Cincinnati vein system, Mahoney Mines area, Tres Hermanas Mining District, Tres Hermanas Mountains, Luna County, New Mexico, USAi
| Regional Level Types | |
|---|---|
| Cincinnati vein system | - not defined - |
| Mahoney Mines area | Area |
| Tres Hermanas Mining District | Mining District |
| Tres Hermanas Mountains | Mountain Range |
| Luna County | Shaft (Reclaimed) |
| New Mexico | State |
| USA | Country |
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Latitude & Longitude (WGS84):
31° 55' 51'' North , 107° 45' 31'' West (est.)
Estimate based on other nearby localities or region boundaries.
Margin of Error:
~0km
Köppen climate type:
Location and access: The Cincinnati vein system is composed of a group of several individual veins located approximately 1½ miles south of the Mahoney mining area. Starting at the windmill near the Mahoney mines, the general area can be reached by traveling either of two roads leading to the south.
History: Several individual mines are located along the Cincinnati vein system. From east to west, the principal ones are the Marie, Cincinnati, Hancock, and Black Hawk mines. The Cincinnati and Hancock are probably the largest, to judge from the size of the present dumps.
Factual information is lacking concerning the early development of the mines. Lindgren (1909) examined the area briefly in 1905. Up to that time, the Golden Cross & Eagle Co. is said to have produced $100,000 (period values) in lead and gold from the Cincinnati mine. Lindgren also reported that the Hancock mine had been developed to a depth of 400 feet by a shaft, and that 1,000 tons of rich lead ore, with some gold, had been produced.
Since 1915 occasional shipments have been recorded from the mines, but the total of these later shipments probably has not been more than 1,000 tons. A reasonable estimate of the total value of the production from all the mines along the vein system since discovery is about $200,000. At the time of the writer's visit to the area (July 1959), most of the claims in the area were owned by, or under lease to, the Western Minerals Co., W. A. White, general manager. This company had reopened the Black Hawk shaft to a depth of 65 feet, and sampled the vein at that level. The company was also contemplating exploring the Cincinnati mine at depth by diamond drilling.
Geology: The Cincinnati vein system extends in a N. 75° E. direction from the ridge of Lower Cretaceous sediments across the early latite breccias and flows, thence through a small outcrop of altered Paleozoic rocks, and finally into the main Tres Hermanas quartz monzonite stock. The total strike length of the system is over 10,000 feet.
The system is not one strong vein that is readily traceable. Instead it is a series of short, disconnected veins that have the same general alinement. The average strike of the veins is N. 75° E., but the dip varies from 75°-80° S. in the western part to 65°-80° N. in the eastern part of the vein system. The veins at the Black Hawk, Cincinnati, and Marie mines are aligned, but the Hancock vein is offset some 500 feet to the south. The position of the Hancock vein could be explained by crossfaulting, or simply as a parallel vein to the main system. Direct evidence for either hypothesis is lacking.
Evidence that the vein system lies along a fault of at least moderate displacement is clearly shown near the Cincinnati mine. A latite porphyry dike striking N. 25° W. with nearly vertical dip is abruptly terminated on the north side of the vein. The extension of the dike was not found on the south side of the vein even though bedrock is fairly well exposed for 500 or more feet on either side of the aforementioned dike outcrop.
At the Marie mine, the contact between the quartz monzonite and the Paleozoic sediments appears to have been displaced in such a manner as to indicate a left lateral movement of about 300 feet. Also, there is a radical change in dip of the sediments across the vein; on the north side the sediments dip 30° to 48° NE., whereas on the south side the dip is 45° SW. At first glance, one might assume a rotation of 90 degrees on the vein fault. The writer hardly believes this to be the case; instead the sediments were probably highly contorted by the intrusion of the quartz monzonite stock prior to the formation of the fault. Certainly some rotation is possible, but not of the magnitude indicated solely by the attitude of the sediments.
The veins are generally very narrow, 4 feet being about the widest observed width. Generally the vein is composed of numerous closely spaced veinlets instead of one main zone. Galena, sphalerite, and pyrite are the principal sulfides, accompanied by considerable quartz and calcite. Gold and silver are reported to be present in the veins, but the forms in which these metals occur is not known. Minor argillic alteration extends several inches to several feet outward from the vein into the wall rock.
The surface outcrops of the veins are highly oxidized, and only sparse sulfide minerals are found. In the oxidation zone the usual assemblage of oxidized lead and zinc minerals is present, accompanied by considerable limonite and manganese oxide. The depth to the present water table in the vicinity of the mines is not known; water, however, is not known to exist in the Hancock mine, which is said to be 400 feet deep. The water level in the well southeast of the Marie mine is reported to be 560 feet below the surface.
The veins appear to be best developed in the latite flows and breccia. The veins are fairly well developed in the quartz monzonite, but the system is very weak, if indeed not absent, in the Paleozoic limestones. This may be attributed to the physical nature of the rocks during faulting and fracturing. The latite and quartz monzonite formed strong fractures, which were permeable to the ore-bearing solutions, whereas the fractures in the limestone may have been rehealed, thus causing that rock type to be relatively impermeable. Another and perhaps supplementary reason for the veins' being stronger in the igneous rocks is that they were nonreactive to the ore solutions; therefore, simple but regular fissure veins were formed. The limestone, on the other hand, being very reactive may have tended to form isolated and, as yet, hidden replacement deposits along the fault plane.
The structural features of the Cincinnati vein system enable the age of the vein mineralization relative to the other geologic events to be determined. The following facts are evident: (1) The vein is younger than the quartz-monzonite stock, which in turn is younger than the early latite sequence. (2) The latite porphyry dike near the Cincinnati mine is older than the vein, for it is truncated by the vein structure. This fact could be explained by post-ore faulting along the vein, but such major movement is not evident. (3) A northeast-striking basic dike, located between the Hancock and Black Hawk mines, appears to cut across the vein system without being displaced. Unfortunately, the outcrops of this dike are somewhat obscured in the vicinity of the vein, and the assumption that the dike is post-ore must be considered as probable but not conclusive.
From the evidence above, it is deduced that the ore deposition took place after the invasion of the Tres Hermanas quartz monzonite stock, but prior to the invasion of the basic dikes. Furthermore, the deposition probably took place immediately following the intrusion of the latite dikes. Unfortunately, the age relationship between the later latite volcanic sequence and ore deposition is not known; it would be plausible to assume them to be nearly contemporaneous.
The two northwest-striking faults on each side of the ridge composed of Lower Cretaceous sediments are believed to be much later than the faulting that localized the Cincinnati vein system; the vein system fault is not evident anywhere on the ridge, and the two fault scarps bounding the ridge are fairly sharp, indicative of a young age.
It is tempting to correlate the age of all the ore mineralization in the Tres Hermanas district with the same period as that of the Cincinnati vein system. Direct evidence for the assumption is lacking, however, and certainly some of the mineralization of the district (viz., the pyrometasomatic iron deposits) is believed to be contemporaneous with the em-placement of the quartz monzonite stock. The writer believes, however, that practically all the ore mineralization of the district originated from deep-seated differentiation products of the quartz monzonite stock. The ore solutions formed from this stock were then released over several different periods, ranging from the time of the emplacement of the stock to the period when the basic dikes were emplaced.
Mining and milling methods: To the writer's knowledge, the ores from the various mines along the Cincinnati vein system were never milled, being only hand sorted and then shipped directly to the smelter. The discussion, therefore, will be limited to the method of mining the veins.
The veins have been developed by numerous shafts, pits, and trenches throughout their known strike lengths. The following shaft depths arc reported: Black Hawk mine, 65-foot inclined shaft; Hancock mine, 400-foot inclined shaft; Cincinnati mine, one vertical shaft, 300 feet deep, and another vertical shaft of unknown depth; Marie mine, one shaft at least 50 feet deep at the east end of the vein.
At present (1961), only the Black Hawk shaft is accessible. Rotten timber in the other shafts prevented the writer from examining them; therefore, the shaft depths reported above for three of the mines could not be verified. Near the surface, the veins were mined by simple trenching methods, small windlasses being used to hoist the ore from the trenches. Stoping from the shaft probably was from levels placed at about 50-foot intervals, the operation involving a combination of shrinkage and over-hand-with-stulls stoping methods. Many of the stopes that connected to the surface are still accessible; their walls have stood fairly well, even though some of these openings are 50 or more years old.
History: Several individual mines are located along the Cincinnati vein system. From east to west, the principal ones are the Marie, Cincinnati, Hancock, and Black Hawk mines. The Cincinnati and Hancock are probably the largest, to judge from the size of the present dumps.
Factual information is lacking concerning the early development of the mines. Lindgren (1909) examined the area briefly in 1905. Up to that time, the Golden Cross & Eagle Co. is said to have produced $100,000 (period values) in lead and gold from the Cincinnati mine. Lindgren also reported that the Hancock mine had been developed to a depth of 400 feet by a shaft, and that 1,000 tons of rich lead ore, with some gold, had been produced.
Since 1915 occasional shipments have been recorded from the mines, but the total of these later shipments probably has not been more than 1,000 tons. A reasonable estimate of the total value of the production from all the mines along the vein system since discovery is about $200,000. At the time of the writer's visit to the area (July 1959), most of the claims in the area were owned by, or under lease to, the Western Minerals Co., W. A. White, general manager. This company had reopened the Black Hawk shaft to a depth of 65 feet, and sampled the vein at that level. The company was also contemplating exploring the Cincinnati mine at depth by diamond drilling.
Geology: The Cincinnati vein system extends in a N. 75° E. direction from the ridge of Lower Cretaceous sediments across the early latite breccias and flows, thence through a small outcrop of altered Paleozoic rocks, and finally into the main Tres Hermanas quartz monzonite stock. The total strike length of the system is over 10,000 feet.
The system is not one strong vein that is readily traceable. Instead it is a series of short, disconnected veins that have the same general alinement. The average strike of the veins is N. 75° E., but the dip varies from 75°-80° S. in the western part to 65°-80° N. in the eastern part of the vein system. The veins at the Black Hawk, Cincinnati, and Marie mines are aligned, but the Hancock vein is offset some 500 feet to the south. The position of the Hancock vein could be explained by crossfaulting, or simply as a parallel vein to the main system. Direct evidence for either hypothesis is lacking.
Evidence that the vein system lies along a fault of at least moderate displacement is clearly shown near the Cincinnati mine. A latite porphyry dike striking N. 25° W. with nearly vertical dip is abruptly terminated on the north side of the vein. The extension of the dike was not found on the south side of the vein even though bedrock is fairly well exposed for 500 or more feet on either side of the aforementioned dike outcrop.
At the Marie mine, the contact between the quartz monzonite and the Paleozoic sediments appears to have been displaced in such a manner as to indicate a left lateral movement of about 300 feet. Also, there is a radical change in dip of the sediments across the vein; on the north side the sediments dip 30° to 48° NE., whereas on the south side the dip is 45° SW. At first glance, one might assume a rotation of 90 degrees on the vein fault. The writer hardly believes this to be the case; instead the sediments were probably highly contorted by the intrusion of the quartz monzonite stock prior to the formation of the fault. Certainly some rotation is possible, but not of the magnitude indicated solely by the attitude of the sediments.
The veins are generally very narrow, 4 feet being about the widest observed width. Generally the vein is composed of numerous closely spaced veinlets instead of one main zone. Galena, sphalerite, and pyrite are the principal sulfides, accompanied by considerable quartz and calcite. Gold and silver are reported to be present in the veins, but the forms in which these metals occur is not known. Minor argillic alteration extends several inches to several feet outward from the vein into the wall rock.
The surface outcrops of the veins are highly oxidized, and only sparse sulfide minerals are found. In the oxidation zone the usual assemblage of oxidized lead and zinc minerals is present, accompanied by considerable limonite and manganese oxide. The depth to the present water table in the vicinity of the mines is not known; water, however, is not known to exist in the Hancock mine, which is said to be 400 feet deep. The water level in the well southeast of the Marie mine is reported to be 560 feet below the surface.
The veins appear to be best developed in the latite flows and breccia. The veins are fairly well developed in the quartz monzonite, but the system is very weak, if indeed not absent, in the Paleozoic limestones. This may be attributed to the physical nature of the rocks during faulting and fracturing. The latite and quartz monzonite formed strong fractures, which were permeable to the ore-bearing solutions, whereas the fractures in the limestone may have been rehealed, thus causing that rock type to be relatively impermeable. Another and perhaps supplementary reason for the veins' being stronger in the igneous rocks is that they were nonreactive to the ore solutions; therefore, simple but regular fissure veins were formed. The limestone, on the other hand, being very reactive may have tended to form isolated and, as yet, hidden replacement deposits along the fault plane.
The structural features of the Cincinnati vein system enable the age of the vein mineralization relative to the other geologic events to be determined. The following facts are evident: (1) The vein is younger than the quartz-monzonite stock, which in turn is younger than the early latite sequence. (2) The latite porphyry dike near the Cincinnati mine is older than the vein, for it is truncated by the vein structure. This fact could be explained by post-ore faulting along the vein, but such major movement is not evident. (3) A northeast-striking basic dike, located between the Hancock and Black Hawk mines, appears to cut across the vein system without being displaced. Unfortunately, the outcrops of this dike are somewhat obscured in the vicinity of the vein, and the assumption that the dike is post-ore must be considered as probable but not conclusive.
From the evidence above, it is deduced that the ore deposition took place after the invasion of the Tres Hermanas quartz monzonite stock, but prior to the invasion of the basic dikes. Furthermore, the deposition probably took place immediately following the intrusion of the latite dikes. Unfortunately, the age relationship between the later latite volcanic sequence and ore deposition is not known; it would be plausible to assume them to be nearly contemporaneous.
The two northwest-striking faults on each side of the ridge composed of Lower Cretaceous sediments are believed to be much later than the faulting that localized the Cincinnati vein system; the vein system fault is not evident anywhere on the ridge, and the two fault scarps bounding the ridge are fairly sharp, indicative of a young age.
It is tempting to correlate the age of all the ore mineralization in the Tres Hermanas district with the same period as that of the Cincinnati vein system. Direct evidence for the assumption is lacking, however, and certainly some of the mineralization of the district (viz., the pyrometasomatic iron deposits) is believed to be contemporaneous with the em-placement of the quartz monzonite stock. The writer believes, however, that practically all the ore mineralization of the district originated from deep-seated differentiation products of the quartz monzonite stock. The ore solutions formed from this stock were then released over several different periods, ranging from the time of the emplacement of the stock to the period when the basic dikes were emplaced.
Mining and milling methods: To the writer's knowledge, the ores from the various mines along the Cincinnati vein system were never milled, being only hand sorted and then shipped directly to the smelter. The discussion, therefore, will be limited to the method of mining the veins.
The veins have been developed by numerous shafts, pits, and trenches throughout their known strike lengths. The following shaft depths arc reported: Black Hawk mine, 65-foot inclined shaft; Hancock mine, 400-foot inclined shaft; Cincinnati mine, one vertical shaft, 300 feet deep, and another vertical shaft of unknown depth; Marie mine, one shaft at least 50 feet deep at the east end of the vein.
At present (1961), only the Black Hawk shaft is accessible. Rotten timber in the other shafts prevented the writer from examining them; therefore, the shaft depths reported above for three of the mines could not be verified. Near the surface, the veins were mined by simple trenching methods, small windlasses being used to hoist the ore from the trenches. Stoping from the shaft probably was from levels placed at about 50-foot intervals, the operation involving a combination of shrinkage and over-hand-with-stulls stoping methods. Many of the stopes that connected to the surface are still accessible; their walls have stood fairly well, even though some of these openings are 50 or more years old.
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Rock Types Recorded
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Alphabetical List Tree DiagramDetailed Mineral List:
Gallery:
List of minerals arranged by Strunz 10th Edition classification
| Group 1 - Elements | |||
|---|---|---|---|
| ⓘ | Native Gold | 1.AA.05 | Au |
| ⓘ | Native Silver | 1.AA.05 | Ag |
| Group 2 - Sulphides and Sulfosalts | |||
| ⓘ | Sphalerite | 2.CB.05a | ZnS |
| ⓘ | Galena | 2.CD.10 | PbS |
| ⓘ | Pyrite | 2.EB.05a | FeS2 |
| ⓘ | Arsenopyrite | 2.EB.20 | FeAsS |
| Group 3 - Halides | |||
| ⓘ | Bromargyrite | 3.AA.15 | AgBr |
| Group 4 - Oxides and Hydroxides | |||
| ⓘ | Goethite | 4.00. | Fe3+O(OH) |
| ⓘ | Hematite | 4.CB.05 | Fe2O3 |
| ⓘ | Quartz | 4.DA.05 | SiO2 |
| ⓘ | Opal var. Opal-AN | 4.DA.10 | SiO2 · nH2O |
| ⓘ | 4.DA.10 | SiO2 · nH2O | |
| ⓘ | Pyrolusite | 4.DB.05 | Mn4+O2 |
| ⓘ | Romanèchite | 4.DK.10 | (Ba,H2O)2(Mn4+,Mn3+)5O10 |
| Group 5 - Nitrates and Carbonates | |||
| ⓘ | Calcite | 5.AB.05 | CaCO3 |
| ⓘ | Smithsonite | 5.AB.05 | ZnCO3 |
| ⓘ | Dolomite | 5.AB.10 | CaMg(CO3)2 |
| ⓘ | Cerussite | 5.AB.15 | PbCO3 |
| ⓘ | Azurite | 5.BA.05 | Cu3(CO3)2(OH)2 |
| ⓘ | Malachite | 5.BA.10 | Cu2(CO3)(OH)2 |
| ⓘ | Aurichalcite | 5.BA.15 | (Zn,Cu)5(CO3)2(OH)6 |
| ⓘ | Hydrozincite | 5.BA.15 | Zn5(CO3)2(OH)6 |
| Group 7 - Sulphates, Chromates, Molybdates and Tungstates | |||
| ⓘ | Anglesite | 7.AD.35 | PbSO4 |
| ⓘ | Baryte | 7.AD.35 | BaSO4 |
| ⓘ | Wulfenite | 7.GA.05 | Pb(MoO4) |
| Group 8 - Phosphates, Arsenates and Vanadates | |||
| ⓘ | Mottramite | 8.BH.40 | PbCu(VO4)(OH) |
| ⓘ | Mimetite | 8.BN.05 | Pb5(AsO4)3Cl |
| ⓘ | Vanadinite | 8.BN.05 | Pb5(VO4)3Cl |
| Group 9 - Silicates | |||
| ⓘ | Willemite | 9.AA.05 | Zn2SiO4 |
| ⓘ | Hemimorphite | 9.BD.10 | Zn4Si2O7(OH)2 · H2O |
| ⓘ | Muscovite | 9.EC.15 | KAl2(AlSi3O10)(OH)2 |
| ⓘ | var. Sericite | 9.EC.15 | KAl2(AlSi3O10)(OH)2 |
| ⓘ | Kaolinite | 9.ED.05 | Al2(Si2O5)(OH)4 |
| ⓘ | Chrysocolla | 9.ED.20 | Cu2-xAlx(H2-xSi2O5)(OH)4 · nH2O, x < 1 |
| Unclassified | |||
| ⓘ | 'Limonite' | - | |
| ⓘ | 'Psilomelane' | - | |
| ⓘ | 'Calamine' | - | |
List of minerals for each chemical element
| H | Hydrogen | |
|---|---|---|
| H | ⓘ Aurichalcite | (Zn,Cu)5(CO3)2(OH)6 |
| H | ⓘ Azurite | Cu3(CO3)2(OH)2 |
| H | ⓘ Chrysocolla | Cu2-xAlx(H2-xSi2O5)(OH)4 · nH2O, x < 1 |
| H | ⓘ Goethite | Fe3+O(OH) |
| H | ⓘ Hemimorphite | Zn4Si2O7(OH)2 · H2O |
| H | ⓘ Opal var. Opal-AN | SiO2 · nH2O |
| H | ⓘ Hydrozincite | Zn5(CO3)2(OH)6 |
| H | ⓘ Kaolinite | Al2(Si2O5)(OH)4 |
| H | ⓘ Malachite | Cu2(CO3)(OH)2 |
| H | ⓘ Mottramite | PbCu(VO4)(OH) |
| H | ⓘ Muscovite | KAl2(AlSi3O10)(OH)2 |
| H | ⓘ Opal | SiO2 · nH2O |
| H | ⓘ Romanèchite | (Ba,H2O)2(Mn4+,Mn3+)5O10 |
| H | ⓘ Muscovite var. Sericite | KAl2(AlSi3O10)(OH)2 |
| C | Carbon | |
| C | ⓘ Aurichalcite | (Zn,Cu)5(CO3)2(OH)6 |
| C | ⓘ Azurite | Cu3(CO3)2(OH)2 |
| C | ⓘ Calcite | CaCO3 |
| C | ⓘ Cerussite | PbCO3 |
| C | ⓘ Dolomite | CaMg(CO3)2 |
| C | ⓘ Hydrozincite | Zn5(CO3)2(OH)6 |
| C | ⓘ Malachite | Cu2(CO3)(OH)2 |
| C | ⓘ Smithsonite | ZnCO3 |
| O | Oxygen | |
| O | ⓘ Anglesite | PbSO4 |
| O | ⓘ Aurichalcite | (Zn,Cu)5(CO3)2(OH)6 |
| O | ⓘ Azurite | Cu3(CO3)2(OH)2 |
| O | ⓘ Baryte | BaSO4 |
| O | ⓘ Calcite | CaCO3 |
| O | ⓘ Cerussite | PbCO3 |
| O | ⓘ Chrysocolla | Cu2-xAlx(H2-xSi2O5)(OH)4 · nH2O, x < 1 |
| O | ⓘ Dolomite | CaMg(CO3)2 |
| O | ⓘ Goethite | Fe3+O(OH) |
| O | ⓘ Hematite | Fe2O3 |
| O | ⓘ Hemimorphite | Zn4Si2O7(OH)2 · H2O |
| O | ⓘ Opal var. Opal-AN | SiO2 · nH2O |
| O | ⓘ Hydrozincite | Zn5(CO3)2(OH)6 |
| O | ⓘ Kaolinite | Al2(Si2O5)(OH)4 |
| O | ⓘ Malachite | Cu2(CO3)(OH)2 |
| O | ⓘ Mimetite | Pb5(AsO4)3Cl |
| O | ⓘ Mottramite | PbCu(VO4)(OH) |
| O | ⓘ Muscovite | KAl2(AlSi3O10)(OH)2 |
| O | ⓘ Opal | SiO2 · nH2O |
| O | ⓘ Pyrolusite | Mn4+O2 |
| O | ⓘ Quartz | SiO2 |
| O | ⓘ Romanèchite | (Ba,H2O)2(Mn4+,Mn3+)5O10 |
| O | ⓘ Smithsonite | ZnCO3 |
| O | ⓘ Vanadinite | Pb5(VO4)3Cl |
| O | ⓘ Willemite | Zn2SiO4 |
| O | ⓘ Wulfenite | Pb(MoO4) |
| O | ⓘ Muscovite var. Sericite | KAl2(AlSi3O10)(OH)2 |
| Mg | Magnesium | |
| Mg | ⓘ Dolomite | CaMg(CO3)2 |
| Al | Aluminium | |
| Al | ⓘ Chrysocolla | Cu2-xAlx(H2-xSi2O5)(OH)4 · nH2O, x < 1 |
| Al | ⓘ Kaolinite | Al2(Si2O5)(OH)4 |
| Al | ⓘ Muscovite | KAl2(AlSi3O10)(OH)2 |
| Al | ⓘ Muscovite var. Sericite | KAl2(AlSi3O10)(OH)2 |
| Si | Silicon | |
| Si | ⓘ Chrysocolla | Cu2-xAlx(H2-xSi2O5)(OH)4 · nH2O, x < 1 |
| Si | ⓘ Hemimorphite | Zn4Si2O7(OH)2 · H2O |
| Si | ⓘ Opal var. Opal-AN | SiO2 · nH2O |
| Si | ⓘ Kaolinite | Al2(Si2O5)(OH)4 |
| Si | ⓘ Muscovite | KAl2(AlSi3O10)(OH)2 |
| Si | ⓘ Opal | SiO2 · nH2O |
| Si | ⓘ Quartz | SiO2 |
| Si | ⓘ Willemite | Zn2SiO4 |
| Si | ⓘ Muscovite var. Sericite | KAl2(AlSi3O10)(OH)2 |
| S | Sulfur | |
| S | ⓘ Anglesite | PbSO4 |
| S | ⓘ Arsenopyrite | FeAsS |
| S | ⓘ Baryte | BaSO4 |
| S | ⓘ Galena | PbS |
| S | ⓘ Pyrite | FeS2 |
| S | ⓘ Sphalerite | ZnS |
| Cl | Chlorine | |
| Cl | ⓘ Mimetite | Pb5(AsO4)3Cl |
| Cl | ⓘ Vanadinite | Pb5(VO4)3Cl |
| K | Potassium | |
| K | ⓘ Muscovite | KAl2(AlSi3O10)(OH)2 |
| K | ⓘ Muscovite var. Sericite | KAl2(AlSi3O10)(OH)2 |
| Ca | Calcium | |
| Ca | ⓘ Calcite | CaCO3 |
| Ca | ⓘ Dolomite | CaMg(CO3)2 |
| V | Vanadium | |
| V | ⓘ Mottramite | PbCu(VO4)(OH) |
| V | ⓘ Vanadinite | Pb5(VO4)3Cl |
| Mn | Manganese | |
| Mn | ⓘ Pyrolusite | Mn4+O2 |
| Mn | ⓘ Romanèchite | (Ba,H2O)2(Mn4+,Mn3+)5O10 |
| Fe | Iron | |
| Fe | ⓘ Arsenopyrite | FeAsS |
| Fe | ⓘ Goethite | Fe3+O(OH) |
| Fe | ⓘ Hematite | Fe2O3 |
| Fe | ⓘ Pyrite | FeS2 |
| Cu | Copper | |
| Cu | ⓘ Aurichalcite | (Zn,Cu)5(CO3)2(OH)6 |
| Cu | ⓘ Azurite | Cu3(CO3)2(OH)2 |
| Cu | ⓘ Chrysocolla | Cu2-xAlx(H2-xSi2O5)(OH)4 · nH2O, x < 1 |
| Cu | ⓘ Malachite | Cu2(CO3)(OH)2 |
| Cu | ⓘ Mottramite | PbCu(VO4)(OH) |
| Zn | Zinc | |
| Zn | ⓘ Aurichalcite | (Zn,Cu)5(CO3)2(OH)6 |
| Zn | ⓘ Hemimorphite | Zn4Si2O7(OH)2 · H2O |
| Zn | ⓘ Hydrozincite | Zn5(CO3)2(OH)6 |
| Zn | ⓘ Smithsonite | ZnCO3 |
| Zn | ⓘ Sphalerite | ZnS |
| Zn | ⓘ Willemite | Zn2SiO4 |
| As | Arsenic | |
| As | ⓘ Arsenopyrite | FeAsS |
| As | ⓘ Mimetite | Pb5(AsO4)3Cl |
| Br | Bromine | |
| Br | ⓘ Bromargyrite | AgBr |
| Mo | Molybdenum | |
| Mo | ⓘ Wulfenite | Pb(MoO4) |
| Ag | Silver | |
| Ag | ⓘ Bromargyrite | AgBr |
| Ag | ⓘ Native Silver | Ag |
| Ba | Barium | |
| Ba | ⓘ Baryte | BaSO4 |
| Ba | ⓘ Romanèchite | (Ba,H2O)2(Mn4+,Mn3+)5O10 |
| Au | Gold | |
| Au | ⓘ Native Gold | Au |
| Pb | Lead | |
| Pb | ⓘ Anglesite | PbSO4 |
| Pb | ⓘ Cerussite | PbCO3 |
| Pb | ⓘ Galena | PbS |
| Pb | ⓘ Mimetite | Pb5(AsO4)3Cl |
| Pb | ⓘ Mottramite | PbCu(VO4)(OH) |
| Pb | ⓘ Vanadinite | Pb5(VO4)3Cl |
| Pb | ⓘ Wulfenite | Pb(MoO4) |
Localities in this Region
- New Mexico
- Luna County
- Tres Hermanas Mountains
- Tres Hermanas Mining District
- Mahoney Mines area
- Cincinnati vein system
- Mahoney Mines area
- Tres Hermanas Mining District
- Tres Hermanas Mountains
- Luna County
Other Regions, Features and Areas containing this locality
North AmericaContinent
North America PlateTectonic Plate
- Basin and Range BasinsBasin
- Mazatzal DomainDomain
- Sierra Madre OrientalWide Rift
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References
Hancock Mine, Cincinnati vein system, Mahoney Mines area, Tres Hermanas Mining District, Tres Hermanas Mountains, Luna County, New Mexico, USA