#7 Ghost Camp Found, 1900-1949 in BC's Boundary Country.
74 هزار بار بازدید -
14 سال پیش
-
http://BcGHOSTtowns.com
This is not "The City of Paris Ghost Town" It is in fact the #7 mine site and is one of nicest little abandoned mine camps found in it's normal state of decay...
Here is the MINEFILE info for the #7
The No. 7 mine is on the claim of the same name (Lot 623), on a ridge crest at the elevation of 1370 metres, 3.3 kilometres east of the confluence of McCarren and Gidon creeks, 7.5 kilometres southeast of Greenwood. Access to the property is 2.4 kilometres travelling southerly and up hill by winding dirt road from the McCarren Creek road. The Lexington (082ESE041) and City of Paris (082ESE042) lie 2.5 kilometres to the southeast.
The intermittent operations of the No. 7 mine from 1901 to 1945 produced a total of 13,748 tonnes of ore yielding 92.4 kilograms of gold, 3110 kilograms of silver, 97 tonnes of lead, and 6.2 tonnes of zinc.
The potential of No. 7 was recognized early in the Greenwood camp and the claim was Crown granted in 1895 to J. Schofield. By 1897, a 40-metre deep inclined shaft was developed on the claim to service 60 metres of underground drifting. At the approximate time of final closing of the mine 50 years later, in 1945, the mine workings comprised a 100-metre inclined shaft, adit levels at 12 and 90 metres, and intermediate levels at 30 and 55 metres. Old mine maps show that the underground work on these four levels totals about 1580 metres. The 90-metre adit level is open from portal to face, a distance of about 580 metres, but the other levels are partly caved southeast of the inclined shaft. Other workings include an adit drift 40 metres northwest of the 12-metre No. 1 adit, a large number of surface pits, and a deep trench along the vein from which some underhand stoping was done.
The mine is developed on a quartz vein on a major southeasterly trending boundary fault between Upper Paleozoic Knob Hill Group on the northeast and Attwood Group on the southwest. Contained in part within the fault zone, and hosting this vein, are a schistose quartz feldspar intrusion and serpentinite. A variety of young Tertiary dikes have invaded, and are superimposed on, the vein structure.
The quartz vein at the mine site has been traced for a strike length of more than 300 metres. The vein ranges from 10 centimetres to 1.5 metres wide and dips 40 to 65 degrees northeast, having dike rocks or chloritic schists of the Knob Hill Group on the hanging wall and highly sheared talc-carbonate rocks of the serpentinite body on the footwall.
Mineralization consists of pyrite, sphalerite and some galena dispersed in blue-grey quartz along the central portion of the vein. The most productive part of the vein was southeast of the inclined shaft above the 55-metre level.
A large number of northeasterly striking faults displace the vein. Displacements along these faults range from a few feet to almost 60 metres. The maximum displacement was measured on the fault exposed in the southeast end of the 90-metre level and on the surface 60 metres southeast of the long open cut. The vein has not been located beyond this fault. Movement along these faults has been largely post mineral. Evidence of some pre-mineral movement is furnished by unbroken vein quartz seams and lenses, up to 20 centimetres by 3 metres, in the fault zone exposed at the southeast end of the 90-metre level. Subsidiary faults of small displacement are part of this same fault zone, and offset both vein and the post mineral quartz trachyte dike. Thus this single fault zone has been the locus of both pre- and post-mineral movements.
The No. 7 fault zone is an ancient structure believed to be a possible continuation of the Chesaw thrust in Washington state. The serpentinite is part of a disrupted Paleozoic ophiolite complex. Because of the ductile nature of these rocks, the belt has become a tectonically active zone and the locus of much shearing, thrusting, igneous intrusion and vein mineralization. The common Mg-Fe carbonate (listwanite) alteration and serpentinization are believed to be related to major thrusting of the ophiolitic rocks during the Jurassic. In the early Tertiary these thrusts were re-activated by a tectonic compression directed subparallel to the developing northerly elongated graben structures. Igneous activity at the same time is believed to be related to numerous vein deposits.
No ore reserve estimate is available for this property.
Cool stuff! I would like to take some pictures of the old cabins. Thanks for sharing!
Thanks to a local resident for help and directions Check back next summer for a video on what is left of the City of Paris BC.
Thanks again to David, Snuffy & Jim
British Columbia Historian
John Mitchell
This is not "The City of Paris Ghost Town" It is in fact the #7 mine site and is one of nicest little abandoned mine camps found in it's normal state of decay...
Here is the MINEFILE info for the #7
The No. 7 mine is on the claim of the same name (Lot 623), on a ridge crest at the elevation of 1370 metres, 3.3 kilometres east of the confluence of McCarren and Gidon creeks, 7.5 kilometres southeast of Greenwood. Access to the property is 2.4 kilometres travelling southerly and up hill by winding dirt road from the McCarren Creek road. The Lexington (082ESE041) and City of Paris (082ESE042) lie 2.5 kilometres to the southeast.
The intermittent operations of the No. 7 mine from 1901 to 1945 produced a total of 13,748 tonnes of ore yielding 92.4 kilograms of gold, 3110 kilograms of silver, 97 tonnes of lead, and 6.2 tonnes of zinc.
The potential of No. 7 was recognized early in the Greenwood camp and the claim was Crown granted in 1895 to J. Schofield. By 1897, a 40-metre deep inclined shaft was developed on the claim to service 60 metres of underground drifting. At the approximate time of final closing of the mine 50 years later, in 1945, the mine workings comprised a 100-metre inclined shaft, adit levels at 12 and 90 metres, and intermediate levels at 30 and 55 metres. Old mine maps show that the underground work on these four levels totals about 1580 metres. The 90-metre adit level is open from portal to face, a distance of about 580 metres, but the other levels are partly caved southeast of the inclined shaft. Other workings include an adit drift 40 metres northwest of the 12-metre No. 1 adit, a large number of surface pits, and a deep trench along the vein from which some underhand stoping was done.
The mine is developed on a quartz vein on a major southeasterly trending boundary fault between Upper Paleozoic Knob Hill Group on the northeast and Attwood Group on the southwest. Contained in part within the fault zone, and hosting this vein, are a schistose quartz feldspar intrusion and serpentinite. A variety of young Tertiary dikes have invaded, and are superimposed on, the vein structure.
The quartz vein at the mine site has been traced for a strike length of more than 300 metres. The vein ranges from 10 centimetres to 1.5 metres wide and dips 40 to 65 degrees northeast, having dike rocks or chloritic schists of the Knob Hill Group on the hanging wall and highly sheared talc-carbonate rocks of the serpentinite body on the footwall.
Mineralization consists of pyrite, sphalerite and some galena dispersed in blue-grey quartz along the central portion of the vein. The most productive part of the vein was southeast of the inclined shaft above the 55-metre level.
A large number of northeasterly striking faults displace the vein. Displacements along these faults range from a few feet to almost 60 metres. The maximum displacement was measured on the fault exposed in the southeast end of the 90-metre level and on the surface 60 metres southeast of the long open cut. The vein has not been located beyond this fault. Movement along these faults has been largely post mineral. Evidence of some pre-mineral movement is furnished by unbroken vein quartz seams and lenses, up to 20 centimetres by 3 metres, in the fault zone exposed at the southeast end of the 90-metre level. Subsidiary faults of small displacement are part of this same fault zone, and offset both vein and the post mineral quartz trachyte dike. Thus this single fault zone has been the locus of both pre- and post-mineral movements.
The No. 7 fault zone is an ancient structure believed to be a possible continuation of the Chesaw thrust in Washington state. The serpentinite is part of a disrupted Paleozoic ophiolite complex. Because of the ductile nature of these rocks, the belt has become a tectonically active zone and the locus of much shearing, thrusting, igneous intrusion and vein mineralization. The common Mg-Fe carbonate (listwanite) alteration and serpentinization are believed to be related to major thrusting of the ophiolitic rocks during the Jurassic. In the early Tertiary these thrusts were re-activated by a tectonic compression directed subparallel to the developing northerly elongated graben structures. Igneous activity at the same time is believed to be related to numerous vein deposits.
No ore reserve estimate is available for this property.
Cool stuff! I would like to take some pictures of the old cabins. Thanks for sharing!
Thanks to a local resident for help and directions Check back next summer for a video on what is left of the City of Paris BC.
Thanks again to David, Snuffy & Jim
British Columbia Historian
John Mitchell
14 سال پیش
در تاریخ 1389/02/31 منتشر شده
است.
74,020
بـار بازدید شده