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At Lupin, the close relationship between quartz veining, gold and sulfides has been recognized by some workers, including the authors, for several years. However, it is primarily in the poorly mineralized portions of the iron formation, or at the margins of mineralized shoots, where the vein/sulfide/gold relationships can be clearly observed. Quartz veining is found throughout the deposit, although vein densities vary. Individual vein thickness range from about 1 metre to a few millimetres.

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Variations in gold concentration at the margins of the high and low grade zones are sharp over lateral distances of 20 metres or less. All levels in the Centre and West Zones pass through two or more of these zones. On some levels, notably 170 through 330 metre levels in the Centre Zone, drifts pass through high grade zones at both ends and have a low grade section in the middle, which results in higher than average grades for these levels.

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