A copper mine operated intermittently in the 1840s and re-opened for a short time in 1876.
Bull (1920): provided the following description:
"The Carlisle copper mine was located on what is now (1920) known as the Captain Wilson estate and the Edward J. Carr estate, in the southerly part of the town, about a mile from the center. Henry N. Hooper & Company of Boston, church bell founders, were in charge of the work, which was carried on intermittently for a period of ten years from 1840. Major B. F. Heald, late of Carlisle, lived near the property, and was general superintendent during the entire period. A shaft was sunk to the depth of about two hundred and twenty feet, being the same depth as the height of Bunker Hill Monument in Charlestown. The ore was hauled to Boston for smelting by ox teams, which proved so expensive that Hooper & Company who were the leading church bell founders and casters in the country at that time, decided to erect a smelter of their own on the property; but as the fumes from the smelter would injure vegetation, it became necessary for the company to purchase the adjoining farms in order to relieve them from the liability of paying damages. This they were unable to do, because of the excessive price charged by the owners of the land, and the idea was abandoned.
Quite a little village sprang up in connection with the mining operations. There were four miners' dwellings, a shaft house, blacksmith shop, cookhouse, barn, and other buildings. One Abel Hodgman had a store on the Carr estate, near the road. The result of working the mine was fairly satisfactory, and probably furnished the company with the copper used in connection with their bell founding, and possibly more, but the industry was abandoned in 1849 upon the discovery of the Lake Superior copper mines in Michigan."
Regions containing this locality
|North America Plate||Tectonic Plate|
Select Mineral List TypeStandard Detailed Strunz Dana Chemical Elements
Commodity ListThis is a list of exploitable or exploited mineral commodities recorded at this locality.
3 valid minerals.
Detailed Mineral List:
| ⓘ Chalcocite|
Reference: Engineering & Mining Journal 22:57 (July 22, 1876)
| ⓘ Copper|
Reference: Bull, Sidney A. - History of the town of Carlisle, Massachusets, 1754-1920
| ⓘ Tenorite ?|
Reference: Engineering & Mining Journal 22:57 (July 22, 1876)
List of minerals arranged by Strunz 10th Edition classification
|Group 1 - Elements|
|Group 2 - Sulphides and Sulfosalts|
|Group 4 - Oxides and Hydroxides|
List of minerals arranged by Dana 8th Edition classification
|Group 1 - NATIVE ELEMENTS AND ALLOYS|
|Metals, other than the Platinum Group|
|Group 2 - SULFIDES|
|AmBnXp, with (m+n):p = 2:1|
|Group 4 - SIMPLE OXIDES|
List of minerals for each chemical element
This geological map and associated information on rock units at or nearby to the coordinates given for this locality is based on relatively small scale geological maps provided by various national Geological Surveys. This does not necessarily represent the complete geology at this locality but it gives a background for the region in which it is found.
Click on geological units on the map for more information. Click here to view full-screen map on Macrostrat.org
|Devonian - Silurian|
358.9 - 443.8 Ma
|Paleozoic sedimentary and volcanic rocks|
Age: Paleozoic (358.9 - 443.8 Ma)
Reference: Chorlton, L.B. Generalized geology of the world: bedrock domains and major faults in GIS format: a small-scale world geology map with an extended geological attribute database. doi: 10.4095/223767. Geological Survey of Canada, Open File 5529. 
|Ordovician - Neoproterozoic|
443.8 - 1000 Ma
Stratigraphic Name: Nashoba Formation
Description: Sillimanite schist and gneiss, partly sulfidic, amphibolite, biotite gneiss, calc-silicate gneiss and marble. Nashoba Formation occurs in Nashoba zone of eastern MA. Consists of interlayered sillimanite-bearing, partly sulfidic schist and gneiss, calc-silicate gneiss, and subordinate quartzite and marble. Protoliths were probably volcanogenic sediments interlayered with limy marine sediments. Bell and Alvord (1976) divided Nashoba into 10 members on basis of lithology. Amphibolite is most abundant near presumed base, namely in Boxford Member. Skehan and Abu-Moustafa (1976) divided Nashoba into 30 members based on section in Wachusett-Marlborough tunnel. Although Bell and Alvord's and Skehan and Moustafa's sections contain similar lithologies, Bell and Alvord's is much thicker, and Boxford Member is not readily identified in Skehan and Abu-Moustafa's. Subdivision of Nashoba is conjectural south of Marlborough and Shrewsbury. On MA State bedrock map (Zen and others, 1983) only Boxford Member is separated out from the rest of the Nashoba because this unit was the only member clearly recognized in several area. A definite sequence of members probably does not exist anywhere in the Nashoba because of lenticularity of assemblages and repeated rock types, both of which could be accounted for by either sedimentary or tectonic processes. Although Castle (1965) considered Fish Brook to be either a premetamorphic intrusive rock or a core gneiss of intrusive or sedimentary ancestry, Bell and Alvord (1976) considered it to be volcanic or volcaniclastic in origin. Zircons in Fish Brook are certainly volcanic in origin and yield a date of 730 +/-26 Ma (Olszewski, 1980). If the rock were a core gneiss, that date would apply only to the Fish Brook and not to surrounding rocks; but, Bell and Alvord (1976) believe Fish Brook to be part of the Marlboro Formation-Nashoba Formation sequence and therefore the date does apply to the sequence. In addition, a 1500 Ma date for Shawsheen Gneiss [reference not given] helps bracket age of Marlboro-Nashoba sequence. An upper limit for the sequence was established from the 430 +/-5 Ma age of intruding Sharpers Pond Diorite and 450 +/-23 Ma age of the intruding Andover Granite (Zartman and Naylor, 1984). Although age on MA State bedrock map is shown as Proterozoic Z or Ordovician (due to uncertainty regarding actual rocks sampled by Olszewski and a strong belief that rocks of Nashoba zone correlated with Ordovician rocks to the west), author now feels that rocks of Nashoba zone (except for Tadmuck Brook Schist) are all Proterozoic, but that they are unlike the Proterozoic rocks of neighboring Milford-Dedham zone. [no formal age change made in this report] (Goldsmith, 1991).
Comments: Part of Nashoba Zone (Silurian and Older Rocks). Secondary unit description per MA017. Age debated. MA017 = Although age on MA State bedrock map is shown as Proterozoic Z or Ordovician (due to uncertainty regarding actual rocks sampled by Olszewski and a strong belief that rocks of Nashoba zone correlated with Ordovician rocks to the west), author now feels that rocks of Nashoba zone (except for Tadmuck Brook Schist) are all Proterozoic, but that they are unlike the Proterozoic rocks of neighboring Milford-Dedham zone (Goldsmith, 1991). MA018 = Fish Brook Gneiss of the Nashoba terrane has been dated by G.R. Dunning at 520+14-11 Ma. This not only establishes a Cambrian age for this unit, but constrains the age of the overlying Marlboro and Nashoba Formations to the interval between 520 Ma and 430 Ma, the age of the cross-cutting Sharpners Pond Diorite. No Precambrian rocks, therefore, are known from the Nashoba terrane (Hepburn and others, 1993). MA019 = Fish Brook Gneiss has yielded a Cambrian to Ordovician U/Pb abraded zircon crystallization age of 499+/-6/-3 Ma. This date constrains the age of the metavolcanic and metasedimentary rocks of the Nashoba terrane to the interval between Late Cambrian and Early Silurian (Hepburn and others, 1994). Original map source: Unpublished Digital Geologic Map of Massachusetts received from Rudi Hon of Boston College in 1998; based on the 1983 USGS paper version (MA002).
Reference: Horton, J.D., C.A. San Juan, and D.B. Stoeser. The State Geologic Map Compilation (SGMC) geodatabase of the conterminous United States. doi: 10.3133/ds1052. U.S. Geological Survey Data Series 1052.