Abstract

Metallic sublimates coated by sulfides and chlorides line the vesicle walls of mafic volcanic lava and bombs from Kīlauea, Vesuvius, Etna, and Stromboli. The metallic sublimates were morphologically and compositionally similar among the volcanoes. The highest concentrations of S and Cl occurred on the surface of the sublimates, while internally they had less than 1 wt % S and Cl in most cases, leading us to classify them as alloys. The major components of the alloys were Cu, Sn, Co, and Ag based on electron microprobe analyses and environmental scanning electron microscope element maps. Alloy element maps showed a covariance of Cu-Sn, while Co and Ag concentrations varied independently. Laser ablation-inductively coupled plasma-mass spectrometry analysis of matrix glass and melt inclusions in bombs from Stromboli showed appreciable amounts of Cu, Co, and Sn. We propose a model for the origin of the metallic grains, which involves syneruptive and posteruptive magma degassing and subsequent cooling of the basalt vesicles. During syneruptive vapor phase exsolution, volatile metals (Cu, Co, and Sn) partition into the vapor along with their ligands, S and Cl. The apparent oxygen fugacity (fO2) in these vapor bubbles is low because of the relative enrichment of the exsolved gas phase in H2 relative to H2O in silicate melts, due to the much higher diffusivity of the former in silicate melts. The high fH2 and low fO2 induces the precipitation of metal alloys from the vapor phase. Subsequently, the reducing environment in the vesicle dissipates as the cooling vapor oxidizes and as H2 diffuses away. Then, metal-rich sulfides (and chlorides) condense onto the outer surfaces of the metal alloy grains either due to a decrease in temperature or an increase in fO2. These alloys provide important insights into the partitioning of metals into a magmatic volatile phase at low pressure and high temperature.

Introduction

From their studies of the 1991 eruptive products of Mount (Mt.) Pinatubo (Philippines) and the giant Bingham Canyon porphyry Cu deposit in Utah, Hattori and Keith (2001) concluded that mafic magma was fundamental in delivering sulfur and chalcophile elements to overlying magma chambers and could contribute to the formation of economic deposits. K. Hattori (pers. commun., 2004) found preliminary evidence of vapor transport of Cu in bombs that had erupted from the Miyake-jima volcano only a few days earlier. To test these conclusions, fresh, recently erupted mafic magma needs to be examined from volcanoes worldwide. Consequently, we sampled active flows from the Pu‘u ‘Ō‘ō vent on Kīlauea volcano, Hawaii. In a preliminary report, Strand et al. (2002, p. 88) found that they had no magmatic sulfides but discovered “heterogeneous particles of Cu-Sn-Co alloys” in the vesicles. We have now examined bombs and flows from other active volcanoes, including Etna, Vesuvius, and Stromboli. Remarkably, as we report here, we found the same metallic alloys, with distinct compositional variations for each volcano, in vesicles from these diverse magmatic systems.

The following observations and experiments demonstrate that volcanic vapors (low-density aqueous fluids) can carry significant quantities of a variety of metallic elements and deposit them as alloys, sulfides, and chlorides. Volcanic eruptions and open-system degassing contribute large quantities of metals into the atmosphere (Meeker et al., 1991; Symonds and Reed, 1993; Hinkley et al., 1999; Allard et al., 2000). Fluid inclusion work provides evidence that the vapor phase is a major mobilizing agent for metals within volcanic systems (Williams-Jones and Heinrich, 2005; Simon et al., 2006; Zajacz and Halter, 2009; Landtwing et al., 2010; Zhai et al., 2018). Additionally, high-temperature, reduced volcanic gasses from fumaroles and their sublimates have been explored using silica tube condensation techniques at various volcanoes, including Merapi, Momotombo, Mt. St. Helens (Bernard et al., 1990; Nadeau et al., 2016), Colima (Taran et al., 2000), Kudryavy (Yudovskaya et al., 2006), and Satsuma-Iwojima (Hedenquist et al., 1994; Africano et al., 2002). At these volcanoes, Au-Cu alloys, Cu-Au-Ag alloys, Cu, Zn, Sn, and Fe sulfides, Cu-Fe sulfides, PbCl, BiCl, etc. formed sublimates on the walls of the gas collecting tubes. In addition, sublimates of many varieties, including native Cu and Au, AuCl, and Pb-BiS, have been found deposited inside and around fumaroles at Mt. Erebus (Meeker et al., 1991), Vulcano (Fulignati and Sbrana, 1998), and Kudryavy (Yudovskaya et al., 2006). These occurrences show that many ore metals are transported by magmatic vapor.

If these volatile metallic species are common constituents of volcanic gasses, what is their fate if they are trapped and condensed in the vesicles of cooling lava? Only a few researchers have found metallic sublimates lining vesicle walls by looking inside vesicles with a scanning electron microscope (SEM)—from submarine basalts by Moore and Chalk (1971) and Mathez (1976), and from Popocatépetl volcano by Larocque et al. (1998, 2008). Larocque et al. (2008) noted that the fine-grained vesicle coatings in lavas were similar to mineral assemblages that occur in high-sulfidation epithermal Au deposits and represent crystallization directly from a magmatic volatile phase during or soon after eruption. They speculated whether it would be possible to look at these delicate grains in thin sections and concluded that one would need special preparation techniques to preserve them.

We propose that our innovative technique for vacuum impregnating samples with epoxy before thin sectioning preserves these delicate grains. Using this sample preparation technique, we have found metallic alloys along with sulfide and chloride sublimates not previously characterized in active volcanic systems. The vesicle-hosted Cu-Sn-Co alloys provide significant new data on metal transport and precipitation from high-temperature magmatic vapors. We anticipate that they will be widely recognized in mafic lavas and scoria elsewhere.

Samples

In reconnaissance studies, we found metallic alloys in vesicles of mafic scoria and lava erupted from several volcanoes in Hawaii and Italy, including Vulcano, Mt. Etna, Stromboli, Vesuvius, Mauna Loa, Mauna Kea, and Kīlauea. In this study, we examined in detail 13 groups of samples from Kīlauea, Etna, Stromboli, and Vesuvius (Table 1). Flows, scoria, and bombs from thousands of years to minutes old were sampled in order to observe the effect of environmental interactions, such as rain and weathering, on sublimate presence. At Kīlauea, we collected fresh lava from 2005 surface breakouts above lava tubes fed from the Pu‘u ‘Ō‘ō vent. In 2005, we sampled from the 2002 and 2005 lava flows on Etna. Stromboli samples, also collected in 2005, consisted of golden pumice and scoria bombs from the 2002 to 2005 eruptive products. On Vesuvius, we collected from seven different eruptive units, with the most recent samples coming from the 1944 flow. The geology of each volcano is briefly described in the next section, and more detailed descriptions of sample types and locations are given in the Appendix text and

through .

Table 1.

Summary of Samples and Alloys Located in Thin Section

VolcanoRock typeEruptionAlloys present
KilaueaOlivine tholeiiteLava from the Pali (2005)20
  Two-day-old flow (2005)20
EtnaTrachybasaltScoria (2002)20
  Scoria (2005)19
StromboliPotassic trachybasaltPumiceous bomb (2005)33
 Golden pumicePumiceous bomb (2005)70
  Pumiceous bomb (2005)28
  Pumiceous bomb (2005)62
 Trachybasaltic andesiteScoriaceous bombs (2002)26
  Scoriaceous bombs (2002)2
  Scoriaceous bombs (2002)11
  Scoriaceous bombs (2002)14
VesuviusPhonolitic tephritesBasalt (1944)10
 Phonolitic tephritesScoria (1944)5
  Vesuvius (1913–1944)0
  Vesuvius (1913–1944)0
  Vesuvius (1906–1913)0
  Vesuvius (1906)0
 Tephritic leucititesVesuvius (1700 B.P.)0
  Vesuvius (1700 B.P.)0
  Vesuvius (1700 B.P.)0
  Vesuvius (1700 B.P.)0
  Vesuvius (1700 B.P.)0
VolcanoRock typeEruptionAlloys present
KilaueaOlivine tholeiiteLava from the Pali (2005)20
  Two-day-old flow (2005)20
EtnaTrachybasaltScoria (2002)20
  Scoria (2005)19
StromboliPotassic trachybasaltPumiceous bomb (2005)33
 Golden pumicePumiceous bomb (2005)70
  Pumiceous bomb (2005)28
  Pumiceous bomb (2005)62
 Trachybasaltic andesiteScoriaceous bombs (2002)26
  Scoriaceous bombs (2002)2
  Scoriaceous bombs (2002)11
  Scoriaceous bombs (2002)14
VesuviusPhonolitic tephritesBasalt (1944)10
 Phonolitic tephritesScoria (1944)5
  Vesuvius (1913–1944)0
  Vesuvius (1913–1944)0
  Vesuvius (1906–1913)0
  Vesuvius (1906)0
 Tephritic leucititesVesuvius (1700 B.P.)0
  Vesuvius (1700 B.P.)0
  Vesuvius (1700 B.P.)0
  Vesuvius (1700 B.P.)0
  Vesuvius (1700 B.P.)0

Geologic Settings

We examined mafic scoria and lava from hot spot (Hawaii) and subduction zone (Italy) settings. Below, we outline the characteristics of the volcanoes that relate to metal transport and deposition, the volcanoes’ eruptive behaviors, their volatile fluxes and degassing styles, and mafic injections in subvolcanic magma reservoirs, as well as the compositions and mode of emplacement of the materials studied.

Kīlauea

Kīlauea is a basaltic shield volcano on the southeastern flank of Hawaii that formed as a result of hot spot volcanism (Lipman et al., 2000). Basaltic magma rises beneath the central summit caldera, where, for the most recent eruptions, it intruded laterally into a rift zone, transferring magma to one or more vents on the surface (Poland et al., 2012). Eruptions are typically nonexplosive effusions into tube systems, but sometimes high fountains form when unusually volatile-rich magma erupts (Poland et al., 2012). Our samples were collected during a period of quiet effusions in 2005 from surface breakouts 10.5 km from the Pu‘u ‘Ō‘ō vent. Pu‘u ‘Ō‘ō erupted continuously from 1983 to 2018 (Poland et al., 2012; Neal et al., 2019). The lava we studied is an olivine tholeiite—the most common type of lava to erupt from Kīlauea (Table 1). However, mixed lava compositions have erupted periodically from Pu‘u ‘Ō‘ō and indicate that magma storage and differentiation occur within the rift (Conrad et al., 1997; Neal et al., 2019). Emission rates for SO2 and CO2 spiked from approximately 1,000 to 2,000 tons per day (tpd) to approximately 3,000 to 5,000 tpd in early 2005 when we were sampling the lava flow. This, along with other geophysical and geochemical observations, has led scientists to hypothesize a mantle-driven surge in magma supply to Kīlauea from 2003 to 2007 (Elias and Sutton, 2007; Poland et al., 2012).

Italian volcanoes

Etna, Stromboli, and Vesuvius are proposed to result from the subduction of the African plate margin beneath the European block (Scandone, 1979; De Natale et al., 2001). Such convergent plate magma sources are tied to many different types of hydrothermal metal deposits along with explosive eruptions.

Etna: Etna is a mafic stratovolcano on the island of Sicily. It is the most active volcano in Europe, and its quiescent, continuous gas release from summit craters and peripheral fumaroles make it one of the world’s largest continuous contributors of volcanic volatiles to the atmosphere (Allard et al., 1991, 1994; Ferlito et al., 2013). It erupts unusually alkaline lavas (including trachybasalts and basalts) for a volcano in a subduction setting. Some have linked the unusual characteristics to back-arc spreading (Cocchi et al., 2009). During Etna’s frequent periods of high activity, emissions as high as 23,000 tpd of SO2 and 40,000 tpd of CO2 occur (Allard et al., 1991). A study of olivine melt inclusions trapped in historical and recent alkali basalts discovered higher amounts of H2O, S, and Cl than in melt inclusions from older alkali basalts (Métrich et al., 1993). We sampled trachybasalt lava flows from a powerful flank eruption in 2002 and from effusive eruptions in 2005. The samples were collected about 3 km from the vent in 2005. The 2002 flank eruption was unique in that it brought volatile-rich alkali basalt up from the deep feeding system, as evidenced by the multidisciplinary data collected (Andronico et al., 2005). The 2005 effusive eruptions are also thought to have originated from the input of deeper, volatile-rich magma sources (Aiuppa et al., 2006).

Stromboli: Stromboli is an active stratovolcano located off the coast of Sicily that has erupted both calc-alkaline and alkaline magmas. Explosions are spaced from 20 min to a few hours apart and are caused by the accumulation of slugs of volatiles in the near-surface plumbing system. Its eruptive style is generally strombolian with effusive activity every 10 to 20 years interspersed with rare explosive paroxysms (Laiolo and Cigolini, 2006). This eruption style has been consistent for the last 14,000 to 18,000 years (Rosi et al., 2000). Métrich et al. (2001, 2010) proposed a model wherein the crystal-rich, degassed basaltic scoria is ejected in strombolian and effusive eruptions from an actively degassing magma in the cone of the volcano (100 MPa, about 3.5 km depth). In contrast, the explosive paroxysms eject high-K basalt characterized as “golden pumice” (crystal poor and volatile rich) from volatile-rich magma originating deeper in the volcano, at ~270 MPa and about 10 km deep, that rises quickly to the surface before it can substantially degas (Di Carlo et al., 2006). Francalanci et al. (2004) found evidence for mixing between the volatile-rich (golden pumice) and volatile-poor (scoria) magmas. Reversely zoned olivine and clinopyroxene and variable volatile concentrations in melt inclusions and matrix glass of the 2005 golden pumice also point to influences of magma mixing. We sampled golden pumice (potassic trachybasalt) erupted from a 2005 paroxysm as well as scoria bombs (trachybasaltic andesite) from more typical eruptions (Baxter, 2008). In addition to the volatile-driven explosions, degassing is continuous and releases 6,000 to 12,000 metric tons of H2O, CO2, SO2, HCl, and HF per day (Allard et al., 1994).

Vesuvius: Vesuvius, east of Naples, represents the southernmost active area of K-rich volcanism (leucite-bearing tephrites) in central Italy (Cioni et al., 2008). Although related to the presence of a continuously subducting slab (De Natale et al., 2001), erupted lavas are highly unusual for this setting and include a wide variety of silica-undersaturated magmas. It has a long history of Plinian and non-Plinian effusive eruptions (Belkin and De Vivo, 1993). Magma resides in shallow 1- to 5-km-deep reservoirs within the Mesozoic carbonate basement (De Natale et al., 2001). We collected scoriaceous lava from the surface of flows ranging from 1,700 years old to those erupted in 1944. The last eruption in 1944 was significant in that it transitioned from effusive eruptions of phonotephritic lavas to fountaining of porphyritic K-tephrites. The commonly believed cause for this eruptive transition is that a volatile-rich magma batch rose from a depth of 11 to 22 km and mixed with a higher-level magma, thus triggering the 1944 eruption (Marianelli et al., 1999).

Analytical Methods

Epoxy vacuum impregnation

Samples were vacuum impregnated with epoxy before being made into polished thin sections following the technique developed by Wagner Petrographic (Lehi, Utah). The samples were dried to prevent moisture from interfering and then submerged in a specially formulated, low-viscosity proprietary epoxy. The thin-section billets were placed in a vacuum chamber, and the pressure was reduced to 100 to 200 torr to remove air in the exposed vesicles and pore spaces. A vacuum was pulled until all the bubbles were removed. Pressure was then increased to 500 to 600 torr to overcome the surface tension of the epoxy and force it into the vesicles. Samples were then allowed to cure. This procedure has been found to preserve sublimates that are loosely attached to the vesicle wall, which would otherwise be lost in a standard thin-sectioning process.

Environmental SEM (ESEM) analysis of vesicles in rock fragments

To image and analyze the uncut sublimates attached to the vesicle walls, 28 whole-rock samples (2- to 5-cm pieces) were mounted on aluminum stubs, carbon coated, and explored using a Philips XL30 ESEM at Brigham Young University (BYU). The backscattered electron (BSE) detector was used to locate metallic sublimates and sulfides. Elements were identified using an energy dispersive X-ray analyzer (EDXA) Genesis system with a SiLi detector for semiquantitative analysis.

X-ray element maps of the thin sections of metallic sublimates were also obtained with the Philips XL30 ESEM. During analyses, an acceleration of 20 kV was used. Additionally, the ESEM was used to create detailed BSE photos of the alloys found in the thin section.

Electron microprobe analysis

Metallic sublimates in polished thin sections were analyzed on a Cameca SX50 electron microprobe. Light and dark portions of the metallic sublimate surface were analyzed using the conditions outlined in Appendix

. Many of the alloys are so thin that the analytical volume extended beyond the boundaries of these small grains (5–80 μm across). Consequently, many of the totals are low. We have reported the concentrations to two decimal places in Table 2, but the analyses should be considered to be semiquantitative.

Table 2.

Semiquantitative Electron Microprobe Analyses of Alloys from Kīlauea, Etna, Vesuvius, and Stromboli Volcanoes

Table 2A. Electron Microprobe Analyses of Alloys, Kīlauea (2005)
SampleKC-K8KC-K8Kh-K9Kh-K9Kh-K9Kh-K9Kh-K9Kh-K9Average
Si (wt %)0.020.070.050.050.235.230.050.170.74
S0.060.180.020.060.020.250.050.050.09
Cl0.000.000.040.070.020.050.200.030.05
Fe1.282.001.653.880.781.511.000.661.59
Co0.621.271.384.100.410.260.820.761.20
Ni0.020.020.010.020.010.010.010.010.01
Cu84.5878.1782.9175.7082.0370.7469.5864.6676.04
Zn0.040.020.010.040.030.060.040.030.03
As0.000.000.080.080.040.000.010.040.03
Pd0.040.000.010.000.000.050.000.010.01
Ag0.000.000.070.050.000.030.000.000.02
Sn13.1917.8913.5113.1815.3313.2717.0332.2516.96
Pt0.050.070.000.000.050.000.000.010.02
Au0.000.000.060.040.000.000.000.000.01
Hg0.000.010.080.000.000.040.000.020.02
Pb0.110.000.060.050.030.000.010.110.05
Total100.0199.6999.9197.3198.9691.4988.8098.8396.88
Table 2A. Electron Microprobe Analyses of Alloys, Kīlauea (2005)
SampleKC-K8KC-K8Kh-K9Kh-K9Kh-K9Kh-K9Kh-K9Kh-K9Average
Si (wt %)0.020.070.050.050.235.230.050.170.74
S0.060.180.020.060.020.250.050.050.09
Cl0.000.000.040.070.020.050.200.030.05
Fe1.282.001.653.880.781.511.000.661.59
Co0.621.271.384.100.410.260.820.761.20
Ni0.020.020.010.020.010.010.010.010.01
Cu84.5878.1782.9175.7082.0370.7469.5864.6676.04
Zn0.040.020.010.040.030.060.040.030.03
As0.000.000.080.080.040.000.010.040.03
Pd0.040.000.010.000.000.050.000.010.01
Ag0.000.000.070.050.000.030.000.000.02
Sn13.1917.8913.5113.1815.3313.2717.0332.2516.96
Pt0.050.070.000.000.050.000.000.010.02
Au0.000.000.060.040.000.000.000.000.01
Hg0.000.010.080.000.000.040.000.020.02
Pb0.110.000.060.050.030.000.010.110.05
Total100.0199.6999.9197.3198.9691.4988.8098.8396.88
Table 2B. Electron Microprobe Analyses of Alloys, Etna (2002)
SampleE9E9E9E9E9E9E9E9E9Average
Si (wt %)0.060.050.050.050.020.090.070.060.070.06
S0.150.140.130.170.050.130.190.100.110.13
Ag0.440.360.365.043.062.402.077.602.632.66
Sn2.122.270.2712.009.063.533.275.473.434.60
Fe0.140.160.110.150.150.110.100.110.130.13
Co80.1680.7678.977.1722.5875.0575.2256.2072.6560.97
Ni0.000.020.000.050.030.040.010.000.010.02
Cu13.0712.9215.0055.8445.8326.0019.7729.3316.9826.08
Total96.4896.6897.3280.4580.77107.35100.6898.8596.0294.65
Table 2B. Electron Microprobe Analyses of Alloys, Etna (2002)
SampleE9E9E9E9E9E9E9E9E9Average
Si (wt %)0.060.050.050.050.020.090.070.060.070.06
S0.150.140.130.170.050.130.190.100.110.13
Ag0.440.360.365.043.062.402.077.602.632.66
Sn2.122.270.2712.009.063.533.275.473.434.60
Fe0.140.160.110.150.150.110.100.110.130.13
Co80.1680.7678.977.1722.5875.0575.2256.2072.6560.97
Ni0.000.020.000.050.030.040.010.000.010.02
Cu13.0712.9215.0055.8445.8326.0019.7729.3316.9826.08
Total96.4896.6897.3280.4580.77107.35100.6898.8596.0294.65
Table 2C. Electron Microprobe Analyses of Alloys, Vesuvius (1944)
SampleV10-J8V10-J8V10-J8V10-J8V10-J8V10-J8V10-J8V10-J8V10-J8Average
Si (wt %)0.160.970.580.570.090.200.360.470.300.44
S0.080.090.110.090.320.110.120.120.110.13
Ag0.960.575.792.441.004.655.444.645.483.75
Sn4.301.912.332.855.511.372.102.902.082.63
Fe0.370.450.090.300.320.070.060.160.050.19
Co47.5154.4566.9556.3058.3482.5574.8363.2275.3066.49
Ni0.030.000.000.010.020.040.010.000.020.01
Cu36.3314.479.7820.1912.585.908.8612.397.8411.50
Zn0.000.070.040.040.090.000.000.020.000.03
As0.320.000.000.110.100.110.520.060.380.16
Pb0.000.040.140.060.000.130.100.080.110.08
Total90.0673.0085.8082.9578.3695.1392.4084.0491.9685.42
 V10-J8V10-J8V10-J8V10-J8V10-J8V10-J8V10-J8V10-k11bV10-k11bAverage
Si (wt %)0.070.060.100.070.060.060.060.120.130.08
S0.210.130.140.180.170.150.270.110.130.16
Ag0.061.231.730.311.062.051.470.090.080.90
Sn0.801.350.460.191.581.147.160.230.191.45
Fe0.360.350.290.370.230.180.290.070.180.26
Co88.1784.2274.3292.6081.5069.2360.6494.2494.0082.10
Ni0.000.000.030.000.120.010.070.030.100.04
Cu3.748.252.392.129.336.8014.782.132.065.73
Zn0.000.000.050.000.170.030.07NANA0.04
As0.190.150.100.000.360.010.00NANA0.12
Pb0.030.000.020.020.000.100.00NANA0.02
Total93.6295.7579.6195.8694.5879.7484.8197.0196.8790.91
Table 2C. Electron Microprobe Analyses of Alloys, Vesuvius (1944)
SampleV10-J8V10-J8V10-J8V10-J8V10-J8V10-J8V10-J8V10-J8V10-J8Average
Si (wt %)0.160.970.580.570.090.200.360.470.300.44
S0.080.090.110.090.320.110.120.120.110.13
Ag0.960.575.792.441.004.655.444.645.483.75
Sn4.301.912.332.855.511.372.102.902.082.63
Fe0.370.450.090.300.320.070.060.160.050.19
Co47.5154.4566.9556.3058.3482.5574.8363.2275.3066.49
Ni0.030.000.000.010.020.040.010.000.020.01
Cu36.3314.479.7820.1912.585.908.8612.397.8411.50
Zn0.000.070.040.040.090.000.000.020.000.03
As0.320.000.000.110.100.110.520.060.380.16
Pb0.000.040.140.060.000.130.100.080.110.08
Total90.0673.0085.8082.9578.3695.1392.4084.0491.9685.42
 V10-J8V10-J8V10-J8V10-J8V10-J8V10-J8V10-J8V10-k11bV10-k11bAverage
Si (wt %)0.070.060.100.070.060.060.060.120.130.08
S0.210.130.140.180.170.150.270.110.130.16
Ag0.061.231.730.311.062.051.470.090.080.90
Sn0.801.350.460.191.581.147.160.230.191.45
Fe0.360.350.290.370.230.180.290.070.180.26
Co88.1784.2274.3292.6081.5069.2360.6494.2494.0082.10
Ni0.000.000.030.000.120.010.070.030.100.04
Cu3.748.252.392.129.336.8014.782.132.065.73
Zn0.000.000.050.000.170.030.07NANA0.04
As0.190.150.100.000.360.010.00NANA0.12
Pb0.030.000.020.020.000.100.00NANA0.02
Total93.6295.7579.6195.8694.5879.7484.8197.0196.8790.91
 V10-k11bV10-k11bAverage
Si (wt %)0.150.860.50
S0.130.150.14
ClNA0.110.11
Ag0.050.000.02
Sn0.4413.356.90
Fe0.130.870.50
Co85.410.7243.06
Ni0.000.000.00
Cu3.3962.7933.09
ZnNA0.040.04
AsNA0.000.00
AuNA0.070.07
PbNA0.060.06
Total89.6879.0184.48
 V10-k11bV10-k11bAverage
Si (wt %)0.150.860.50
S0.130.150.14
ClNA0.110.11
Ag0.050.000.02
Sn0.4413.356.90
Fe0.130.870.50
Co85.410.7243.06
Ni0.000.000.00
Cu3.3962.7933.09
ZnNA0.040.04
AsNA0.000.00
AuNA0.070.07
PbNA0.060.06
Total89.6879.0184.48
Table 2D. Electron Microprobe Analyses of Alloys, Stromboli (2005)
 S1-K12S1-K12S1-K12S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6Average
Si (wt %)0.120.070.350.080.120.070.070.090.030.11
S0.110.150.230.130.040.260.140.120.080.14
ClNANANANANANANANANANA
Fe0.360.040.080.090.410.170.100.100.070.16
Co89.1795.9976.1495.9916.2286.1196.4197.3941.5977.22
Ni0.000.000.030.000.000.060.000.000.020.01
Cu4.142.242.521.9068.116.033.091.667.6110.81
ZnNANANANANANANANANANA
AsNANANANANANANANANANA
PdNANANANANANANANANANA
Ag0.700.521.580.022.640.080.150.0042.255.33
Sn0.850.360.820.1412.161.580.650.166.102.54
PtNANANANANANANANANANA
AuNANANANANANANANANANA
HgNANANANANANANANANANA
PbNANANANANANANANANANA
Total95.4599.3781.7398.3599.7194.36100.6299.5297.7596.32
 S5-K6S5-K8S5-K8S5-K8S5-K8S5-K8S5-K8S5-K8S5-K8Average
Si (wt %)0.040.100.070.050.140.060.380.040.140.11
S2.430.010.020.020.010.020.020.030.010.29
ClNA0.050.000.030.040.000.000.000.040.02
Fe0.291.521.090.911.251.241.202.141.251.21
Co1.531.200.720.420.911.041.072.570.911.15
Ni0.000.030.020.020.020.020.030.020.020.02
Cu68.5679.6880.7182.0477.4483.4479.2384.4977.4479.22
ZnNA0.020.020.070.060.020.050.030.060.04
AsNA0.050.000.060.160.020.030.500.160.12
PdNA0.000.040.000.000.000.000.010.000.01
Ag10.600.000.040.000.000.060.010.000.001.19
Sn11.6914.7814.5814.7414.2012.0915.899.2814.2013.49
PtNA0.000.000.000.000.000.040.050.000.01
AuNA0.000.020.110.000.000.000.000.000.02
HgNA0.050.000.000.000.020.020.010.000.01
PbNA0.030.000.010.000.000.120.150.000.04
Total95.1497.5297.3598.5094.2298.0198.0999.3394.2296.96
Table 2D. Electron Microprobe Analyses of Alloys, Stromboli (2005)
 S1-K12S1-K12S1-K12S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6Average
Si (wt %)0.120.070.350.080.120.070.070.090.030.11
S0.110.150.230.130.040.260.140.120.080.14
ClNANANANANANANANANANA
Fe0.360.040.080.090.410.170.100.100.070.16
Co89.1795.9976.1495.9916.2286.1196.4197.3941.5977.22
Ni0.000.000.030.000.000.060.000.000.020.01
Cu4.142.242.521.9068.116.033.091.667.6110.81
ZnNANANANANANANANANANA
AsNANANANANANANANANANA
PdNANANANANANANANANANA
Ag0.700.521.580.022.640.080.150.0042.255.33
Sn0.850.360.820.1412.161.580.650.166.102.54
PtNANANANANANANANANANA
AuNANANANANANANANANANA
HgNANANANANANANANANANA
PbNANANANANANANANANANA
Total95.4599.3781.7398.3599.7194.36100.6299.5297.7596.32
 S5-K6S5-K8S5-K8S5-K8S5-K8S5-K8S5-K8S5-K8S5-K8Average
Si (wt %)0.040.100.070.050.140.060.380.040.140.11
S2.430.010.020.020.010.020.020.030.010.29
ClNA0.050.000.030.040.000.000.000.040.02
Fe0.291.521.090.911.251.241.202.141.251.21
Co1.531.200.720.420.911.041.072.570.911.15
Ni0.000.030.020.020.020.020.030.020.020.02
Cu68.5679.6880.7182.0477.4483.4479.2384.4977.4479.22
ZnNA0.020.020.070.060.020.050.030.060.04
AsNA0.050.000.060.160.020.030.500.160.12
PdNA0.000.040.000.000.000.000.010.000.01
Ag10.600.000.040.000.000.060.010.000.001.19
Sn11.6914.7814.5814.7414.2012.0915.899.2814.2013.49
PtNA0.000.000.000.000.000.040.050.000.01
AuNA0.000.020.110.000.000.000.000.000.02
HgNA0.050.000.000.000.020.020.010.000.01
PbNA0.030.000.010.000.000.120.150.000.04
Total95.1497.5297.3598.5094.2298.0198.0999.3394.2296.96
Table 2E. Electron Microprobe Analyses of Alloys, Stromboli (2005)
 S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6Average
Si (wt %)0.080.020.030.060.060.020.080.070.120.06
S0.030.020.040.030.010.060.160.100.040.05
Cl0.010.010.000.000.030.000.040.000.010.01
Fe3.451.591.594.140.500.512.480.963.832.12
Co3.471.471.373.660.440.152.690.873.251.93
Ni0.000.010.040.030.010.010.010.030.020.02
Cu73.2380.3384.0276.8876.4789.7370.6178.2871.3977.88
Zn0.060.020.050.030.050.040.030.070.040.04
As0.000.120.000.000.130.290.050.270.000.10
Pd0.010.000.000.050.000.030.000.000.030.01
Ag0.000.010.000.040.000.000.000.000.050.01
Sn17.9514.2612.0014.4822.028.0022.6317.3619.2816.44
Pt0.000.000.000.000.000.000.000.040.000.00
Au0.000.050.000.000.000.010.000.030.000.01
Hg0.000.000.030.000.050.000.100.050.070.03
Pb0.000.000.090.010.130.040.000.000.000.03
Total98.2997.9199.2699.3999.8998.8898.8798.1398.1398.75
 S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6Average
Si (wt %)0.130.040.101.200.050.150.080.180.330.25
S0.020.020.020.030.060.010.000.000.000.02
Cl0.010.040.060.130.000.220.030.070.050.07
Fe1.281.711.741.329.111.031.371.532.442.39
Co0.891.621.571.0610.840.690.721.021.252.18
Ni0.020.020.020.030.020.030.010.030.010.02
Cu77.5678.7763.5860.7964.7758.7379.4977.2461.8969.20
Zn0.050.050.030.040.050.030.040.110.030.05
As0.000.000.320.040.000.340.010.070.000.09
Pd0.000.000.040.000.000.000.000.050.000.01
Ag0.010.030.000.000.030.010.070.000.000.02
Sn13.649.5722.6210.2711.2010.499.1513.1722.5313.63
Pt0.000.040.000.010.030.000.000.000.030.01
Au0.000.000.010.020.000.000.040.000.000.01
Hg0.070.010.000.000.010.000.040.030.000.02
Pb0.030.080.000.000.000.000.040.000.000.02
Total93.6992.0290.1074.9196.1671.7291.0893.4888.5687.97
Table 2E. Electron Microprobe Analyses of Alloys, Stromboli (2005)
 S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6Average
Si (wt %)0.080.020.030.060.060.020.080.070.120.06
S0.030.020.040.030.010.060.160.100.040.05
Cl0.010.010.000.000.030.000.040.000.010.01
Fe3.451.591.594.140.500.512.480.963.832.12
Co3.471.471.373.660.440.152.690.873.251.93
Ni0.000.010.040.030.010.010.010.030.020.02
Cu73.2380.3384.0276.8876.4789.7370.6178.2871.3977.88
Zn0.060.020.050.030.050.040.030.070.040.04
As0.000.120.000.000.130.290.050.270.000.10
Pd0.010.000.000.050.000.030.000.000.030.01
Ag0.000.010.000.040.000.000.000.000.050.01
Sn17.9514.2612.0014.4822.028.0022.6317.3619.2816.44
Pt0.000.000.000.000.000.000.000.040.000.00
Au0.000.050.000.000.000.010.000.030.000.01
Hg0.000.000.030.000.050.000.100.050.070.03
Pb0.000.000.090.010.130.040.000.000.000.03
Total98.2997.9199.2699.3999.8998.8898.8798.1398.1398.75
 S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6S5-K6Average
Si (wt %)0.130.040.101.200.050.150.080.180.330.25
S0.020.020.020.030.060.010.000.000.000.02
Cl0.010.040.060.130.000.220.030.070.050.07
Fe1.281.711.741.329.111.031.371.532.442.39
Co0.891.621.571.0610.840.690.721.021.252.18
Ni0.020.020.020.030.020.030.010.030.010.02
Cu77.5678.7763.5860.7964.7758.7379.4977.2461.8969.20
Zn0.050.050.030.040.050.030.040.110.030.05
As0.000.000.320.040.000.340.010.070.000.09
Pd0.000.000.040.000.000.000.000.050.000.01
Ag0.010.030.000.000.030.010.070.000.000.02
Sn13.649.5722.6210.2711.2010.499.1513.1722.5313.63
Pt0.000.040.000.010.030.000.000.000.030.01
Au0.000.000.010.020.000.000.040.000.000.01
Hg0.070.010.000.000.010.000.040.030.000.02
Pb0.030.080.000.000.000.000.040.000.000.02
Total93.6992.0290.1074.9196.1671.7291.0893.4888.5687.97

Notes: Low totals are due to the small sizes (5–80 μm) and variable thicknesses of the grains, which allows the electron beam to excite surrounding epoxy or vesicle wall; some analyses did not include all of the major elements

X-ray element maps were also generated with the electron microprobe. A beam scan was used with a magnification tailored to the size of the alloy and a beam current of 200 nA with a beam size of 10 μm. Dwell time was 50 ms with a definition of 256 × 256 pixels.

Whole-rock chemistry

For samples containing metallic sublimates, trace element analyses of whole rocks by commercial inductively coupled plasma-mass spectrometry (ICP-MS) were completed. Samples from each volcano were analyzed for base and precious metals at the Vancouver (Canada) ALS laboratory using a four-acid near-complete digestion. Uncertainties based on comparisons with the standards analyzed with the unknowns range from 5 to as much as 20% for the lowest concentrations. Au, Pt, and Pd were analyzed using fire assay fusion and inductively coupled plasma-atomic emission spectroscopy (ICP-AES). Sulfur was analyzed using a Leco furnace technique with an uncertainty of about 5% relative.

Laser ablation-ICP-MS (LA-ICP-MS) analyses

LA-ICP-MS analyses were conducted at the Magmatic and Ore-Forming Processes Research Laboratory at the University of Toronto, Canada. An Agilent 7900 quadrupole mass spectrometer attached to an NWR 193 UC laser ablation system was used to determine the trace element composition of the matrix glass and silicate melt inclusions in minerals. Sixteen unknown analyses were bracketed by two U.S. Geological Survey GSD-1g basalt glass standard analyses at the beginning and end of each analysis block. The instrument was tuned to oxide and doubly charged ion production rates of approximately 0.3% as monitored on ThO/Th and mass 21/42Ca count rates while ablating the NIST 610 standard glass. Data quantification was conducted using the software SILLS (Guillong et al., 2008). The total of the major element oxides was used as an internal standard. Ag and Au count rates were corrected for the contribution of polyatomic interferences (91Zr16O on 107Ag and 181Ta16O on 197Au). The production rate of these oxides was determined using natural zircon and rutile, which were ablated before and after each analysis block.

Results

Uncut vesicle-hosted metallic sublimates

Vesicles within the volcanic products of Kīlauea, Etna, Stromboli, and Vesuvius were imaged and analyzed for three-dimensional grains in situ using rock fragments in an ESEM. Numerous bright metallic phases containing Au, Ag, Cu, Sn, Co, Fe, S, Cl, Bi, Ba, Zn, Ni, Pb, and Ti decorated the vesicles. Minerals lining the vesicles were identified based on major element peaks in the EDXA spectra and are listed in Table 3. Examples of some of the sublimates imaged by BSE imaging are shown in Figure 1. Various textures, fine compositional zonation, and compositions similar to those described in other studies—from Popocatépetl by Larocque et al. (1998, 2008), Vulcano by Fulignati and Sbrana (1998), and Kudryavy by Yudovskaya et al. (2006)—of vesicle-lining minerals and fumarole sublimates indicated formation from a vapor phase trapped within the vesicle.

(A-X) Metal sublimates attached to the vesicle walls of pumice and scoria samples from Etna (A-F), Vesuvius (G-L), Stromboli (M-R), and Kīlauea (S-X) volcanoes. BSE images of vesicle-lining materials on broken rock surfaces. In BSE images, darker shades of gray represent glass and silicate minerals while metals are white and were identified based on EDXA spectra. Important surface coatings are labeled.

(A-X) Metal sublimates attached to the vesicle walls of pumice and scoria samples from Etna (A-F), Vesuvius (G-L), Stromboli (M-R), and Kīlauea (S-X) volcanoes. BSE images of vesicle-lining materials on broken rock surfaces. In BSE images, darker shades of gray represent glass and silicate minerals while metals are white and were identified based on EDXA spectra. Important surface coatings are labeled.

Table 3.

Outer Surface Composition of Metallic Sublimates in Vesicles

Etna (2002)Mt. Vesuvius (1949)Stromboli (2005)Kīlauea (2005)
Cu-AuBa sulfideFe-Cu sulfideBi-Cu
Cu-Fe sulfideFe-Ti oxidesFe-Cr-NiNi
Fe-Ti oxidesCu sulfideAuAu-Fe
Ba sulfideAuCuAg sulfideSn chlorideBi
Cu-FeCu-Fe OxidePb sulfideFe-Ti oxides
Cu-Fe-NiAu sulfideCu-Pb-ZnCu sulfide
Au sulfideAg-Sn-FeCu-Zn chlorideFe sulfide
Co-Zn-Fe sulfideFe sulfideSn-Fe chloride 
 Fe-Ni sulfideNa chloride (halite) 
 Sn chloride  
 Ag-Sn-Cu chlorosulfide  
 Cu-Fe sulfide  
Etna (2002)Mt. Vesuvius (1949)Stromboli (2005)Kīlauea (2005)
Cu-AuBa sulfideFe-Cu sulfideBi-Cu
Cu-Fe sulfideFe-Ti oxidesFe-Cr-NiNi
Fe-Ti oxidesCu sulfideAuAu-Fe
Ba sulfideAuCuAg sulfideSn chlorideBi
Cu-FeCu-Fe OxidePb sulfideFe-Ti oxides
Cu-Fe-NiAu sulfideCu-Pb-ZnCu sulfide
Au sulfideAg-Sn-FeCu-Zn chlorideFe sulfide
Co-Zn-Fe sulfideFe sulfideSn-Fe chloride 
 Fe-Ni sulfideNa chloride (halite) 
 Sn chloride  
 Ag-Sn-Cu chlorosulfide  
 Cu-Fe sulfide  

Etna’s 2002 eruptive products contained an abundance of Fe-Ti oxides and Cu-Fe sulfides within the vesicles. A 20-mm grain of Cu-Au alloy (Fig. 1A), which had a similar composition and anhedral rounded texture to fumarole sublimates from the Kudryavy volcano (Yudovskaya et al., 2006, 2008), was found. A CoZnFe sulfide grain (Fig. 1E) had a very similar size and euhedral texture, composed of randomly oriented blades similar to those pictured in vesicle sublimates from Popocatépetl (Larocque et al., 2008) and fumarole condensates from the Kudryavy volcano (Yudovskaya et al., 2006). The CuFe sulfide sublimates found at Etna (Fig. 1B, C) had compositions similar to those of the Cu-Fe sulfides reported by Larocque et al. (2008). A porous ball of Cu sulfide was found (Fig. 1D, F) from Etna that appeared to have beehive-shaped outgrowths containing Cu and possibly S, similar to those described by Mavrogenes et al. (2010).

The 1944 eruptive products from Vesuvius contained a mix of sulfide, sulfate, chloride, and oxide sublimates lining the vesicle walls. A Cu sulfide compound in the vesicles showed concentric layers indicative of nucleation and sequential deposition (Fig. 1J). The AgSnCuFeClS (Fig. 1H) and BaS (Fig. 1I, L) vesicle-lining sublimates were similar to the barite and FeCuSnS compounds from Popocatépetl (Larocque et al., 1998).

Bombs from a 2005 eruption at Stromboli contained a mix of chloride, sulfide, and native gold grains lining the vesicle walls. The 40-μm Au sublimate (Fig. 1P) had twisting lamellar plates and was very similar in appearance to lamellar aggregates of Au deposited from vapors on the sides of fumaroles and tube sublimates from the Kudryavy volcano (Yudovskaya et al., 2006, 2008).

The 2005 Kīlauea vesicles investigated had abundant FeTi oxides and fewer sulfide and native metal grains than the other volcanoes. FeTi oxides and Cu sulfides (Fig. 1S, V) were similar in composition and appearance to FeTi oxides and Cu sulfides located in vesicles at Popocatépetl by Larocque et al. (1998) using SEM.

Metallic sublimates in thin sections

The studied vesicles contained many oxide, sulfide, and chloride sublimates, as described above, in unpolished rock samples (Fig. 1). However, when the third dimension was examined by cross sectioning the sublimates, we found the interiors to be made of compositionally distinct metallic alloys. These alloys are generally hidden by the outer layer of sulfide and chloride sublimates (e.g., Fig. 2). No previous studies have reported on the internal composition and nature of these vesicle-lining alloys. Using epoxy vacuum-impregnated thin sections of the scoria or pumice samples, the small metallic sublimates lining the vesicle walls could be preserved, examined, and analyzed using microanalytical techniques.

Fig. 2.

BSE image of cross-sectioned alloy grain from Stromboli (see also Fig. 5) with element maps for Cu, Sn, Co, S, Cl, and Ag. The curved upper surface lies along a vesicle wall. This grain is predominantly Co. In low-Co areas, note the strong correlation of Cu and Sn. The highest concentrations of S and Cl occur on the outer surface of the grain (toward bottom of image), which was thinly coated with epoxy and left uncut.

Fig. 2.

BSE image of cross-sectioned alloy grain from Stromboli (see also Fig. 5) with element maps for Cu, Sn, Co, S, Cl, and Ag. The curved upper surface lies along a vesicle wall. This grain is predominantly Co. In low-Co areas, note the strong correlation of Cu and Sn. The highest concentrations of S and Cl occur on the outer surface of the grain (toward bottom of image), which was thinly coated with epoxy and left uncut.

The cut sublimates were easily located in thin sections under a microscope with 20× magnification in reflected light and are best classified as alloys because the anions present amounted to less than 1% in most cases (Table 2). We found alloys in thin sections from volcanic products collected at Kīlauea, Etna, Stromboli, and Vesuvius, as shown in Table 1. The alloys were found within vesicles usually detached from the wall and were a highly reflective yellow-gold color (Fig. 3). They range in size from a few to 150 μm. The alloys all had a similar appearance, with slight color differences showing variable compositions. Microprobe analysis (Table 2) constrained the compositional bands in the alloys (Fig. 4).

Fig. 3.

Metal alloys in reflected light in thin sections impregnated with epoxy. (A) Metal alloy grains are attached to a vesicle wall (Stromboli). (B) Most of the alloys are detached from the wall but some are still in place (Vesuvius). (C) In places, the alloys are found among broken fragments that settled to the inferred bottom of the vesicle (Kīlauea). (D) Rarely, the alloys are found in fractures leading away from vesicles (Stromboli). (E) Metal alloy with heterogeneous composition evident in reflected light (Etna). (F) Alloys commonly have convex surfaces that follow the contours of the vesicle even where they are detached from the wall (Vesuvius).

Fig. 3.

Metal alloys in reflected light in thin sections impregnated with epoxy. (A) Metal alloy grains are attached to a vesicle wall (Stromboli). (B) Most of the alloys are detached from the wall but some are still in place (Vesuvius). (C) In places, the alloys are found among broken fragments that settled to the inferred bottom of the vesicle (Kīlauea). (D) Rarely, the alloys are found in fractures leading away from vesicles (Stromboli). (E) Metal alloy with heterogeneous composition evident in reflected light (Etna). (F) Alloys commonly have convex surfaces that follow the contours of the vesicle even where they are detached from the wall (Vesuvius).

Fig. 4.

BSE images of vesicle walls and Cu-Sn-Co alloys in epoxy vacuum-impregnated thin sections of basalt. (A) Metal alloy grains are commonly contoured the same as the vesicles that contain them (Stromboli). (B) A BSE image of an alloy showing compositional variation (Stromboli). (C) Alloy with convex surfaces, which follow the contours of the vesicle wall, and a cockscomb texture, which is common and visible depending on the orientation in which the grain was cut (Vesuvius). (D) Alloys commonly float in the epoxy—a consequence of separation from the vesicle after growth and perhaps during thin-section preparation (Stromboli). (E) Alloy showing light and dark compositional bands (Etna). (F) Alloy detached from vesicle wall (Stromboli). (G) Alloy floating in epoxy within vesicle (Stromboli). (H) Alloy floating in epoxy within vesicle (Stromboli). (I) Alloy showing light and dark compositional bands surrounded by epoxy in vesicle (Vesuvius).

Fig. 4.

BSE images of vesicle walls and Cu-Sn-Co alloys in epoxy vacuum-impregnated thin sections of basalt. (A) Metal alloy grains are commonly contoured the same as the vesicles that contain them (Stromboli). (B) A BSE image of an alloy showing compositional variation (Stromboli). (C) Alloy with convex surfaces, which follow the contours of the vesicle wall, and a cockscomb texture, which is common and visible depending on the orientation in which the grain was cut (Vesuvius). (D) Alloys commonly float in the epoxy—a consequence of separation from the vesicle after growth and perhaps during thin-section preparation (Stromboli). (E) Alloy showing light and dark compositional bands (Etna). (F) Alloy detached from vesicle wall (Stromboli). (G) Alloy floating in epoxy within vesicle (Stromboli). (H) Alloy floating in epoxy within vesicle (Stromboli). (I) Alloy showing light and dark compositional bands surrounded by epoxy in vesicle (Vesuvius).

The alloys have never been found on lava surfaces or in the matrix glass but almost always in vesicles found in both glassy and crystallized matrices. Rarely, the alloy grains are found in fractures surrounding the vesicles (Fig. 3D). The alloy grains are commonly found directly adjacent or attached to the vesicle wall, and the curvature of the alloy usually matches that of the nearby vesicle wall (Fig. 3E, F). This suggests that the alloys were originally attached to the vesicle wall and grew into the interior of the vesicle. Many of them became detached from their original growth surface either due to shrinkage of the vesicle (or expansion of the wall) during cooling or during sample collection and preparation (Fig. 3E, F).

Morphology of metallic sublimates

Metallic sublimates come in many shapes (Fig. 4) depending on how the three-dimensional grain was cross sectioned (Fig. 5). Generally, the euhedral sulfides, chlorides, and oxides that decorate the outer surfaces of the sublimates have very distinctive compositions and shapes and are not easily confused with metal alloys.

Fig. 5.

This BSE image shows how the unique geometry of the cut alloys relates to the three-dimensional grain structure of uncut sublimates lining the vesicle walls.

Fig. 5.

This BSE image shows how the unique geometry of the cut alloys relates to the three-dimensional grain structure of uncut sublimates lining the vesicle walls.

Compositions of metal alloys

The internal structure and compositions of metal alloys from each of the investigated volcanoes were analyzed using both an electron microprobe and ESEM. Internally, the alloys showed compositional banding. Microprobe spot analyses within a single grain yield substantially different compositions, which we interpret to be the result of exsolution on the submicrometer scale. Nevertheless, multiple spot analyses of alloys on the microprobe (Table 2), element maps from the microprobe (Fig. 6), and from the ESEM (Figs. 2, 7, 8) revealed three major exsolved components—Co, Cu-Sn, and Ag. Maximum abundances (in wt %) of other trace or minor elements analyzed on the electron microprobe were Fe (3.0), Zn (0.11), As (0.50), Pd (0.05), Pt (0.05), Au (0.05), Hg (0.10), and Pb (0.13), as shown in Table 2.

Fig. 6.

Microprobe X-ray element maps of a vesicle-lining alloy from Etna’s 2002 lava flow. Cu-rich portions are Sn and Ag rich and Co poor.

Fig. 6.

Microprobe X-ray element maps of a vesicle-lining alloy from Etna’s 2002 lava flow. Cu-rich portions are Sn and Ag rich and Co poor.

Fig. 7.

BSE image of cross-sectioned alloy grain from Kīlauea with EDXA element maps for Cu, Sn, Co, Fe, and S. Images collected from a thin section of an epoxy-impregnated sample. The curved upper surface lies along a vesicle wall. This grain is predominantly composed of two or more exsolved bronze alloys.

Fig. 7.

BSE image of cross-sectioned alloy grain from Kīlauea with EDXA element maps for Cu, Sn, Co, Fe, and S. Images collected from a thin section of an epoxy-impregnated sample. The curved upper surface lies along a vesicle wall. This grain is predominantly composed of two or more exsolved bronze alloys.

Fig. 8.

BSE image of cross-sectioned alloy grain from Vesuvius with element maps for Cu, Sn, Co, Fe, Ag, and S. This grain is predominantly Co. In low-Co areas, note the strong correlation of Cu and Sn. Fe is detected in the rind surrounding the alloy. The highest concentrations of S and Cl occur in a sulfide- and chloride-rich crust that can be seen in the brighter portions of the grain.

Fig. 8.

BSE image of cross-sectioned alloy grain from Vesuvius with element maps for Cu, Sn, Co, Fe, Ag, and S. This grain is predominantly Co. In low-Co areas, note the strong correlation of Cu and Sn. Fe is detected in the rind surrounding the alloy. The highest concentrations of S and Cl occur in a sulfide- and chloride-rich crust that can be seen in the brighter portions of the grain.

An element map of an alloy grain from a 2005 Kīlauea lava flow displays at least two exsolved bronze components: one Sn rich (5–13 wt %) and the other Sn poor (<5 wt %) (Fig. 7). Microprobe spot analyses suggest considerable variability in the ratio of Cu to Sn (or our inability to resolve each exsolved region during analysis).

A BSE image of an alloy grain from a 2005 pumiceous bomb from Stromboli shows an uncut surface down in the epoxy that represents the alloy’s outer growth surface (Fig. 2). This outer surface had higher concentrations of S and Cl than the interior of the grain.

A BSE image of an alloy grain from the 1944 flows on Vesuvius with ESEM element maps for Cu, Sn, Co, Fe, Ag, and S is shown in Figure 8. This grain was predominantly composed of Co, but it is remarkably rich in Ag as well. In low-Co areas, Cu and Sn are strongly correlated. Fe was concentrated in the material coating the alloy grains. The highest concentrations of S and Cl occurred on the brighter portions of the grain that appeared to have a rough texture, which may be representative of an uncut surface thinly coated with epoxy.

The relative abundances of these three components (Co, Cu-Sn, Ag) varied substantially in alloys from the four volcanoes studied. Remarkably, the alloys located in the Kīlauea lava samples were morphologically similar but compositionally distinct from the alloys found in the volcanic products of Vesuvius, Etna, and Stromboli (Fig. 9). Kīlauean alloys were predominantly Cu-Sn (bronze) with little Co and Ag. There is a systematic decrease in the bronze component and an increase in Co in grains from Stromboli to Etna to Vesuvius (Fig. 9). Average Ag abundances peaked at about 3% in Etna and Stromboli samples.

Fig. 9.

Comparison of Italian and Hawaiian alloy compositions from electron microprobe analysis in weight percent. Kīlauea grains are Cu-Sn rich and Co poor.

Fig. 9.

Comparison of Italian and Hawaiian alloy compositions from electron microprobe analysis in weight percent. Kīlauea grains are Cu-Sn rich and Co poor.

Metal concentrations in melt inclusions and matrix glasses from Stromboli bombs

LA-ICP-MS analyses were acquired for the melt inclusions and matrix glasses in pumiceous and scoriaceous bombs from Stromboli, providing information on the abundance of the metals. The analyses showed high concentrations of Cu in the scoriaceous bombs (groundmass glass: 187 ppm [±25, 1 standard deviation], melt inclusions: 189 ppm [±56]) and pumiceous bombs (groundmass: 121 ppm [±12], melt inclusions: 124 ppm [±68]). Cobalt was also abundant in the scoriaceous bombs (groundmass: 25 ppm [±1], melt inclusions: 25 ppm [±2]) and pumiceous bombs (ground mass: 31.0 ppm [±0.2], melt inclusions: 22 ppm [±3]), and the analyses showed a few parts per million of Sn (

, ).

Distribution of metal alloys

The vesicles in the 2005 bombs from Stromboli hosted the largest and most abundant alloys found in our study. In order to better understand the distribution of these alloys in individual samples, the size and number of alloy grains were measured in thin sections under reflected light from both the crystallized interiors and the glassy rinds of two types of bombs (pumiceous and scoriaceous) from Stromboli (Fig. 10). The alloy grains range in size from ~2 to 150 μm across. The size distributions were skewed to the right (non-normal distribution), so the Wilcoxon rank-sum test (Keller, 2001) was used to determine if the alloy grain sizes and abundances in the volatile-rich pumiceous bombs were statistically distinct from the degassed scoriaceous bombs. Although the sample size is small, most sample pairs indicated strong evidence that the pumiceous bombs contained more metal alloys of a larger size than the scoriaceous bombs (Fig. 10). The Wilcoxon rank-sum test was also used to compare the alloys in the slowly cooled, crystallized interior of the bombs to those in the quenched, glassy rinds. The crystallized interiors of both types of bombs contained more alloy grains than the glassy rinds. However, the test indicated that the size distributions of the alloy grains in the bomb interiors were not statistically different from those in the crystallized rinds. This could mean that the processes forming the metal alloys in the crystallized interior of the bomb were the same as the processes forming metal alloys in the glassy rind, the only difference being the abundance of grains (Fig. 11).

Fig. 10.

For samples from Stromboli, the number of metal alloy grains in a thin section were classed by the largest dimension of the grain. (A) The number of alloy grains in the pumiceous bombs depends on the location. The more slowly cooled, crystallized interior of the bomb contains more alloy grains than the quenched glassy rind. (B) The number of alloys found in the scoriaceous bombs also depends on the location inside the bomb. The Wilcoxon rank-sum test indicated that there was no evidence that size distributions of the alloy grains from the bomb interiors were statistically different from those in the crystallized rinds. When comparing areas of pumiceous bombs to the same areas of the scoriaceous bombs, it is apparent that the pumiceous bombs contain more alloys of a larger size.

Fig. 10.

For samples from Stromboli, the number of metal alloy grains in a thin section were classed by the largest dimension of the grain. (A) The number of alloy grains in the pumiceous bombs depends on the location. The more slowly cooled, crystallized interior of the bomb contains more alloy grains than the quenched glassy rind. (B) The number of alloys found in the scoriaceous bombs also depends on the location inside the bomb. The Wilcoxon rank-sum test indicated that there was no evidence that size distributions of the alloy grains from the bomb interiors were statistically different from those in the crystallized rinds. When comparing areas of pumiceous bombs to the same areas of the scoriaceous bombs, it is apparent that the pumiceous bombs contain more alloys of a larger size.

Fig. 11.

Model of the processes at Stromboli that may be involved in the formation of the metal alloy grains. The pumiceous bombs rich in metal alloys likely originate from a deeper magma that is more primitive and volatile rich. The scoriaceous bombs (alloy poor) originate from a shallower magma that is relatively degassed. (A) When the bombs are erupted, volatiles and the metals they complex with (metal-rich sulfides and chlorides) move toward inflating vesicles. (B) During cooling, the metals are reduced (perhaps by the addition of H2 gas) to form the metal alloy grains; H2S and HCl (products of the reducing reactions) fill the vesicle. (C) Eventually, the reducing environment in the vesicle disappears as H2 is consumed. Then, the excess metal-rich sulfides (and chlorides) condense onto the outer surface of the metal alloys. Pressure of scoria magma from Métrich et al. (2001). Pressure of golden pumice magma and temperature from Di Carlo et al. (2006).

Fig. 11.

Model of the processes at Stromboli that may be involved in the formation of the metal alloy grains. The pumiceous bombs rich in metal alloys likely originate from a deeper magma that is more primitive and volatile rich. The scoriaceous bombs (alloy poor) originate from a shallower magma that is relatively degassed. (A) When the bombs are erupted, volatiles and the metals they complex with (metal-rich sulfides and chlorides) move toward inflating vesicles. (B) During cooling, the metals are reduced (perhaps by the addition of H2 gas) to form the metal alloy grains; H2S and HCl (products of the reducing reactions) fill the vesicle. (C) Eventually, the reducing environment in the vesicle disappears as H2 is consumed. Then, the excess metal-rich sulfides (and chlorides) condense onto the outer surface of the metal alloys. Pressure of scoria magma from Métrich et al. (2001). Pressure of golden pumice magma and temperature from Di Carlo et al. (2006).

Discussion

To explain the genesis of the metal precipitates, the following key questions need to be answered: (1) How were the metals transported into the inflating vesicles? (2) Why was this specific set of metals enriched in the fluid phase filling the vesicles? (3) Why did the metals precipitate in elemental form as alloys rather than as metal sulfides or oxides? In the following sections we address these points, first by considering metal transport into the vesicles and then by providing a hypothesis that explains the occurrence of the metallic precipitates.

The role of Cl and S in the solubility and transportation of metals

Separation of magmatic volatiles and the portioning of metals into an aqueous phase may occur over a broad range of depths (van Hinsberg et al., 2016). The magmatic volatile phase (MVP) and associated metals can rise through low-viscosity magma or may be transported via magma convection followed by escape to the atmosphere during open-system degassing. We suggest that early formed volatile phases are not the ones trapped in vesicles, the condensation products of which are examined here, because these would likely have sufficient concentrations of H2S to stabilize metal sulfide rather than metal alloys, due to the strong partitioning of reduced S species into the fluid phase at subvolcanic depths, even from mafic melts (Zajacz et al., 2012a, 2013). Rather, the vesicles formed during rapid decompression during or after eruption. As syneruptive formation of vesicles is a rather fast process, both equilibrium thermodynamics and the kinetics of the mass transfer processes must be considered when trying to understand the transfer of elements into the vesicles. First, we focus on the equilibrium partitioning aspect.

Copper, Sn, Ag, and Au are known to be extracted from magmas by exsolving volatiles, which are major contributors to the metal budgets of magmatic hydrothermal deposits. Unfortunately, very little is known about the partitioning behavior of Co between silicate melts and the MVP, and it is not commonly analyzed in magmatic fluid inclusions. Therefore, we focus our discussion on Cu, Sn, Ag, and Au.

Cu, a major component of most metal alloys described in this study, is known to form stable complexes with both chloride- and sulfur-bearing ligands in magmatic volatiles (Candela and Holland, 1984; Williams et al., 1995; Etschmann et al., 2010; Zajacz et al., 2011; Mei et al., 2013). At a temperature similar to that of the erupted magmas studied here but a higher pressure, Zajacz et al. (2011) concluded that Cu forms stable bisulfide and chloride complexes, with the latter being more significant at the weight percent level of dissolved chloride concentrations. Similarly, studies conducted at lower-temperature hydrothermal and ambient conditions concluded that Cu hydrosulfide complexes predominate only at low temperature and relatively high S/Cl ratios in the fluid phase (Mountain and Seward, 1999, 2003; Louvel et al., 2017). At lower temperatures but more closely matching fluid (vapor) density, Migdisov et al. (2014) found CuCl complexes to be stable and Cu solubility to be an exponential function of fH2O partial pressure due to increasing hydration numbers with increasing fH2O. Direct fluid/melt partitioning experiments also concluded that both S and Cl may play a role in Cu extraction from magmas (Candela and Holland, 1984; Williams et al., 1995; Simon et al., 2006). The most relevant fluid/melt partition coefficients for mafic magmas were estimated by Zajacz et al. (2012b), who proposed modest Cu partitioning into the MVP (DCufluid/melt~12); however, these numbers were estimated for pressure in subvolcanic magma reservoirs.

The relative enrichment of Au in the alloys compared to the host magma was even higher than that of Cu. Gold in the alloys from Stromboli had a concentration of about 0.01 wt % on average (Table 2) versus 0.001 ppm in the whole rock (

), with an enrichment factor of about 100,000. Copper in the alloys from Stromboli had a concentration of about 60 wt % versus 84 ppm in the whole rock, with an enrichment factor of about 7,000. Just like Cu, Au is known to form complexes with both S and Cl in high-temperature, aqueous fluids. However, the stability of complexes formed with sulfur-bearing ligands is much higher than those with chloride in most hydrothermal fluids (Williams-Jones et al., 2009) and even in high-temperature, relatively low density magmatic vapors (Zajacz et al., 2010). Indeed, Zajacz et al. (2012b) proposed DAufluid/melt up to ~200 for mafic magmas at fO2 less than the Ni-NiO buffer (NNO). This may have contributed to the observed relative enrichment of Au being higher than that of Cu.

Silver shows transitional behavior between Cu and Au, because both bisulfide and chloride complexes may play an important role in its solubility in magmatic fluids (Yin and Zajacz, 2018). Simon et al. (2008) determined that Ag partitions ~100 times more strongly into the fluid phase than Na in an S-free rhyolite melt-aqueous vapor/brine system, and Ag shows increasing preference for the fluid phase with decreasing pressure. Unfortunately, to our knowledge, no fluid/melt partitioning experiments have been done on Ag using S-bearing fluids.

Very few experimental data exist to assess whether Sn may have efficiently degassed from mafic magmas, as the available studies are restricted to S-free and predominantly chloride-or fluoride-bearing felsic systems (Keppler and Wyllie, 1991; Duc-Tin et al., 2007; Hu et al., 2008, 2009). These studies reported DSn fluid/melt in the range of 0 to 10, with generally increasing values with increasing Cl concentration, which was consistent with the data obtained from coexisting natural fluid and melt inclusions (Zajacz et al., 2008). Additionally, Sn oxides are known to be rather volatile at high temperatures (Lamoreaux et al., 1987; Migdisov and Williams-Jones, 2005). Therefore, though no quantification is possible, our observations suggest that Sn may degas not only from felsic magmas but also from mafic magmas, at least at relatively low pressures.

All things considered, it is apparent that Cu, Au, Ag, and Sn tend to partition into the MVP; however, no experiments resemble the pressure-temperature-composition (P-T-X) conditions of the vesicle formation in the studied mafic magmas closely enough to allow a quantitative estimation of the equilibrium metal concentrations in the gas phase. It is also evident that the presence of either chlorine or sulfur is required to facilitate the transfer of the metals into the volatile phase for most of the metals considered.

Formation of metal alloys

Perhaps the most intriguing feature of the precipitates in the vesicles was that the metals were present in their native form and were coated with only a thin layer of sulfides or oxides (Fig. 5), as opposed to the oxides and sulfides that dominate magmatic-hydrothermal ore deposits and high-temperature condensates of fumarolic gases in silica tubes (Bernard et al., 1990; Hedenquist et al., 1994; Taran et al., 2000; Africano et al., 2002; Yudovskaya et al., 2006). This observation indicates that the fugacities of oxygen and sulfur in the vesicles of the studied rocks were lower in the gas phase than during subvolcanic, quiescent degassing.

To put constraints on maximum oxygen and sulfur fugacities in the vesicles, we conducted thermodynamic calculations to predict the phase boundaries between native metals, metal oxides, and metal sulfides. The calculations were done for the Cu and Co end-member systems, because these are the two most abundant metals in the alloys. We assumed either 1 or 30 bar as end-member internal pressures, because the low viscosities of these mafic melts would likely not allow the buildup of much higher pressure in the vesicles after eruption.

In Figure 12, we show the phase diagram calculated from basic thermochemical data. It is apparent that the mole fraction of S allowed to be present in the volatile phase without stabilizing metal sulfides is dependent on oxygen fugacity (with a minimum at the H2S to SO2 transition), temperature, and pressure. The effect of pressure is mainly due to the fact that higher pressure yields higher fH2O, which shifts the SO2 + H2O = H2S + 1.5O2 reaction to the right. It is apparent that the presence of metallic Cu is feasible over a very wide range in fO2, as the Cu-Cu2O buffer reaction is only at about fO2 = NNO + 4. However, over much of the fO2 range, only 0.01 to 1.00 mol % of S was allowed to be present in the gas phase, except at above NNO + 1, which is a more oxidizing condition than that of most magmas studied here. The absence of CoS0.89 allowed for a somewhat higher concentration of S in the volatile phase than the absence of Cu2S, again with the values strongly dependent on fO2, with a minimum at about NNO – 1.5. The maximum concentration of S outside the sulfide stability field decreased about one order of magnitude in response to a temperature drop from 1,100° to 900°C in both systems. This is consistent with the observed narrow sulfide overgrowth on some of the alloy grains.

Fig. 12.

The stability of various (A) Cu and (B) Co compounds as a function of fO2 and the mole fraction of S in the gas phase. Thermochemical data from Barin et al. (1977) were used to predict equilibrium constants for the participating chemical reactions. We assumed fugacity coefficients of 1 for all gases, which is reasonable considering the low density of the gas phase. In addition, a water vapor mole fraction of 0.8 was assumed. The stability fields of metal sulfides with higher S to metal ratios (e.g., CuS) as well as the stability of sulfate compounds fall outside the shown fO2 and XS range.

Fig. 12.

The stability of various (A) Cu and (B) Co compounds as a function of fO2 and the mole fraction of S in the gas phase. Thermochemical data from Barin et al. (1977) were used to predict equilibrium constants for the participating chemical reactions. We assumed fugacity coefficients of 1 for all gases, which is reasonable considering the low density of the gas phase. In addition, a water vapor mole fraction of 0.8 was assumed. The stability fields of metal sulfides with higher S to metal ratios (e.g., CuS) as well as the stability of sulfate compounds fall outside the shown fO2 and XS range.

The allowed range of S concentrations without the stabilization of metal sulfides was somewhat lower than what is typically found in syneruptive gases discharged by mafic volcanoes (Williams-Jones and Heinrich, 2005). This mismatch may be explained by kinetic limitations. The diffusivity of S in the silicate melt is about four orders of magnitude lower than that of H2O (Baker et al., 2005; Freda et al., 2005; Zhang et al., 2010), and therefore it is likely that during rapid syneruptive vesicle growth, the amount of S effectively transferred to the gas phase is less than expected from equilibrium partitioning (Su et al., 2016). The higher total concentration of S in volcanic gases is likely due to the onset of volatile exsolution at depth before the eruption, resulting in a population of more S-rich bubbles in the magma, the rise of which has been proposed to explain the excess sulfur phenomenon in volcanic eruptions (Westrich and Gerlach, 1992; Wallace and Gerlach, 1994; Pasteris, 1996). However, because of their small sizes and closed outlines, the vesicles studied here are thought to have nucleated only during eruption and emplacement.

In addition to S, Cl may promote the transfer of most metals found in the precipitates into the exsolving volatile phase. The diffusivity of chlorine in silicate melts is about two to three orders of magnitude higher than that of S and only one to two orders of magnitude lower than that of water (Freda et al., 2005; Alletti et al., 2007; Zhang et al., 2010). This suggests that during rapid syneruptive degassing, it is feasible that the volatile phase filling the vesicles is characterized by much higher Cl/S ratios than equilibrium partitioning would dictate. Although the partition coefficient for Cl between magmatic volatiles and mafic-intermediate melts is generally <5 even at subvolcanic pressures (Stelling et al., 2008; Alletti et al., 2009; Zajacz et al., 2012a), this, combined with the measured Cl concentrations, still predicts thousands of parts per million Cl in the volatile phase. Considering the small volume fraction of alloy grains in the vesicles, it is conceivable that this amount of Cl along with the relatively low S concentrations was sufficient to extract the metals from the silicate melt.

Assuming a typical vesicle diameter of 1 mm and a pure Cu sublimate (or summation of grains) that is 2 × 10 × 20 μm in size, the concentration of Cu in a vapor that completely filled the vesicle would have only been 7 ppm. The vapor/melt partition coefficients found by Simon et al. (2006) for Cu were 316 (±22) for an S-bearing rhyolite and 63 (±31) for an S-free system, which, combined with a whole-rock concentration of 100 ppm of Cu, would yield an equilibrium value of about 6,300 to 31,600 ppm of Cu in a magmatic vapor. Thus, the metal concentrations in vapors implied by typical sizes are not excessive. Closed-system partitioning of Cu into a vapor appears feasible.

When discussing kinetically limited degassing, one must also consider the diffusivities of the metals themselves. Using the compilation by Zhang et al. (2010) on element diffusivities in silicate melts, our best estimates for a nearly anhydrous mafic melt at around 1,100°C expressed in m2/s are as follows: lnDSn ≈ –28, lnDPb ≈ –28, lnDCo ≈ –26, lnDZn ≈ –26, lnDAg ≈ –23, and lnDCu ≈ –21. As no experimental data is available for Cu and Ag, these values were estimated by using analogy to Na and Li, respectively, based on the identical charge and nearly equal ionic radius of Ag+/Na+ and Cu+/Li+ pairs. These values were higher overall than the estimated value for S (lnDs ≈ –30 m2/s) but partly overlapped with that of Cl (lnDCl ≈ –25.5 m2/s). Therefore, it is conceivable that the metals and Cl are simultaneously transferred into the gas phase while S lags behind. Absolute concentrations, of course, would depend on the composition of the melt.

However, it appears that diffusion-limited mass transfer does not explain separation between chloride-complexed elements that occur as (Cu, Ag, Co) alloys and those (Pb, Zn, Fe) that form sublimates coating the alloys (Table 1). One must consider not only the transfer of the metals into the gas phase but also their precipitation mechanism. Metal precipitation is likely induced by decreasing temperature, pressure, and potentially fO2. Unfortunately, there is not sufficient experimental data to put any quantitative constraints on the effect of pressure and temperature on the solubility of the metals of interest at the relevant conditions. Overall, metal solubility decreases with decreasing fO2, because the metals first need to be dissolved in a fluid phase, independent of the complex-forming ligands. In the case of chloride complexes, the dissolution reaction can be generalized as follows:

 

M(s)+HCl(g)=MCln(g)+n/2H2(g),
(1)

where M stands for metal with a valence state of n. The value of fH2 is inversely linked to fO2 through the water decomposition reaction.

It is clear from equation (1) that increasing fH2 and therefore decreasing fO2 will promote metal precipitation. In a magma, fO2 is mostly imposed by the ratio of heterovalent elements in various oxidation states, most notably Fe2+/Fe3+ ratios, whereas fH2 will be controlled by fH2O and fO2. Hydrogen is known to diffuse faster than H2O in silicate melts (Zhang and Ni, 2010), and therefore it is conceivable that upon fast vesicle growth, hydrogen is preferentially enriched in the vesicle relative to H2O, while the Fe3+/Fe2+ ratio increases in the residual silicate melt. As the gap between the diffusivity of H2 and H2O increases with decreasing temperature, it may be possible that H2/H2O ratios increase with decreasing temperature in the gas phase trapped in the vesicles, which may promote metal precipitation.

The changes in oxidation state do not need to be large (Fig. 12), and thus the vapor would not need to be pure H2 but just have an elevated H2/H2O ratio. The presence of Co-rich alloys in some of the vesicles shows that the fO2 in the vesicles was near or below the Co-CoO buffer (~NNO – 1.5), which is near that of the magmas (NNO – 2 to NNO + 2) involved here (Chou, 1987). The same holds for Cu that would be stable at magmatic fO2 if the fugacity of sulfur was low enough (Fig. 12). Elements expected to be transferred into the vesicles but missing from the alloy grains (e.g., Fe, Pb, and Zn) may have lower redox potentials, meaning that they tend to remain oxidized despite the higher fH2, helping them to stay in solution. An indication of this, for example, is that the Fe-FeO buffer is at about 3 log units lower fO2 than the Co-CoO buffer (Chou, 1987). The narrow sulfide overgrowth on the allow grains (Fig. 11) may be due to the fact that the sulfide stability fields extend to lower S concentrations in the fluid phase at constant fO2, as discussed above (Fig. 12), or potentially due to decreasing fH2 and thus increasing fO2 induced by the consumption of H2 during metal alloy precipitation.

Another possible mechanism for formation of metallic alloys in vesicles was suggested by the works of Mungall et al. (2015) and Knipping et al. (2015). They suggested that blebs of immiscible sulfide melt form and then adhere to bubbles; the sulfides could then be dissolved into the bubbles and released through volcanic vents, thus explaining observations made by Nadeau et al. (2010), Keith et al. (1997), and Larocque et al. (2000). If some of that metal-laden vapor was trapped as a vesicle, eventual precipitation on the walls might ensue. This might explain the concentric layering (Fig. 1J) where an alloy rim (altered material) covers fresh material (from an entrapped sulfide bleb). It is possible that this mechanism might explain the transport and concentration of some metals with high solubilities in immiscible sulfides (Cu, Ag, Au), but it doesn’t explain why Sn and Co, which have very low solubilities in sulfide melts, would also be concentrated.

A third mechanism to form alloy-filled vesicles also bears consideration. Perhaps the metals were transported in hydrothermal fluids (rather than in low-density vapors) as suspended or colloidal particles, transferred to the vesicles, and eventually aggregated as metallic clusters. This possibility is hard to address in the absence of information on the behavior of suspended particles or colloids at magmatic conditions, but it seems unlikely based on the textures and distributions observed. This physical mechanism of transport should leave deposits along the passageways for the fluids, for which we see no evidence. However, the mechanism begs the question as to how the particles of Cu-Au-Ag-Sn-Co formed in the first place. Why weren’t particles of other metals (e.g., Ti, V, Zr) also formed and transported? It seems more reasonable to conclude that the metals were complexed with ligands and dissolved into low-density fluids that formed vesicles. The nature of the precipitated metals (which are known to form complexes with Cl, S, etc.) better accords with this process. In general, we conclude that the unexpected but apparently widespread presence of Cu, Co, Sn, and Ag alloy precipitates within the vesicles of volcanic rocks is a result of kinetically controlled mass transfer into the vesicles and such induced element separation upon volcanic eruption (Fig. 11).

Economic implications of metal alloys and ore deposits

The low-pressure, kinetically controlled nature of the processes proposed here as responsible for the precipitation of the metal alloy grains does not allow for making direct links to magmatic-hydrothermal ore-forming processes, as these typically occur at greater pressure and much longer time scales. However, there are a few key observations that may indirectly enhance our understanding of ore metal extraction from magmas and raise questions that could be addressed by future research.

One of these is the surprisingly high mobility of Sn, Co, Cu, Au, and Ag in low-density fluids at temperatures characteristic of mafic magmas. Although Cu, Ag, and Au have been shown to be soluble in low-density vapors (Zajacz et al., 2010, 2011; Migdisov et al., 2014; Hurtig and William-Jones, 2015), no data are available for Sn and Co. Some researchers have suggested that the ratios of metals such as Cu, Au, and Ag present in magmatic sulfides are inherited by ore deposits from the associated magmatic system (Halter et al., 2005; Stavast et al., 2006; Nadeau et al., 2010, 2016; Nadeau, 2015). The model invoked in these papers is that the ultimate source of most of the metals and sulfur in large porphyry systems is from under-plated degassing mafic magma. Although such mafic magmas would degas at a much greater depth, the increase of pressure and thus fH2O would only further increase the solubility of Cu and Au (Hurtig and William-Jones, 2014; Migdisov et al., 2014) and potentially other metals as well. Thus, the alloy precipitates observed in this study support the hypothesis that mafic magmas are able to donate ore metals to more overlying felsic systems.

The other interesting observation is the preferential degassing of H2 into the vesicles, leading to reducing conditions adequate for precipitating metal alloys rather than oxides. A corollary of this would be the oxidation of the residual magma during nonequilibrium degassing, as demonstrated by Burnham (1975), Stolper (1982), Mathez (1984), and Waters and Lange (2016). It remains unclear if this may be a viable mechanism of magma oxidation under certain conditions, affecting the potential for magmatic-hydrothermal ore genesis.

Conclusions

Newly discovered alloys are present as scattered grains along vesicle walls in several volcanic systems from contrasting tectonic settings. Our finding of Cu-Sn-Co-Ag metal alloys in volcanic rocks from Kīlauea, Etna, Vesuvius, and Stromboli suggests that metal partitioning to the vapor phase exsolving from mafic magmas at low pressure is a common process. It is likely that the unexpected but apparently widespread presence of Cu, Sn, Co, and Ag alloy precipitates within the vesicles of volcanic rocks is a result of kinetically controlled mass transfer into the vesicles at high temperatures (>900°C) and low pressure (a few bars).

The conditions under which the metal alloys form are likely varied, but there are several factors that seem to be especially important in their formation. We hypothesize that ore metals along with sulfur and chlorine are transferred into syneruptively formed vesicles within cooling lava. Kinetically induced preferential enrichment of H2 over H2O and S in the vesicles induces the precipitation of metal alloys rather than sulfide minerals, whereas a subsequent drop in temperature and/or potential increase in fO2 leads to the formation of a narrow sulfide overgrowth on the alloy grains.

Chlorine and sulfur are especially vital and likely reflect the importance of these elements in larger-scale ore deposits. We suspect that although the number of alloy grains in vesicles is sparse, they are widespread and will soon be recognized in many basaltic systems.

Acknowledgments

The authors would like to thank Keiko Hattori, Dana Griffen, David Tingey, Claudio Scarpati, Jani Radebaugh, and Don Swanson for their help, observations, and insights on this project. We also appreciate the invaluable assistance from Mike Standing, Jeff Farrer, and all those in the BYU microscopy lab during ESEM analysis. The authors extend thanks to Elizabeth Ryscamp, Megan Pickard, and Annika Quick for helping collect the many samples needed. Thanks is also given to Wagner Petrographic for their excellent sample preparation. The authors are also grateful for the help of family in attending to young children during the editing process. Finally, the authors would also like to thank Larry Meinert, Nicole Hurtig, Oliver Nadeau, and Anthony E. William Jones for their insightful and pertinent reviews, which have helped make this manuscript more robust. This publication has been supported in part by a research grant from the SEG Foundation.

REFERENCES

Africano
,
F.
,
Van Rompaey
,
G.
,
Bernard
,
A.
, and
Le Guern
,
F.
,
2002
,
Deposition of trace elements from high temperature gases of Satsuma-Iowjima volcano
:
Earth, Planets and Space
 , v.
54
, p.
275
286
.
Aiuppa
,
A.
,
Federico
,
C.
,
Giudice
,
G.
,
Gurrieri
,
S.
,
Liuzzo
,
M.
,
Shinohara
,
H.
,
Favara
,
R.
, and
Valenza
,
M.
,
2006
,
Rates of carbon dioxide plume degassing from Mount Etna volcano
:
Journal of Geophysical Research
 , v.
111
, p.
1
8
.
Allard
,
P.
,
Carbonnelle
,
J.
,
Dajlevic
,
D.
,
Le Bronec
,
J.C.
,
Morel
,
P.
,
Maurenas
,
J.M.
,
Robe
,
M.C.
,
Faivre-Pierret
,
R.
,
Sabroux
,
J.C.
, and
Zettwoog
,
P.
,
1991
,
Eruptive and diffuse emissions of carbon dioxide from Etna volcano
:
Nature
 , v.
351
, p.
387
391
.
Allard
,
P.
,
Carbonelle
,
J.
,
Métrich
,
N.
,
Loyer
,
H.
, and
Zettwoog
,
P.
,
1994
,
Sulphur output and magma degassing of Stromboli volcano
:
Nature
 , v.
368
, p.
326
330
.
Allard
,
P.
,
Aiuppa
,
A.
,
Loyer
,
H.
,
Carrot
,
F.
,
Gaudry
,
A.
,
Pinte
,
G.
,
Michel
,
A.
, and
Dongarra
,
G.
,
2000
,
Acid gas and metal emission rates during long-lived basalt degassing at Stromboli volcano
:
Geophysical Research Letters
 , v.
27
, p.
1207
1210
.
Alletti
,
M.
,
Baker
,
D.R.
, and
Freda
,
C.
,
2007
,
Halogen diffusion in a basaltic melt
:
Geochimica et Cosmochimica Acta
 , v.
71
, p.
3570
3580
.
Alletti
,
M.
,
Baker
,
D.R.
,
Scaillet
,
B.
,
Aiuppa
,
A.
,
Moretti
,
R.
, and
Ottolini
,
L.
,
2009
,
Chlorine partitioning between a basaltic melt and H2O-CO2 fluids at Etna
:
Chemical Geology
 , v.
263
, p.
37
50
.
Andronico
,
D.
,
Branca
,
S.
,
Calvari
,
S.
,
Burton
,
M.
,
Caltabiano
,
T.
,
Corsaro
,
R.S.
,
Del Carol
,
P.
,
Garfi
,
G.
,
Lodato
,
L.
,
Miraglia
,
L.
,
Mure
,
F.
,
Neri
,
M.
,
Pecara
,
E.
,
Pompilio
,
M.
,
Salerno
,
G.
, and
Spampinato
,
L.
,
2005
,
A multidisciplinary study of the 2002–3 Etna eruption: Insights into a complex plumbing system
:
Bulletin of Volcanology
 , v.
67
, p.
314
330
.
Baker
,
D.R.
,
Freda
,
C.
,
Brooker
,
R.A.
, and
Scarlato
,
P.
,
2005
,
Volatile diffusion in silicate melts and its effects on melt inclusions
:
Annals of Geophysics
 , v.
48
, p.
699
717
.
Barin
,
I.
,
Knacke
,
O.
, and
Kubaschewski
,
O.
,
1977
,
Thermochemical properties of inorganic Compounds
 :
Berlin
,
Springer-Verlag
, p.
825
.
Baxter
,
N.L.
,
2008
,
Magmatic sulfur and chlorine abundances at Stromboli, Italy, and their role in the formation of vesicle-hosted metal alloys
: Unpublished M.Sc. thesis,
Provo, Utah
,
Brigham Young University
,
88
p.
Belkin
,
H.E.
, and
De Vivo
,
B.
,
1993
,
Fluid inclusion studies of ejected nodules from Plinian eruptions of Mt. Somma-Vesuvius nodules
:
Journal of Volcanology and Geothermal Research
 , v.
58
, p.
89
100
.
Bernard
,
A.
,
Symonds
,
R.B.
, and
Rose
,
W.I.
,
1990
,
Volatile transport and deposition of Mo, W and RE in high temperature magmatic fluids
:
Applied Geochemistry
 , v.
5
, p.
317
326
.
Burnham
,
C.W.
,
1975
,
Water and magmas; a mixing model
:
Geochimica et Cosmochimica Acta
 , v.
39
, p.
1077
1084
.
Candela
,
P.A.
, and
Holland
,
H.D.
,
1984
,
The partitioning of copper and molybdenum between silicate melts and aqueous fluids
:
Geochimica et Cosmochimica Acta
 , v.
48
, p.
373
380
.
Chou
,
I.
,
1987
,
Oxygen buffer and hydrogen sensor techniques at elevated pressures and temperatures
, in
Ulmer
,
G.C.
, and
Barnes
,
H.L.
, eds.,
Hydrothermal experimental techniques
 :
New York
,
Wiley
, p.
61
99
.
Cioni
,
R.
,
Bertagnini
,
A.
,
Santacroce
,
R.
, and
Andronico
,
D.
,
2008
,
Explosive activity and eruption scenarios at Somma-Vesuvius (Italy): Towards a new classification scheme
:
Journal of Volcanology and Geothermal Research
 , v.
178
, p.
331
346
.
Cocchi
,
L.
,
Caratori Tontini
,
F.
,
Muccini
,
F.
,
Marani
,
M.P.
,
Bortoluzzi
,
G.
, and
Carmisciano
,
C.
,
2009
,
Chronology of the transition from a spreading ridge to an accretional seamount in the Marsili backarc basin (Tyrrhenian Sea)
:
Terra Nova
 , v.
21
, p.
369
374
.
Conrad
,
M.E.
,
Thomas
,
D.M.
,
Flexser
,
S.
, and
Vennemann
,
T.W.
,
1997
,
Fluid flow and water-rock interaction in the East rift zone of the Kilauea volcano, Hawaii
:
Journal of Geophysical Research: Solid Earth
 , v.
102
, p.
15,021
15,037
.
De Natale
,
G.
,
Troise
,
C.
,
Pingue
,
F.
,
De Gore
,
P.
, and
Chiarabba
,
C.
,
2001
,
Structure and dynamics of the Somma-Vesuvius volcanic complex
:
Mineralogy and Petrology
 , v.
73
, p.
5
22
.
Di Carlo
,
I.
,
Pichavant
,
M.
,
Rotolo
,
S.G.
, and
Scaillet
,
B.
,
2006
,
Experimental crystallization of a high-K arc basalt: The golden pumice, Stromboli volcano (Italy)
:
Journal of Petrology
 , v.
47
, p.
1317
1343
.
Duc-Tin
,
Q.
,
Audetat
,
A.
, and
Keppler
,
H.
,
2007
,
Solubility of tin in (Cl, F)-bearing aqueous fluids at 700 degrees C, 140 MPa: A LA-ICP-MS study on synthetic fluid inclusions
:
Geochimica et Cosmochimica Acta
 , v.
71
, p.
3323
335
.
Elias
,
T.
, and
Sutton
,
A.J.
,
2007
,
Sulfur dioxide emission rates from Kīlauea volcano, Hawaii, an update 2002–2006
:
U.S. Geological Survey, Open-File Report 2007-1114
 ,
37
p.
Etschmann
,
B.E.
,
Liu
,
W.
,
Testemale
,
D.
,
Muller
,
H.
,
Rae
,
N.A.
,
Proux
,
O.
,
Hazemann
,
J.L.
, and
Brugger
,
J.
,
2010
,
An in situ XAS study of copper(I) transport as hydrosulfide complexes in hydrothermal solutions (25–592 degrees C, 180–600 bar): Speciation and solubility in vapor and liquid phases
:
Geochimica et Cosmochimica Acta
 , v.
74
, p.
4723
4739
.
Ferlito
,
C.
,
Coltori
,
M.
,
Lanzafame
,
G.
, and
Giacomoni
,
P.P.
,
2013
,
The volatile flushing triggers eruptions at open conduit volcanoes: Evidence from Mount Etna volcano (Italy)
:
Lithos
 , v.
184–187
, p.
447
455
.
Francalanci
,
L.
,
Tommasini
,
S.
, and
Conticelli
,
S.
,
2004
,
The volcanic activity of Stromboli in the 1906–1998 AD period: Mineralogical, geochemical and isotope data relevant to the understanding of the plumbing system
:
Journal of Volcanology and Geothermal Research
 , v.
131
, p.
179
211
.
Freda
,
C.
,
Baker
,
D.R.
, and
Scarlato
,
P.
,
2005
,
Sulfur diffusion in basaltic melts
:
Geochimica et Cosmochimica Acta
 , v.
69
, p.
5061
5069
.
Fulignati
,
P.
, and
Sbrana
,
A.
,
1998
,
Presence of native gold and tellurium in the active high-sulfidation hydrothermal system of the La Fossa volcano (Vulcano, Italy)
:
Journal of Volcanology and Geothermal Research
 , v.
86
, p.
187
198
.
Guillong
,
M.
,
Meier
,
D.L.
,
Allan
,
M.M.
,
Heinrich
,
C.A.
, and
Yardley
,
B.W.D.
,
2008
,
SILLS: A matlab-based program for the reduction of laser ablation ICP-MS data of homogeneous materials and inclusions
:
Mineralogical Association of Canada, Short Course
 
40
, p.
328
333
.
Halter
,
W.E.
,
Heinrich
,
C.A.
, and
Pettke
,
T.
,
2005
,
Magma evolution and the formation of porphyry Cu-Au ore fluids: Evidence from silicate and sulphide melt inclusions
:
Mineralium Deposita
 , v.
39
, p.
845
863
.
Hattori
,
K.H.
, and
Keith
,
J.D.
,
2001
,
Contribution of mafic melt to porphyry copper mineralization: Evidence from Mount Pinatubo, Philippines, and Bingham Canyon, Utah, USA
:
Mineralium Deposita
 , v.
36
, p.
799
806
.
Hedenquist
,
J.W.
,
Matsuhisa
,
Y.
,
Izawa
,
E.
,
White
,
N.C.
,
Giggenbach
,
W.F.
, and
Aoki
,
M.
,
1994
,
Geology, geochemistry, and origin of high sulfidation Cu-Au mineralization in the Nansatusu district, Japan
:
Economic Geology
 , v.
89
, p.
1
30
.
Hinkley
,
T.K.
,
Lamothe
,
P.J.
,
Wilson
,
S.A.
,
Finnegan
,
D.L.
, and
Gerlach
,
T.M.
,
1999
,
Metal emissions from Kīlauea, and a suggested revision of estimated worldwide metal output by quiescent degassing of volcanoes
:
Earth and Planetary Science Letters
 , v.
170
, p.
315
325
.
Hu
,
X.
,
Bi
,
X.
,
Hu
,
R.
,
Shang
,
L.
, and
Fan
,
W.
,
2008
,
Experimental study on tin partition between granitic silicate melt and coexisting aqueous fluid
:
Geochemical Journal
 , v.
42
, p.
141
150
.
Hu
,
X.
,
Bi
,
X.
,
Shang
,
L.
,
Hu
,
R.
,
Cai
,
G.
, and
Chen
,
Y.
,
2009
,
An experimental study of tin partition between melt and aqueous fluid in F/Cl-coexisting magma
:
Chinese Science Bulletin
 , v.
54
, p.
1087
1097
.
Hurtig
,
N.C.
, and
Williams-Jones
,
A.E.
,
2014
,
An experimental study of the transport of gold through hydration of AuCl in aqueous vapour and vapour-like fluids
:
Geochemica et Cosmochimica Acta
 , v.
127
, p.
305
325
.
Hurtig
,
N.C.
, and
Williams-Jones
,
A.E.
,
2015
,
Porphyry-epithermal Au-Ag-Mo ore formation by vapor-like fluids: New insights from geochemical modeling
:
Geology
 , v.
43
, p.
587
590
.
Keith
,
J.D.
,
Whitney
,
J.A.
,
Hattori
,
K.
,
Ballantyne
,
G.H.
,
Christiansen
,
E.H.
,
Barr
,
D.L.
,
Cannan
,
T.M.
, and
Hook
,
C.J.
,
1997
,
The role of magmatic sulfides and mafic alkaline magmas in the Bingham and Tintic mining districts, Utah
:
Journal of Petrology
 , v.
38
, p.
1679
1690
.
Keller
,
G.
,
2001
,
Applied statistics with Microsoft® Excel
 :
California
,
Duxbury Thomson Learning
,
670
p.
Keppler
,
H.
, and
Wyllie
,
P.J.
,
1991
,
Partitioning of Cu, Sn, Mo, W, U, and Th between melt and aqueous fluid in the systems haplogranite-H2O HCl and haplogranite-H2O Hf
:
Contributions to Mineralogy and Petrology
 , v.
109
, p.
139
150
.
Knipping
,
J.L.
,
Bilenker
,
L.D.
,
Simon
,
A.C.
,
Reich
,
M.
,
Barra
,
F.
,
Deditius
,
A.P.
,
Wälle
,
M.
,
Heinrich
,
C.A.
,
François
,
H.
, and
Munizaga
,
R.
,
2015
,
Trace elements in magnetite from massive iron oxide-apatite deposits indicate a combined formation by igneous and magmatic-hydrothermal processes
:
Geochemica et Cosmochimica Acta
 , v.
171
, p.
15
38
.
Laiolo
,
M.
, and
Cigolini
,
C.
,
2006
,
Mafic and ultramafic xenoliths in San Bartolo lava field: New insights on the ascent and storage of Stromboli magmas
:
Bulletin of Volcanology
 , v.
68
, p.
653
670
.
Lamoreaux
,
R.H.
,
Hildenbrand
,
D.L.
, and
Brewer
,
L.
,
1987
,
High temperature vaporization behavior of oxides. II. Oxides of Be, Mg, Ca, Sr, Ba, B Al, Ga, In, Tl, Si, Ge, Sn, Pb, Zn, Cd and Hg
:
Journal of Physical and Chemical Reference Data
 , v.
16
, p.
419
443
.
Landtwing
,
M.R.
,
Furrer
,
C.
,
Redmond
,
P.B.
,
Pettke
,
T.
,
Guillong
,
M.
, and
Heinrich
,
C.A.
,
2010
,
The Bingham Canyon porphyry Cu-Mo-Au deposit. III. Zoned copper-gold ore deposition by magmatic vapor expansion
:
Economic Geology
 , v.
105
, p.
91
118
.
Larocque
,
A.
,
Stimac
,
J.
, and
Siebe
,
C.
,
1998
,
Metal-residence sites in lavas and tuffs from Volcán Popocatépetl, Mexico: Implications for metal mobility in the environment
:
Environmental Geology
 , v.
33
, p.
197
208
.
Larocque
,
A.
,
Stimac
,
J.
,
Keith
,
J.D.
, and
Huminicki
,
M.A.E.
,
2000
,
Evidence for open-system behavior in immiscible Fe-S-O liquids in silicate magmas: Implications for contribution of metals and sulfur to ore-forming fluids
:
The Canadian Mineralogist
 , v.
38
, p.
1233
1249
.
Larocque
,
A.
,
Stimac
,
J.
,
Siebe
,
C.
,
Greengrass
,
K.
,
Chapman
,
R.
, and
Mejia
,
S.
,
2008
,
Deposition of a high-sulfidation Au assemblage from a magmatic volatile phase, Volcán Popocatépetl, Mexico
:
Journal of Volcanology and Geothermal Research
 , v.
170
, p.
51
60
.
Lipman
,
P.A.
,
Sisson
,
T.W.
,
Tadahide
,
U.
, and
Naka
,
J.
,
2000
,
In search of ancestral Kilauea volcano
:
Geology
 , v.
28
, p.
1079
1082
.
Louvel
,
M.
,
Bordage
,
A.
,
Tripoli
,
B.
,
Testemale
,
D.
,
Hazemann
,
J.L.
, and
Mavrogenes
,
J.
,
2017
,
Effect of S on the aqueous and gaseous transport of Cu in porphyry and epithermal systems: Constraints from in situ XAS measurements up to 600°C and 300 bars
.
Chemical Geology
 , v.
466
, p.
500
511
.
Marianelli
,
P.
,
Métrich
,
N.
, and
Sbrana
,
A.
,
1999
,
Shallow and deep reservoirs involved in magma supply of the 1944 eruption of Vesuvius
:
Bulletin of Volcanology
 , v.
61
, p.
48
63
.
Mathez
,
E.A.
,
1976
,
Sulfur solubility and magmatic sulfides in submarine basalt glass
:
Journal of Geophysical Research
 , v.
81
, p.
4269
4276
.
Mathez
,
E.A.
,
1984
,
Influence of degassing on oxidation states of basaltic magmas
:
Nature
 , v.
310
, p.
371
375
.
Mavrogenes
,
J.
,
Henley
,
R.W.
,
Reyes
,
A.G.
, and
Berger
,
B.
,
2010
,
Sulfasalt melts: Evidence of high-temperature vapor transport of metals in the formation of high-sulfidation lode gold deposits
:
Economic Geology
 , v.
105
, p.
257
262
.
Meeker
,
K.A.
,
Chuan
,
R.L.
,
Kyle
,
P.R.
, and
Palais
,
J.M.
,
1991
,
Emission of elemental gold particles from Mount Erebus, Ross Island, Antarctica
:
Geophysical Research Letters
 , v.
18
, p.
1405
1408
.
Mei
,
Y.
,
Sherman
,
D.M.
,
Liu
,
W.
, and
Brugger
,
J.
,
2013
,
Ab initio molecular dynamics simulation and free energy exploration of copper (I) complexation by chloride and bisulfide in hydrothermal fluids
:
Geochimica et Cosmochimica Acta
 , v.
102
, p.
45
64
.
Métrich
,
N.
,
Clocchiatti
,
R.
,
Mosbah
,
M.
, and
Chaussidon
,
M.
,
1993
,
The 1989–1990 activity of Etna. Magma mingling and ascent of H2O-Cl-S-rich basaltic magma. Evidence from melt inclusions
:
Journal of Volcanology and Geothermal Research
 , v.
59
, p.
131
144
.
Métrich
,
N.
,
Bertagnini
,
A.
,
Landi
,
P.
, and
Rosi
,
M.
,
2001
,
Crystallization driven by decompression and water loss at Stromboli volcano (Aeolian Islands, Italy)
:
Journal of Petrology
 , v.
42
, p.
1471
1490
.
Métrich
,
N.
,
Bertagnini
,
A.
, and
Di Muro
.,
A.
,
2010
,
Conditions of magma storage, degassing and ascent at Stromboli: New insights into the volcano plumbing system with inferences on the eruptive dynamics
:
Journal of Petrology
 , v.
51
, p.
603
626
.
Migdisov
,
A.A.
, and
Williams-Jones
,
A.E.
,
2005
,
An experimental study of cassiterite solubility in HCL-bearing water vapour at temperatures up to 350°C. Implications for tin ore formation
:
Chemical Geology
 , v.
217
, p.
29
40
.
Migdisov
,
A.A.
,
Bychkov
,
A.Y.
,
Williams-Jones
,
A.E.
, and
van Hinsberg
,
V.J.
,
2014
,
A predictive model for the transport of copper by HCl-bearing water vapour in ore-forming magmatic-hydrothermal systems: Implications for copper porphyry ore formation
:
Geochimica et Cosmochimica Acta
 , v.
129
, p.
33
53
.
Moore
,
J.G.
, and
Chalk
,
L.
,
1971
,
Sulfide spherules in vesicles of dredged pillow basalt
:
American Mineralogist
 , v.
56
, p.
476
488
.
Mountain
,
B.W.
, and
Seward
,
T.M.
,
1999
,
The hydrosulphide sulphide complexes of copper(I): Experimental determination of stoichiometry and stability at 22 degrees C and reassessment of high temperature data
:
Geochimica et Cosmochimica Acta
 , v.
63
, p.
11
29
.
Mountain
,
B.W.
, and
Seward
,
T.M.
,
2003
,
Hydrosulfide/sulfide complexes of copper(I): Experimental confirmation of the stoichiometry and stability of Cu(HS)(2-) to elevated temperatures
:
Geochimica et Cosmochimica Acta
 , v.
67
, p.
3005
3014
.
Mungall
,
J.E.
,
Brenan
,
J.M.
,
Godel
,
B.
,
Barnes
,
S.J.
, and
Gaillard
,
F.
,
2015
,
Transport of metals and sulphur in magmas by flotation of sulphide melt on vapour bubbles: Nature Geoscience, v
.
8
, p.
216
219
.
Nadeau
,
O.
,
2015
,
Ore metals beneath volcanoes: Nature Geoscience, v
.
8
, p.
168
170
.
Nadeau
,
O.
,
Williams-Jones
,
A.E.
, and
Stix
,
J.
,
2010
,
Sulphide magma as a source of metals in arc-related magmatic hydrothermal ore fluids: Nature Geoscience, v
.
3
, p.
502
505
.
Nadeau
,
O.
,
Stix
,
J.
, and
Williams-Jones
,
A.E.
,
2016
,
Links between arc volcanoes and porphyry-epithermal ore deposits: Geology, v
.
44
, p.
11
14
.
Neal
,
C.A.
,
Brantley
,
S.R.
,
Antolik
,
L.
,
Babb
,
J.L.
,
Burgess
,
M.
,
Calles
,
K.
,
Cappos
,
M.
,
Chang
,
J.C.
,
Conway
,
S.
,
Desmither
,
L.
,
Dotray
,
P.
,
Elias
,
T.
,
Fukunaga
,
P.
,
Fuke
,
S.
,
Johanson
,
I.A.
,
Kamibayashi
,
K.
,
Kauahikaua
,
J.
,
Lee
,
R.L.
,
Pekalib
,
S.
,
Miklius
,
A.
,
Million
,
W.
,
Moniz
,
C.J.
,
Nadeau
,
P.A.
,
Okubo
,
P.
,
Parcheta
,
C.
,
Patrick
,
M.R.
,
Shiro
,
B.
,
Swanson
,
D.A.
,
Tollett
,
W.
,
Trusdell
,
F.
,
Younger
,
E.F.
,
Zoeller
,
M.H.
,
Montgomery-Brown
,
E.K.
,
Anderson
,
K.R.
,
Poland
,
M.P.
,
Ball
,
J.L.
,
Bard
,
J.
,
Coombs
,
M.
,
Dietterich
,
R.H.
,
Kern
,
C.
,
Thelen
,
W.A.
,
Cervelli
,
P.F.
,
Orr
,
T.
,
Houghton
,
B.F.
,
Gansecki
,
C.
,
Hazlett
,
R.
,
Lundgren
,
P.
,
Diefenbach
,
A.K.
,
Lerner
,
A.H.
,
Wait
,
G.
,
Kelly
,
P.
,
Clor
,
L.
,
Werner
,
C.
,
Mulliken
,
K.
,
Fisher
,
G.
, and
Damby
,
D.
,
2019
,
The 2018 rift eruption and summit collapse of Kīlauea volcano
:
Science
 , v.
363
, p.
367
374
.
Pasteris
,
J.D.
,
1996
,
Mount Pinatubo volcano and “negative” porphyry copper deposits
:
Geology
 , v.
24
, p.
1075
1078
.
Poland
,
M.P.
,
Mikilus
,
A.
,
Sutton
,
J.A.
, and
Thornber
,
C.R.
,
2012
,
A mantle-driven surge in magma supply to Kīlauea volcano during 2003–2007
:
Nature Geoscience
 , v.
5
, p.
295
300
.
Rosi
,
M.
,
Bertagnini
,
A.
, and
Landi
,
P.
,
2000
,
Onset of the persistent activity at Stromboli volcano (Italy)
:
Bulletin of Volcanology
 , v.
62
, p.
294
300
.
Scandone
,
P.
,
1979
,
Origin of the Tyrrhenian Sea and Calabrian arc
:
Bollettino della Societa Geologica Italiana
 , v.
98
, p.
27
-
Si34
.
Simon
,
A.C.
,
Pettke
,
T.
,
Candela
,
P.A.
,
Piccoli
,
P.M.
, and
Heinrich
,
C.A.
,
2006
,
Copper partitioning in a melt-vapor-brine-magnetite-pyrrhotite assemblage
:
Geochimica et Cosmochimica Acta
 , v.
70
, p.
5583
5600
.
Simon
,
A.C.
,
Pettke
,
T.
,
Candela
,
P.A.
, and
Piccoli
,
P.M.
,
2008
,
The partitioning behavior of silver in a vapor-brine-rhyolite melt assemblage
:
Geochimica et Cosmochimica Acta
 , v.
72
, no.
6
, p.
1638
1659
.
Stavast
,
W.J.A.
,
Keith
,
J.D.
,
Christiansen
,
E.H.
,
Dorais
,
M.J.
,
Tingey
,
D.
,
Larocque
,
A.
, and
Evans
,
N.
,
2006
,
The fate of magmatic sulfides during intrusion or eruption, Bingham and Tintic districts
:
Economic Geology
 , v.
101
, p.
329
345
.
Stelling
,
J.
,
Botcharnikov
,
R.E.
,
Beermann
,
O.
, and
Nowak
,
M.
,
2008
,
Solubility of H(2)O- and chlorine-bearing fluids in basaltic melt of Mount Etna at T = 1050–1250 degrees C and P = 200 MPa
:
Chemical Geology
 , v.
256
, p.
102
110
.
Stolper
,
E.
,
1982
,
The speciation of water in silicate melts
:
Geochimica et Cosmochimica Acta
 , v.
46
, p.
2609
2620
.
Strand
,
S.R.
,
Keith
,
J.D.
,
Dorais
,
M.J.
,
Stavast
,
W.J.
,
Aase
,
J.
,
Harper
,
M.P.
,
Harris
,
W.B.
, and
Porter
,
J.
,
2002
,
Mobility of copper, chlorine, and sulfur during quenching of Hawaiian basaltic magmas
:
Geological Society of America Abstracts with Programs
 , v.
34
, no.
6
, p.
88
.
Su
,
Y.
,
Huber
,
C.
,
Bachmann
,
O.
,
Zajacz
,
Z.
,
Wright
,
H.
, and
Vazquez
,
J.
,
2016
,
The role of crystallization-driven exsolution on the sulfur mass balance in volcanic arc magmas
:
Journal of Geophysical Research: Solid Earth
 , v.
121
, p.
5624
5640
.
Symonds
,
R.B.
, and
Reed
,
M.H.
,
1993
,
Calculation of multicomponent chemical equilibria in gas-solid-liquid systems: Calculation methods, thermochemical data and applications to studies of high-temperature volcanic gases with examples from Mount St. Helens
:
American Journal of Science
 , v.
293
, p.
758
864
.
Taran
,
Y.A.
,
Bernard
,
A.
,
Gavilanes
,
J.C.
, and
Africano
,
F.
,
2000
,
Native gold in mineral precipitates from high-temperature volcanic gases of Colima volcano, Mexico
:
Applied Geochemistry
 , v.
15
, p.
337
346
.
van Hinsberg
,
V.
,
Berlo
,
K.
,
Migdisov
,
A.A.
, and
Williams-Jones
,
A.E.
,
2016
,
CO2-fluxing collapses metal mobility in magmatic vapour
:
Geochemical Perspective Letters
 , v.
2
, p.
169
177
.
Wallace
,
P.J.
, and
Gerlach
,
T.M.
,
1994
,
Magmatic vapor source for sulfur-dioxide released during volcanic eruptions: Evidence from Mount Pinatubo
:
Science
 , v.
265
, p.
497
499
.
Waters
,
L.E.
, and
Lange
,
R.A.
,
2016
,
No effect of H2O degassing on the oxidation state of magmatic liquids
:
Earth and Planetary Science Letters
 , v.
447
, p.
48
59
.
Westrich
,
H.R.
, and
Gerlach
,
T.M.
,
1992
,
Magmatic gas source for the stratospheric SO2 cloud from the June 15, 1991, eruption of Mount Pinatubo
:
Geology
 , v.
20
, p.
867
870
.
Williams
,
T.J.
,
Candela
,
P.A.
, and
Piccoli
,
P.M.
,
1995
,
The partitioning of copper between silicate melts and 2-phase aqueous fluids: An experimental investigation at 1 Kbar, 800 degrees C and 0.5 Kbar, 850 degrees C
:
Contributions to Mineralogy and Petrology
 , v.
121
, p.
388
399
.
Williams-Jones
,
A.E.
, and
Heinrich
,
C.A.
,
2005
,
100th anniversary special paper: Vapor transport of metals and the formation of magmatic-hydrothermal ore deposits
:
Economic Geology
 , v.
100
, p.
1287
1312
.
Williams-Jones
,
A.E.
,
Bowell
,
R.J.
, and
Migdisov
,
A.A.
,
2009
,
Gold in solution
:
Elements
 , v.
5
, p.
281
287
.
Yin
,
Y.
, and
Zajacz
,
Z.
,
2018
,
The solubility of silver in magmatic fluids: Implications for silver transfer to the magmatic-hydrothermal ore-forming environment
:
Geochimica et Cosmochimica Acta
 , v.
238
, p.
235
251
.
Yudovskaya
,
M.A.
,
Distler
,
V.V.
, and
Chaplygin
,
I.V.
,
2006
,
Gaseous transport and deposition of gold in magmatic fluid: Evidence from the active Kudryavy volcano, Kurile Islands
:
Mineralium Deposita
 , v.
40
, p.
828
.
Yudovskaya
,
M.A.
,
Svetlana
T.
,
Distler
,
V.V.
,
Chaplygin
,
I.V.
,
Chugaev
,
A.V.
, and
Dikov
,
Y.P.
,
2008
,
Behavior of highly siderophile elements during magma degassing: A case study at the Kudryavy volcano
:
Chemical Geology
 , v.
248
, p.
318
341
.
Zajacz
,
Z.
, and
Halter
,
W.E.
,
2009
,
Copper transport by high temperature, sulfur-rich magmatic vapor: Evidence from silicate melt and vapor inclusions in a basaltic andesite from the Villarrica volcano (Chile)
:
Earth and Planetary Science Letters
 , v.
282
, p.
115
121
.
Zajacz
,
Z.
,
Halter
,
W.E.
,
Pettke
,
T.
, and
Guillong
,
M.
,
2008
,
Determination of fluid/melt partition coefficients by LA-ICPMS analysis of co-existing fluid and silicate melt inclusions: Controls on element partitioning
:
Geochimica et Cosmochimica Acta
 , v.
72
, p.
2169
2197
.
Zajacz
,
Z.
,
Seo
,
J.H.
,
Candela
,
P.A.
,
Piccoli
,
P.M.
,
Heinrich
,
C.A.
, and
Guillong
,
M.
,
2010
,
Alkali metals control the release of gold from volatile-rich magmas
:
Earth and Planetary Science Letters
 , v.
297
, p.
50
56
.
Zajacz
,
Z.
,
Seo
,
J.H.
,
Candela
,
P.A.
,
Piccoli
,
P.M.
, and
Tossell
,
J.A.
,
2011
,
The solubility of copper in high-temperature magmatic vapors: A quest for the significance of various chloride and sulfide complexes
:
Geochimica et Cosmochimica Acta
 , v.
75
, p.
2811
2827
.
Zajacz
,
Z.
,
Candela
,
P.A.
,
Piccoli
,
P.M.
, and
Sanchez-Valle
,
C.
,
2012a
,
The partitioning of sulfur and chlorine between andesite melts and magmatic volatiles and the exchange coefficients of major cations
:
Geochimica et Cosmochimica Acta
 , v.
89
, p.
828
848
.
Zajacz
,
Z.
,
Candela
,
P.A.
,
Piccoli
,
P.M.
,
Sanchez-Valle
,
C.
, and
Wälle
,
M.
,
2012b
,
Gold and copper in volatile saturated mafic to intermediate magmas: Solubilities, partitioning and implications for ore deposit formation
:
Geochimica et Cosmochimica Acta
 , v.
91
, p.
140
159
.
Zajacz
,
Z.
,
Candela
,
P.A.
,
Piccoli
,
P.M.
,
Sanchez-Valle
,
C.
, and
Wälle
,
M.
,
2013
,
Solubility and partitioning behavior of Au, Cu, Ag and reduced S in magmas
:
Geochimica et Cosmochimica Acta
 , v.
112
, p.
288
304
.
Zhai
,
D.
,
Liu
,
J.
,
Tombros
,
S.
, and
Williams-Jones
,
A.E.
,
2018
,
The genesis of the Hashitu porphyry molybdenum deposit, Inner Mongolia, NE China: Constraints from mineralogical, fluid inclusion, and multiple isotope (H, O, S, Mo, Pb) studies
:
Mineralium Deposita
 , v.
53
, p.
377
397
.
Zhang
,
Y.
, and
Ni
,
H.
,
2010
,
Diffusion of H, C, and O components in silicate melts
:
Reviews in Mineralogy and Geochemistry
 , v.
72
, p.
171
225
.
Zhang
,
Y.
,
Ni
,
H.
, and
Chen
,
Y.
,
2010
,
Diffusion data in silicate melts
:
Reviews in Mineralogy and Geochemistry
 , v.
72
, p.
311
408
.

Elizabeth Hunter: My husband, Jake, and I have been fortunate to have great mentors in geology both in our schooling and in our careers. We have worked in economic geology doing new mineral exploration with Golden Gryphon Explorations and have worked the past 10 years at Chevron on asset development teams. We now consult on various projects. Recently we have partnered with over 20 universities in publishing a kindergarten through 12th grade science curriculum called STEMTaught. We have also set up a nonprofit organization called the STEMTaught Foundation to help teachers get better science supplies and training for running hands-on labs in their classrooms.

Gold Open Access: This paper is published under the terms of the CC-BY 3.0 license.

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