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Minerals 2012, 2(3), 228-243; doi:10.3390/min2030228
Published: 14 August 2012
Abstract: Tertiary low sulfidation (LS) epithermal deposits in the western USA often show evidence of the former presence of nanoparticle-sized precious-metal and silica phases in the highest grade (bonanza) ores. Here, nanoparticles are defined to have a size less than ~10−7 m. The ore-mineral textures that formed from aggregation of nanoparticles (or colloids) observed to date in these ores include electrum and naumannite (Ag2Se). Here it is proposed that chalcopyrite also forms nanoparticles in these ores, but sulfide nanoparticles apparently have significantly different physical (surface) properties than the precious-metal phases, and thus exhibit different mineral textures (e.g., no textural evidence of previous chalcopyrite nanoparticles). Textures described here show that nanoparticles of precious-metal phases and silica were episodically and often repeatedly deposited to form the banded bonanza veins typical of many western USA epithermal deposits. Chalcopyrite is the most abundant metal-sulfide mineral in these bonanza ores, and it was also deposited episodically as well, and it appears to replace earlier formed naumannite dendrites. However, this apparent “replacement” texture may just be the result of naumannite dendrite limbs trapping chalcopyrite nanoparticles that later recrystallized to the apparent replacement texture. The episodic and repetitive nature of the metal-depositing events may record periodic “degassing” of magma chambers at depth, where metals are repeatedly delivered to the shallow epithermal environment by “vapor-phase” metal (loid) transport.
The “paragenetic sequence” diagram has been the hallmark of ore-textural investigations for more than a century, and it has proven useful to illustrate time relationships in ore-forming events. Such evidence as replacement textures, cross-cutting relationships, exsolution features, and crustification sequences have been used to deduce chronology during ore formation. Some of these evidences perhaps are more ambiguous than others. However, it is a central tenet of geology that the deposition of subsequent layers of geologic materials is the ultimate tool in deciphering the chronology of events. In ores, nowhere is this principle illustrated better than in banded bonanza epithermal ores, where successive layers of ore and gangue minerals coat fracture (vein) walls. Investigations of some of these Tertiary banded bonanza ores in western USA (Figure 1) reveal some universal features in these ores besides their rich endowments of precious metals at the hand-sample scale: (1) fine-grained quartz (and locally opal) textures implying former presence of amorphous silica precursors or chalcedony in addition to direct quartz precipitation; (2) they are commonly Se-rich and locally contain ubiquitous Ag-Se(±S) phases; (3) sulfide and sulfosalts in intimate association with precious- metal minerals at the hand-sample scale are typically much less abundant than electrum+naumannite; and (4) they all have some textural evidence of silica and Au-Ag phases being transported and deposited in the bonanza ore setting as small particles [1,2,3,4]. A similar interpretation perhaps can be made from Hishikari, Kushikino, and Koryu epithermal deposits in Japan [5,6,7,8,9,10].
Textural evidence [1,2] from the bonanza low-sulfidation Sleeper deposit in Nevada supported the concept that gold (and silica) colloids played an important role in forming extraordinary high-grade Au-Ag ores there. Earlier, Lindgren  had made a similar proposal for extremely high-grade ores from the National Deposit, National District, Nevada which he had studied previously . Saunders  also showed that naumannite formed dendritic growths associated with colloidal silica at the Sleeper deposit, and later Saunders et al.  proposed that naumannite (Ag2Se) also formed colloids in bonanza Se-rich epithermal deposits of western USA. This conclusion is supported by naumannite textures elsewhere in Nevada, such as at Midas , Buckskin National [3,4,14], Seven Troughs , and Republic (Washington) , and perhaps the above-mentioned Japanese deposits.
Textures often are notoriously difficult to interpret in the absence of controlled experiments e.g., , but the primary textural evidence described below for episodic introduction of metals into bonanza ores is generally unambiguous given the banded crustification textures of the ores described. However, in terms of colloid formation, there is some ambiguity given the propensity of colloids to (re)crystallize over time, as has been well documented for silica in the inversion of opal to chalcedony and quartz [16,17]. Saunders et al.  proposed two different textures that support nanoparticle formation in epithermal ores: (1) evidence of physical transport of nanoparticles by ore-forming fluids, which Saunders et al.  “sluice box” textures; and (2) a specific colloid aggregation texture which we call “fractal dendrites”. The term dendrite has different connotations to different users. Saunders et al.  differentiated between “dendritic” gold crystals that have a “feathery” appearance yet where dendrite branching was controlled by internal crystal structure, versus a 3-dimensional chaotic growth pattern which they interpreted to form by colloid aggregation. The latter follow a fractal growth pattern caused by efficient sticking of the metal colloids [18,19] and has the general appearance of a conifer tree or perhaps even sage brush  and have been called “fractal dendrites” to distinguish these features from more crystalline dendrites. Irrespective of their appearance, they formed as positive “topographic” features on the vein walls and point toward the center of the vein (“younging” direction [2,3,17]).
Saunders [1,2] proposed that electrum and silica colloids at the Sleeper deposit nucleated as a consequence of H2S loss in the boiling zone in the shallow epithermal system. The more recent recognition that naumannite also forms ubiquitous colloids in the bonanza epithermal ores of western USA perhaps argues against a simple boiling model: If the loss of H2S leads to electrum particle nucleation during boiling, it would seem that a similar loss in H2Se would mitigate against naumannite colloid formation in the same zone. Further, recent reconnaissance Pb-isotopic investigations by Kamenov et al.  suggest that electrum and naumannite have “locked in” a deep, primitive, mafic-magma Pb-isotope signature. Further, more recent hypotheses regarding “vapor-phase” transport of metal(loid)s up from the magmatic environment to the epithermal setting [22,23,24] beg the question that perhaps some precious-metal mass transport to the epithermal setting might be accomplished by nano-particles. Thus, the purpose of this note is to document some ore textures in a few admittedly non-typical, very high-grade epithermal deposits to pose the possibility that these textures might be the result of deep ore-forming processes, and that evidence of those processes might be preserved in the shallow bonanza ores.
A colloid is small particle (crystalline, organic, or amorphous) generally thought of as an entity that is larger than ~10−9 m and a nanoparticle is typically considered to have a size less than 10−7 m. Because atoms are at the scale of ~10−10 m, the “nano” realm only comprises about 3 orders of magnitude in size. Although colloids have size implications and their diameters can overlap with nanoparticles, colloids have the added constraint that they must be dispersed in a liquid. In hydrothermal settings, it is proposed here that the term nanoparticle should be used instead of “colloid” as there is no evidence that the particles are either dispersed in or transported by a true liquid (more likely, a super-critical fluid). However, from a materials engineering standpoint, the 10−7 m threshold is the approximate size below which nanoparticles may have different physical and chemical “surface” properties than the bulk solids, and thus might have some interesting industrial applications.
From a geologic standpoint, what might be their significance? The average pore diameter in shale or the width of a microfracture in crystalline rock is on the order of 10−6 m e.g.,  and thus a nanoparticle is smaller than that by ~1–3 orders of magnitude and thus can be transported through these solids. Although we typically think of shale as an “aquitard” in hydrogeology, fluids can flow through essentially any kind porous media. Fluid flow is a function of not only a function of the intrinsic permeability of the geologic material, but also of viscosity and density of the fluid itself .
SEM images of electrum surfaces from fractal dendrites from the Sleeper deposit, Nevada  indicate that if they formed by aggregation of small particles, then the particles were ~10−7 to 10−8 m in size. Thus in the newer terminology those “fractal” dendrites were made from electrum nanoparticles as opposed to colloids. Others have interpreted the origin of “fractal” dendrites in bonanza epithermal gold ore to be the result of diffusion of gold in silica gels . Do gold (or naumannite) nanoparticles have different physical properties than gold colloids, and do nanoparticles of gold as they are transported up? Clearly some experimental investigations might shed some light on these questions. In gold sols (a stable aqueous suspension of colloid/nanoparticles) gold nanoparticles repel each other upon mutual approach at room temperature (preventing “sticking”), which is the expected behavior of gold colloids with negatively-charged surfaces . Irrespective of whether gold (electrum) nanoparticles have different physical properties than macro-scale gold particles or crystals, the working hypothesis now is that nanoparticles in these bonanza epithermal systems form deeper than the epithermal setting as their Pb-isotopic composition is very primitive and magma-like . This suggests that the nanoparticles formed near their magmatic source, locked in a magmatic isotopic signature, and were transported upward to the epithermal environment and deposited there. Perhaps the surface properties of the nanoparticles and/or colloids is precisely what keeps them entrained in the upward moving fluids and brings them to the point of deposition that perhaps result in the textures described below.
2. Ore Textures
Evidence of silica and precious-metal nanoparticles has been observed in ores from the 11 deposits and districts shown in Figure 1. Most of the bonanza deposits shown in Figure 1 are mid-Miocene in age and have been interpreted to be related to the initial emergence of the Yellowstone Hotspot [14,27], with the exception of bonanza veins in the Republic district of Washington which are Eocene . Irrespective of their age or possible geotectonic origin, all of the deposits considered here have additional similarities not described above. These include a banded nature of the veins, composed of successively deposited layers of ore and gangue minerals; and that chalcopyrite is typically the most abundant sulfide phase present in the highest-grade Au-Ag ores. The latter is also similar to the above-mentioned Japanese deposits, and at Hishikari there is a stronger statistical correlation between Au and Cu. Copper is by far the most abundant base metal in the bonanza ores [8,9]. In the US deposits, textural evidence indicates that ore and gangue minerals were deposited episodically and repeatedly, such that ores exhibiting the most number of banding events typically have the highest grades . Because these episodic/banded textures are best exhibited by the Sleeper and Buckskin National deposits they will be used here to illustrate these features. These two deposits also represent “end-member” mineralogical types of ores of the 11 deposits shown in Figure 1. Sleeper represents ores (similar to Jumbo and National) where electrum is by far the most abundant mineral of any variety in the bonanza ore; and Buckskin National represents the opposite situation, where naumannite is by far the most abundant ore mineral and electrum only occurs rarely (similar to DeLamar, Silver City, ID, USA). Most of the rest contain significantly more naumannite than electrum, and by value of contained metals, they would be considered “gold” ores (such as at Midas and Ivanhoe-Hollister, Nevada; War Eagle and Florida Mountains, Silver City, ID, USA).
Bonanza ore textures from Sleeper have been documented previously [1,2] primarily with the intent to illustrate that both silica and electrum nanoparticles were important in forming those ores and perhaps others elsewhere. More recently, Saunders  discussed one implication of the 100 s of episodes of gold deposition at Sleeper, suggesting that each perhaps represented a discrete (short) time interval for each gold layer formation, and further suggested that perhaps the entire bonanza ore-forming event might have been much shorter than previously thought (a possibility also suggested by Heinrich et al.  Simmons and Brown , and Heinrich ).
In the Sleeper “main” vein (Figure 2), many electrum-depositing events can be seen even at the cm-scale. Some hand samples of bonanza ores from Sleeper show up to 50 different electrum-rich bands, which represents successive deposition (coating) of electrum on the vein walls over time . Individual electrum-rich bands are typically 50%–70% by volume of electrum (Figure 2) and at the Sleeper deposit electrum is often the only ore mineral in the bands. Opal typically (perhaps slightly (re)crystallized) and trace amounts of adularia form the remainder of the electrum bands. Intervening silica bands often exhibit textures suggesting amorphous silica precursors as well (often crystallized gels), and also locally include abundant adularia . As documented by Saunders  and Saunders and Schoenly [18,19], electrum-rich bands consist aggregates (“forests”) of fractal electrum dendrites with tree-like shapes (Figure 3) that formed by electrum and silica colloid aggregation. Although they form by a fractal-growth process, the dendrites are excellent examples of “natural” fractals, which are self-similar over a number of scales. Such electrum fractals can range from <0.1 mm in size to >10 cm in diameter, with the largest fractal dendrites yet observed from the National deposit [3,11,12].
The National and Buckskin National deposits (Figure 1) are both located in the National district and are only a few km apart, but differ significantly in the abundance of ore minerals in the bonanza ores . Highest grade ores from Buckskin National are banded and contain large and spectacular fractal naumannite drendites (Figure 4) that formed episodically. As in the case of the fractal electrum dendrites from Sleeper, the dendrites point toward the center of the vein. Electrum in these ores is typically rarely observed . However, in the sample shown in Figure 4, electrum is fairly abundant as inclusions in naumannite dendrites, and it appears to have been incorporated into the dendrites at discrete time intervals, but perhaps more significantly, a single electrum-rich band occurs in at least one instance after one stage of naumannite dendrite formation ceased (Figure 4). This texture has not been seen by the author (or documented) at Buckskin National previously, and represents a rare electrum >> naumannite stage of ore deposition there. In detail, the electrum-rich band consists of a number of fractal electrum dendrites (Figure 5) that are very similar to those seen in the Sleeper deposit and thus probably also formed by electrum nanoparticle aggregation along the vein wall at that time.
Another sample from the Bell vein, Buckskin National, shows that chalcopyrite was also introduced episodically in the ore (Figure 6). It generally appears to have been deposited late in the naumannite dendrite growth in the various bands. In detail, chalcopyrite appears to encrust and replace naumannite in the dendrites, leaving un-replaced “islands” of naumannite (Figure 7). Locally, other precious-metal and sulfide minerals can also be found in the naumannite dendrite and may be part of the dendrite “structure”, as in the case of pyrargyrite shown in Figure 8.
Barton et al.  and Roedder  have documented that even relatively slow-moving hydrothermal solutions can transport colloidal-sized particles in ore-forming systems, and that those particles sometimes can be trapped as solid inclusions in fluid inclusions (as opposed to forming as true daughter phases). Kouzmanov et al.  also documented that Au-Ag solid nanoparticles were trapped in fluid inclusions (in the deep porphyry environment) they analyzed for metal contents using laser-ablation-ICP-MS. Brown  documented that colloidal precious-metal alloys and metal sulfides, along with silica colloids, formed due to boiling (by a controlled pressure drop) in a geothermal well at Ohaaki (formerly known as Broadlands), New Zealand. Brown also calculated for the first time how much dissolved gold was apparently present in that geothermal reservoir. Similarly, Fournier [16,17] documented the transport of silica colloids in hydrothermal fluids, and proposed gold may attach to them. Further Lindgren  states: “Gold is easily brought into the colloidal state and as such may be transported in solutions of colloidal silica.” Saunders  demonstrated that silica and gold (electrum) colloids of similar size apparently were physically transported together and codeposited to form the spectacularly-high grade ores from the Sleeper deposit. More recent studies [3,4,12] documented conclusively that naumannite forms colloidal or nano-sized particles in some bonanza epithermal ores of western USA, and can be physically transported to the site of ore deposition. This contribution documents that chalcopyrite is a ubiquitous ore mineral present in these bonanza ores, and proposes (by analogy to former presence of electrum, naumannite and silica colloids in the same ores) that it too was physically transported to the site of ore deposition.
Sulfide nanoparticles have been described previously, particularly Fe-sulfide phases e.g., [36,37]. Bacteria-mediated ZnS formation has also been documented, and sphalerite formed by this process commonly occurs as self-organized spheroidal particles that are ~100 nm in diameter, which in turn composed of smaller aggregated nanoparticles of ZnS [38,39,40,41]. Chalcopyrite nanoparticles are routinely synthesized for their use in “nano” technological applications  and amorphous biogenic Cu(Fe)-S nanoparticles have also been documented by Saunders et al.  forming in groundwater under sulfate-reducing conditions. No doubt other base-metal sulfide nanoparticles also form in black smoker settings along with FeS nanoparticles. Nano-scale inclusions of chalcopyrite in sphalerite have had a long history of debate concerning their origin  but a “direct” colloidal origin of those textures was ruled out by Barton and Bethke . Thus suffice it to say that sulfide nanoparticles have been documented in the literature, and perhaps their formation is a common phenomenon but is probably not well preserved due to post-depositional changes, metamorphism, etc., and only a few studies have been done on actual hydrothermal solutions such that by Yucel et al. .
Assuming that both metal “alloys” (electrum, naumannite) and sulfide nanoparticles form in the epithermal deposits discussed here, and their deposition leads to the textures documented here (and most likely their extreme high grades), an important question is where do they form? Saunders [1,2] proposed that they formed in the shallow epithermal setting due to boiling and were also deposited there. However, new reconnaissance Pb-isotope  and Re-Os data  suggest that the electrum has locked in a deep, primitive isotopic signature not consistent with it nucleating at a shallow depth. Additional isotopic studies are ongoing to better evaluate that initial interpretation. However, for the sake of this discussion, why might such particle form deep below the normal epithermal setting, and why would be they be entrained in the hydrothermal fluid? With regards to the latter, Yucel et al.  calculated using Stoke’s Law that a 200 nm (colloidal size by the definition set forth here) pyrite particle would have a settling velocity in a stagnant aqueous solution of 1.43 m/year, and thus even a slow moving fluid could easily carry it along during flow. The density of electrum would require perhaps a faster moving fluid than for entraining pyrite nanoparticles, but earliest formed particles would be 1–2 orders of magnitude smaller than the particle size used in Yucel et al.’s calculation . Why would they be entrained as opposed to sticking to pore/fracture walls? Again, we know little of nanoparticle physical behavior for metal alloys or sulfides, but it is possible that surface charge considerations are even more important than for colloid-sized particles discussed by Saunders [1,2], and thus there could be a natural repulsion of the nanoparticles by the pore walls (and from their own surfaces as the nanoparticles approach each other). As nanoparticles move up they grow bigger, which ultimately can lead to their sticking to each other and/or surfaces of other mineral phases by a process called orthokinetic aggregation . Orthokinetic aggregation is caused by increasing the momentum (mass × velocity) of a nanoparticle such that they can overcome surface-charge repulsion, allowing them collide and stick. In the epithermal environment, boiling of the hydrothermal solutions may accelerate the particles causing orthokinetic aggregation.
With regards to why or how the nanoparticles might form at depth, one can only speculate on this point. Gold crystals (~10−6 m in diameter) grew in a silica tube inserted into a fumarole vent (T = 800 °C) at Colima volcano, Mexico  attesting to the capability of super-critical (magmatic?) fluids to transport gold, which is consistent with recent findings from laser-ablation ICP-MS fluid inclusion studies e.g., [22,23]. Kamenov et al.  and Saunders et al.  proposed that basaltic magmas were the source of gold and related elements in the mid-Miocene western USA ores. If a low-density, volatile-rich and metal-rich magmatic fluid is rereleased from such a magma chamber or separates from a denser brine, as suggested by Heinrich et al. [23,24], then several hundred degrees of cooling likely would be an effective mechanism of saturating the fluid with respect to the nanoparticle minerals electrum, naumannite, and chalcopyrite as it moves up through the porphyry-to-epithermal setting. Perhaps some laboratory experiments could be designed to test this hypothesis. However, Yucel et al.  showed that FeS nanoparticle formation had occurred prior to the mixing of discharging high temperature hydrothermal fluids with cold seawater in a seafloor “black smoker”, suggesting transport of them for some distance below the surface in that setting.
It is proposed here that the episodic deposition of ore minerals in the ores that are the subject of this communication is best explained by episodic and periodic incursion of low-density magmatic fluids (“vapors”) rich in metals. Previously, Saunders  proposed that the formation of 100 s of gold-rich bands at the Sleeper deposit was a function of episodic boiling in that system. It has been demonstrated [30,35] that boiling is an effective gold-depositional process in geothermal fluids significantly under-saturated with respect to gold prior to boiling. But does this conclusion hold for gold-rich ore forming fluids such as interpreted by Saunders and Schoenly  for deposits such as Sleeper? Saunders  revisited the episodic boiling model for Sleeper, and documented that hydrothermal solutions were boiling even during times between gold depositional events there. Thus if episodic boiling did not cause multiple gold-silver depositional events recorded in bonanza ores from Sleeper and other deposits considered here, then what did? Perhaps the simplest explanation might be episodic degassing of a magma chamber at depth, with subsequent “vapor-phase” transport of metals up into the epithermal setting, and ultimately the magmatic-vapors were absorbed by the heated groundwater in the shallow subsurface. Clearly much more study of bonanza Au-Ag ore formation is warranted.
Although perhaps best evident in LS epithermal deposits from Nevada, Idaho, and Washington of the western USA such as those discussed here, gold/electrum nanoparticles might also be locally important in some bonanza epithermal ores such as in Japan [5,6,7,8,9,10] and elsewhere in western USA such as McLaughlin, California , and the Sunnyside gold mine  of the Silverton district, San Juan Mountains, Colorado. High-grade Sunnyside ores contained discrete electrum/gold-rich depositional events that also appear to have formed by colloid aggregation (Figure 9). Further, recent exploration core drilling at the historic Haile mine in the Carolina Slate belt of South Carolina, (which is probably a metamorphosed LS epithermal deposit: author’s interpretation only) has encountered bonanza mineralization with spectacular textures reminiscent of silica and gold textures from Sleeper (Figure 10). Finally, the well-documented extremely fine-grained gold grains typical of Carlin-type deposits perhaps could be due to some degree of physical transport of gold nanoparticles .
The term “nanoparticle” (particles < 100 nm; 10−7 m) is proposed here with respect to ores and hydrothermal fluids, as opposed to colloids that are more of a low-temperature laboratory construct (although dispersed clays in surface waters mimic laboratory-produced sols). With recent advances in “nano” science, the assumption that nanoparticles are dissolved is no longer tenable, and as shown by Yucel et al.  can contribute significantly to hydrothermal max flux of metals, sulfur, etc.
With respect to epithermal systems, it appears that nanoparticles can be important in mass flux of metals in the porphyry-to-epithermal environment. However, textural evidence of this at the point of deposition is perhaps best preserved in only the highest-grade ores and ore-forming systems. And in such ores from western USA that are the subject of this contribution, there is ample evidence for this metal influx occurring episodically, which might be the result of episodic magma-degassing events at depth.
This work was supported by a grant from the National Science Foundation to J. Saunders (EAR-0838208). Special thanks to James Berry of Romarco Minerals for providing the photographs of the bonanza ores from the Haile deposit, South Carolina, and Paul B. Barton, Jr., for the sample from Sunnyside Mine, Colorado. Detailed observations of bonanza ores from the Ken Snyder deposit (Midas) by Derick Unger and John Marma of Newmont Mining were most helpful in this research. Collins Aseto aided in figure preparation as well as sample preparation from his thesis area of the Silver City, Idaho district.
- Saunders, J.A. Colloidal transport of gold and silica in epithermal precious metal systems: Evidence from the sleeper deposit, Humboldt County, Nevada. Geology 1990, 18, 757–760. [Google Scholar] [CrossRef]
- Saunders, J.A. Silica and gold textures at the sleeper deposit, Humboldt County, Nevada: Evidence for colloids and implications for ore-forming processes. Econ. Geol. 1994, 89, 628–638. [Google Scholar] [CrossRef]
- Saunders, J.A.; Schoenly, P.A.; Cook, R.B. Electrum disequilibrium crystallization textures in volcanic-hosted bonanza epithermal gold deposits. In Geology and Ore Deposits of the America Cordillera; Proceedings of Nevada Symposium, Reno-Sparks, NV, USA, 10–13 April 1995; Coyner, A.R., Fahey, P.L., Eds.; Geological Society of Nevada: Reno-Sparks, NV, USA, 1996; pp. 173–179. [Google Scholar]
- Saunders, J.A.; Vikre, P.; Unger, D.L.; Beasley, L. Colloidal and physical transport textures exhibited by electrum and naumannite in bonanza epithermal veins from western USA, and their significance. In Great Basin Evolution and Metallogeny; Proceedings of Geological Society of Nevada 2010 Symposium, Reno-Sparks, NV, USA, 14 May 2010; Steininger, R., Pennell, W., Eds.; Geological Society of Nevada: Reno-Sparks, NV, USA, 2011; pp. 825–832. [Google Scholar]
- Shikazono, N. A comparison of temperatures estimated from the electrum-sphalerite-pyrite-argentite assemblage and filling temperatures of fluid inclusions from epithermal Au-Ag vein-type deposits in Japan. Econ. Geol. 1985, 80, 1415–1494. [Google Scholar] [CrossRef]
- Matsuhisa, Y.; Morishita, Y.; Sato, T. Oxygen and carbon isotope variations in gold-bearing hydrothermal veins in the Kushikino mining area, Southern Kyushu, Japan. Econ. Geol. 1985, 80, 283–293. [Google Scholar] [CrossRef]
- Izawa, E.; Urashima, Y.; Ibaraki, K.; Suzuki, R.; Yokohama, T.; Kawasaki, K.; Koga, A.; Taguchi, S. The Hishikari gold deposit: High-grade epithermal veins in Quaternary volcanics of Southern Kyushu, Japan. J. Geochem. Explor. 1990, 36, 1–56. [Google Scholar] [CrossRef]
- Shikazono, N.; Nagayama, T. Origin and deposition mechanisms of the Hishikari gold-quartz-adularia mineralization. Resource Geol. 1993, 14, 47–56. [Google Scholar]
- Nagayama, T. Precipitation sequence of veins at the Hishikari deposits, Kyushu, Japan. Resource Geol. 1993, 14, 13–28. [Google Scholar]
- Shimizu, T.; Matsueda, H.; Ishiyama, D.; Matsubaya, O. Genesis of epithermal Au-Ag mineralization of the Koryu Mine, Hokkaido, Japan. Econ. Geol. 1998, 93, 303–325. [Google Scholar] [CrossRef]
- Lingdren, W. Mineral Deposits, 4th ed.; McGraw-Hill: New York, NY, USA, 1933; p. 486. [Google Scholar]
- Lindgren, W. Geology and mineral deposits of the National District, Nevada. U.S. Geol. Surv. Bull. 1915, 601, 1–58. [Google Scholar]
- Goldstrand, P.M.; Schmidt, K.W. Geology, mineralization, and ore controls at the Ken Snyder gold-silver mine, Elko County, Nevada. In Geology and Ore Deposits 2000: The Great Basin and Beyond; Proceedings of Nevada Symposium, Reno-Sparks, NV, USA, 15–18 May, 2000; John, D.A., Wallace, A.R., Eds.; Geological Society of Nevada: Reno-Sparks, NV, USA, 2000; pp. 265–287. [Google Scholar]
- Saunders, J.A.; Unger, D.L.; Kamenov, G.D.; Fayek, M.; Hames, W.E.; Utterback, W.C. Genesis of Middle Miocene Yellowstone-hotspot-related bonanza epithermal Au-Ag deposits, Northern Great Basin Region, USA. Mineral. Dep. 2008, 43, 715–734. [Google Scholar] [CrossRef]
- Simmons, S.F.; Christenson, B.W. Origins of calcite in a boiling geothermal system. Am. J. Sci. 1994, 294, 361–400. [Google Scholar] [CrossRef]
- Fournier, R.O. Silica minerals as indicators of conditions during gold deposition. U.S. Geol. Surv. Bull. 1985, 1646, 15–26. [Google Scholar]
- Fournier, R.O. The behavior of silica in hydrothermal solutions. Rev. Econ. Geol. 1986, 2, 45–62. [Google Scholar]
- Saunders, J.A.; Schoenly, P.A. Boiling, colloid nucleation and aggregation, and the genesis of bonanza gold mineralization at the Sleeper Deposit, Nevada. Mineral. Dep. 1995, 30, 199–211. [Google Scholar] [CrossRef]
- Saunders, J.A.; Schoenly, P.A. Fractal structure of electrum dendrites in bonanza epithermal Au-Ag deposits. In Fractal Geometry and Its Use in the Earth Sciences; Barton, C.C., La Pointe, P.R., Eds.; Plenum Publishing: New York, NY, USA, 1995; pp. 251–261. [Google Scholar]
- Vikre, P.G. Precious metal vein system in the National district, Humboldt County, Nevada. Econ. Geol. 1985, 80, 360–393. [Google Scholar] [CrossRef]
- Kamenov, G.D.; Saunders, J.A.; Hames, W.E.; Unger, D.L. Mafic magmas as sources for gold in middle Miocene epithermal deposits of the Northern Great Basin, United States: Evidence from Pb isotope compositions of native gold. Econ. Geol. 2007, 102, 1191–1195. [Google Scholar] [CrossRef]
- Heinrich, C.A.; Gunther, D.; Audetat, A.; Ulrich, T.; Frischknect, R. Metal fractionation between magmatic brine and vapor, determined by microanalysis of fluid inclusions. Geology 1999, 27, 755–758. [Google Scholar]
- Heinrich, C.A.; Driesner, T.; Stefansson, A.; Seward, T.M. Magmatic vapor contraction and the transport of gold from the porphyry environment to epithermal ore deposits. Geology 2004, 32, 761–764. [Google Scholar] [CrossRef]
- Williams-Jones, A.E.; Heinrich, C.A. Vapor transport of metals and the formation of magmatic-hydrothermal ore deposits. Econ. Geol. 2005, 100, 1287–1312. [Google Scholar] [CrossRef]
- Freeze, A.R.; Cherry, J.A. Groundwater; Prentice Hall: New York, NY, USA, 1979. [Google Scholar]
- Sherlock, R.L.; Lehrman, N.J. Occurrences of dendritic gold at the McLaughlin mine. Miner. Dep. 1995, 30, 323–327. [Google Scholar] [CrossRef]
- Hames, W.E.; Unger, D.L.; Saunders, J.A.; Kamenov, G.D. Metallogeny and magmatism in the early Yellowstone hotspot. J. Volcan. Geotherm. Res. 2009, 188, 214–224. [Google Scholar] [CrossRef]
- Fifarek, R.H.; Devlin, B.D.; Tschauder, R.J., Jr. Au-Ag mineralization at the Golden Promise deposit, Republic district, Washington: Relation to graben development and hot spring processes. In Geology and Ore Deposits of the America Cordillera; Proceedings of Nevada Symposium, Reno-Sparks, NV, USA, 10–13 April 1995; Coyner, A.R., Fahey, P.L., Eds.; Geological Society of Nevada: Reno-Sparks, NV, USA, 1996; pp. 1063–1088. [Google Scholar]
- Saunders, J.A. Geologic Time and Epithermal ore Formation: SEG Newsletter; Society of Economic Geologists: Littleto, CO, USA, 2010; pp. 10–11. July; No. 82. [Google Scholar]
- Simmons, S.F.; Brown, K.L. Gold in magmatic hydrothermal solutions and the rapid formation of a giant ore deposit. Science 2006, 314, 288–291. [Google Scholar] [CrossRef]
- Heinrich, C.A. How fast does gold trickle out of volcanoes? Science 2006, 314, 163–264. [Google Scholar]
- Barton, P.B., Jr.; Bethke, P.M.; Toulmin, P., III. An attempt to determine the vertical component of flow rate of ore-forming solutions in the OH vein, Creede, Colorado. In Proceedings of IAGOD 1970 Meeting, Kyoto, Japan, 1971; pp. 132–136.
- Roedder, E. Fluid Inclusions; Ribbe, P.H., Ed.; Mineralogical Society of America: San Francisco, CA, USA, 1984; Volume 12, p. 644. [Google Scholar]
- Kouzmanov, K.; Pettke, T.; Heinrich, C.A. Direct analysis of ore-precipitating fluids: Combined IR microscopy and LA-ICP-MS study of fluid Inclusions in opaque ore minerals. Econ. Geol. 2010, 105, 351–373. [Google Scholar] [CrossRef]
- Brown, K.L. Gold deposition from geothermal discharges in New Zealand. Econ. Geol. 1986, 81, 979–983. [Google Scholar] [CrossRef]
- Wilkin, R.T.; Barnes, H.L. Formation processes of framboidal pyrite. Geochim. Cosmochim. A. 1997, 61, 323–339. [Google Scholar] [CrossRef]
- Yucel, M.; Gartman, A.; Chan, C.S.; Luther, G.W., III. Hydrothermal vents as a kinetically stable source of iron-sulphide-bearing nano particles to the ocean. Nature Geosci. 2011, 4, 367–371. [Google Scholar] [CrossRef]
- Labrenz, M.; Druchel, G.; Thomsen-Ebert, T.; Gilbert, B.; Welch, S.A.; Kemner, K.M.; Logan, G.A.; Summons, R.E.; de Stasio, G.; Bond, P.L.; Lai, B.; Kelly, S.D.; Banfield, J.F. Formation of sphalerite (ZnS) deposits in natural biofilms of sulfate reducing bacteria. Science 2000, 290, 1744–1747. [Google Scholar]
- Druschel, G.K.; Labrenz, M.; Thomsen-Ebert, T.; Fowle, D.A.; Banfield, J.F. Geochemical modeling of ZnS in biofilms: An example of ore depositional processes. Econ. Geol. 2002, 97, 1319–1329. [Google Scholar] [CrossRef]
- Southam, G.; Saunders, J.A. Geomicrobiology of ore deposits. Econ. Geol. 2005, 100, 1067–1084. [Google Scholar] [CrossRef]
- Saunders, J.A.; Lee, M-K.; Wolf, L.A.; Morton, C.M.; Feng, Y.; Thomson, I.; Park, S. Geochemical, microbiological and geophysical assessments of anaerobic immobilization of heavy metals. Bioremed. J. 2005, 9, 33–48. [Google Scholar]
- Nairn, J.J.; Shapiro, P.J.; Twamley, B.; Pounds, T.; Wandruszka, R.V.; Fletcher, R.T.; Williams, M.; Wang, C.; Norton, M.G. Preparation of ultrafine chalcopyrite nanoparticles via the photochemical decomposition of molecular single-source precursors. Nano Lett. 2006, 6, 1218–1223. [Google Scholar]
- Barton, P.B., Jr; Bethke, P.M. Chalcopyrite disease in sphalerite: Pathology and epidemiology. Am. Mineral. 1987, 72, 451–467. [Google Scholar]
- Saunders, J.A.; Kamenov, G.D.; Hofstra, A.H.; Unger, D.L.; Creaser, R.A.; Barra, F. “Forensic” geochemical approaches to constrain the source of Au-Ag in low-sulfidation epithermal ores. In Great Basin Evolution and Metallogeny; Proceedings of Geological Society of Nevada 2010 Symposium, Reno-Sparks, NV, USA, 14 May 2010; Steininger, R., Pennell, W., Eds.; Geological Society of Nevada: Reno-Sparks, NV, USA, 2011; pp. 693–700. [Google Scholar]
- Taran, Y.A.; Bernard, A.; Gavilanes, J.-C.; Africano, F. Native gold in mineral precipitates from high-temperature volcanic gases of Colima volcano, Mexico. Appl. Geochem. 2000, 15, 337–346. [Google Scholar] [CrossRef]
- Casadevall, T.; Ohmoto, H. unnyside Mine, Eureka mining district, San Juan County, Colorado; geochemistry of gold and base metal ore deposition in a volcanic environment. Econ. Geol. 1977, 72, 1285–1320. [Google Scholar] [CrossRef]
- Hough, R.M.; Noble, R.R.P.; Reich, M. Natural gold nanoparticles. Ore Geol. Rev. 2012, 42, 55–61. [Google Scholar]
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