HYPOGENE ALTERATION AND MINERALIZATION IN THE DOS POBRES
PORPHYRY CU(-AU-MO) DEPOSIT, SAFFORD DISTRICT, ARIZONA:
A GOLD- AND MAGNETITE-RICH VARIANT OF
ARIZONA PORPHYRY COPPER SYSTEMS
By
Daniel Russin
_________________
A Thesis Submitted to the Faculty of the
DEPARTMENT OF GEOSCIENCES
In Partial Fulfillment of the Requirements
For the Degree of
MASTER OF SCIENCE
In the Graduate College
THE UNIVERSITY OF ARIZONA
2008
2
STATEMENT BY THE AUTHOR
This thesis has been submitted in partial fulfillment of requirements for the
Master of Science degree at The University of Arizona and is deposited in the Antevs
Reading Room to be made available to borrowers, as are copies of regular theses and
dissertations.
Brief quotations from this manuscript are allowable without special permission,
provided that accurate acknowledgment of the source is made. Requests for permission
for extended quotation from or reproduction of this manuscript in whole or in part may be
granted by the Department of Geosciences when the proposed use of the material is in the
interests of scholarship. In all other instances, however, permission must be obtained
from the author.
Daniel Russin______________________________
(author’s signature)
___________________
(date)
APPROVAL BY RESEARCH COMMITTEE
As members of the Research Committee, we recommend that this thesis be accepted as
fulfilling the research requirement for the degree of Master of Science.
Mark D. Barton_____________________________
Major Advisor (type name)
(signature)
__________________
(date)
Eric Seedorff_______________________________
(type name)
(signature)
__________________
(date)
Jon Patchett________________________________
(type name)
(signature)
__________________
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3
Hypogene alteration and mineralization in the Dos Pobres porphyry
Cu(-Au-Mo) deposit, Safford District, Arizona: A gold- and magnetiterich variant of Arizona porphyry copper systems.
Daniel Russin*
Mark D. Barton
Eric Seedorff
Center for Mineral Resources, Department of Geosciences, University of Arizona,
Tucson, Arizona 85721-0077
* E-mail: daniel.russin@gmail.com
Abstract
The Dos Pobres Cu(-Au-Mo) deposit (211 million metric tonnes sulfide resource
0.73% Cu with up to 1 ppm Au) is located in the Safford district of southeastern Arizona
and is one of several Au-bearing porphyry systems in Arizona. The deposit is centered on
Paleocene (57 Ma) quartz monzodioritic porphyry dikes that intrude and alter Late
Cretaceous (67-73 Ma) basaltic andesites. The porphyry dikes locally contain igneous
anhydrite. The volcanic rocks dip gently (10-15° ) to the northeast; they and the ENEtrending porphyry dikes are cut by a NW-striking down-to-the-west normal fault that
down-drops the southwestern portion of the Dos Pobres system by roughly 1 km. This
study focuses on the characterization and distribution of veins, hydrothermal alteration,
and ore minerals below the base of weathering, utilizing core logging and petrography
4
coupled with whole-rock geochemical and electron microprobe analyses, as well as U-Pb
and Re-Os geochronology.
Hypogene veins at Dos Pobres are divided into groups based on their mineralogy,
textures, and alteration envelopes. Five early vein types have envelopes that are
dominated by biotite and/or K-feldspar. These are: hairline biotite (biotite ± magnetite ±
bornite); sugary quartz (quartz + K-feldspar ± sulfide (bornite chalcopyrite) ± biotite ±
anhydrite); comb quartz (inward-growing quartz + K-feldspar ± sulfide (bornite <
chalcopyrite) ± biotite); complex biotite (biotite + K-feldspar + quartz + sulfide (pyrite <
bornite < chalcopyrite) ± anhydrite); and green mica veins (biotite + sericite + K-feldspar
± sulfide (bornite chalcopyrite) ± anhydrite ± andalusite). Two types of veins with
chlorite ± sericite envelopes are sulfide-sericite (sulfide (chalcopyrite > pyrite)
± q u a r t z ± sericite ± chlorite ± anhydrite) and clotty sulfide-chlorite (quartz
± sulfides (chalcopyrite > pyrite) ± chlorite ± sericite ± anhydrite). These veins cut those
with biotite and/or K-feldspar envelopes. Veins consisting of chlorite + epidote + calcite
+ quartz ± sulfide (pyrite > chalcopyrite) with chlorite + epidote + calcite envelopes are
also common and cut those with chlorite ± sericite envelopes. Zeolite veins without
alteration envelopes cut all other vein types.
Potassic alteration assemblages with pervasive biotite ± K-feldspar ±
magnetite comprise the best developed and earliest alteration suite. It is most intense in
proximal locations where quartz + K-feldspar veins locally compose upwards of 30 vol
percent of the rock. The intensity of this alteration diminishes outward and upward.
Scattered biotite + actinolite-hornblende + magnetite alteration is interpreted to represent
5
the fringes of pervasive potassic alteration. Hydrolytic alteration, characterized by
sericite- and chlorite-rich replacement of feldspars and biotite is later and/or peripheral,
partially
overprinting
potassic
alteration.
Propylitic
alteration
(chlorite
± epidote ± calcite) forms a weakly defined zone that overprints the earlier assemblages
and shows a gradational boundary with unaltered host rock. Whole-rock geochemical
analyses indicate that the Dos Pobres rocks have unextraordinary igneous compositions
but that many of them have experienced significant metasomatic addition of
K2O, whereas hydrolytic alteration is quantitatively minor.
Hypogene sulfides are abundant and systematically distributed beneath the base of
oxidation (depth ~350 m). Early bornite (± chalcocite ± digenite) dominates the deep
core of the deposit coincident with the most intense K-silicate alteration and quartz veins.
There is a transition from these through bornite-chalcopyrite assemblages into
chalcopyrite-dominated veins. The chalcopyrite-bearing veins typically cut bornite-rich
veins and surround the bornite-dominated core but are also associated with K-silicate
alteration. Pyrite (± chalcopyrite)-bearing veins have hydrolytic envelopes and are most
abundant in a ring-shaped zone surrounding the core. Molybdenite is rare but is most
commonly associated with chalcopyrite in deep, flanking veins with associated hydrolytic
alteration. Gold occurs as tiny (mostly <10 μm) grains of electrum (~10-15 wt % Ag) and
sylvanite in early bornite. Silver is also present in early bornite, occurring as electrum,
hessite, sylvanite, and a silver sulfide mineral (argentite?). Silver also occurs as hessite
and sparse argentiferous galena (up to ~2.5 wt % Ag) that commonly rim and crosscut all
6
Cu-Fe sulfides. Supergene bornite, chalcocite, and rare covellite locally replace hypogene
sulfides beneath the oxide zone.
Dos Pobres is unusual among Arizona porphyry deposits in that it is relatively
gold- and bornite-rich, and magnetite-bearing and is intimately associated with relatively
mafic (quartz monzodiorite - low silica granodiorite) porphyry dikes. Conversely, it has
considerably less pyrite and acid alteration than most other Arizona porphyry deposits.
These features are like those in many other Au-rich porphyry systems, and they have also
stimulated comparisons with andesite-hosted iron-oxide(-Cu-Au) (IOCG) systems such
as Candelaria.
At Dos Pobres, as in most Cu-Au-Mo porphyry deposits, Cu-Fe sulfides are
deposited with voluminous early quartz veins, magnetite is widespread but minor in
abundance, bornite is the dominant early ore mineral, deposition of pyrite postdates most
deposition of Cu, and there is a close spatial and temporal association of mineralization
with relatively mafic porphyry intrusions – all features consistent with introduction and
cooling of magmatic fluids. These characteristics differ profoundly from andesite-hosted
IOCG deposits, which typically have abundant Fe-oxides (tens of percent), REE
enrichment, voluminous Na-Ca and/or K-Ca alteration, comparatively sparse quartz
veins, and generally late copper mineralization.
Introduction
The Dos Pobres porphyry Cu(-Au-Mo) deposit is located in the North American
Laramide porphyry belt, which extends from western Mexico into Arizona and New
7
Mexico. This region is richly endowed with porphyry Cu-(Mo) deposits, yet Dos Pobres,
one of at least four porphyry deposits in the Safford district (Langton and Williams,
1982), represents one of the few porphyry Cu(-Au-Mo) deposits, a distinctive family of
porphyry deposits that are commonly associated with relatively mafic intrusive rocks
(Seedorff et al., 2005), that has been documented to date. The spatial and temporal
association of Dos Pobres with comparatively Au-poor porphyry Cu-Mo deposits in the
region and perhaps in the Safford district poses questions about comparisons between
these systems and the processes that form them. Many hypotheses have been presented,
including differences in composition and/or thickness of underlying crust (Hollister,
1975), differences in emplacement depth or wall-rock properties (Kesler, 1973), vertical
zoning of Cu and Au coupled with different erosion levels (Titley, 1982), composition of
mineralizing intrusions (Kesler, 1973; Sillitoe, 1979), and other complex magmatic
geochemical factors (Sillitoe, 2000). As more of these deposits have been discovered and
described, it is apparent that these systems show differences among themselves and that
none of these hypotheses is sufficient – thus there is the need for continued systematic
study of the deposits themselves and for their comparison with others.
This study, which was sponsored by Phelps Dodge Exploration (now FreeportMcMoRan Copper and Gold), was undertaken with the twin goals of characterizing the
mineralogy and distribution of precious metals in the hypogene mineralization and
developing insight into the possible reasons for the unusual metal endowments in this
atypically (for Arizona) Au-rich porphyry copper system.
8
Dos Pobres shows strong similarities to many other porphyry Cu(-Au-Mo)
deposits worldwide, such as the predominance of early potassic (secondary biotite
± K-feldspar) alteration that carries most Cu and has associated precious metals (cf.
Gustafson and Hunt, 1975; Sillitoe, 1979; Seedorff et al., 2005), lack of well-developed
quartz + sericite alteration (Sillitoe, 1979), and relatively low molybdenum content. As
the other deposits in the Safford district become more completely explored and described,
the district may present an uncommon opportunity to compare and contrast different
deposits that formed in identical host rocks and closely in time. The data presented in this
study will add to the understanding of vein and alteration types and mineralization style
present in Cu(-Au-Mo) deposits.
This study presents data on the host and intrusive rocks and their geochemistry
and U-Pb geochronology, alteration types and distribution, vein types (and their
distribution, paragenetic sequence, and Re-Os geochronology), and sulfide mineralogy
and distribution. Selected intervals of drill core were logged to enable the construction of
an ENE-trending cross section through the deposit and a plan map on the 2,000 ft (600
m) level; selected samples from these intervals were made into polished thin sections.
These results compile to give a detailed picture that shows that Dos Pobres resembles
aspects of other porphyry Cu-Au deposits worldwide, notably in the southwest Pacific,
such as Grasberg, Papua, Indonesia, and Panguna, Bougainville, Papua New Guinea
(Rubin and Kyle, 1997; Fountain, 1972), Far Southeast, Philippines (Hedenquist et al.,
1998), and Goonumbla and Endeavour, New South Wales, Australia (Lickfold et al.,
2003; Wilson et al., 2003).
9
Location
Dos Pobres is located in southeastern Arizona ~50 km southwest of the Morenci
district (Fig. 1A), near the boundary between the Basin and Range province of southern
and western Arizona and the Colorado Plateau to the northeast. Dos Pobres is located in
the Safford (Lone Star) district, which contains a NW-SE oriented group of porphyry
deposits located northeast of the town of Safford, in the northwest-trending Gila Range
(Fig. 1B). Dos Pobres is situated at the northwestern end of the district; the other deposits
include San Juan, Lone Star, and Sanchez, as well as several small prospects. The Lone
Star deposit is situated beneath the spine of the Gila Range, whereas Dos Pobres, San
Juan, and Sanchez crop out in the southwestern foothills.
Exploration and Development History
Copper mineralization in the Safford (Lone Star) district has been known for over
one hundred years. The San Juan, Lone Star, and Sanchez deposits were claimed in the
late 1800s, and some small-scale exploration and mining took place at these three
deposits in the late 19th and early 20th centuries. By about 1920, exploration and
production had largely ceased (Robinson and Cook, 1966).
Porphyry copper exploration of the district by many companies resumed in the
late 1940s and was most active until the late 1960s. The Dos Pobres deposit was
discovered by Phelps Dodge in 1958 (Langton and Williams, 1982). A project in the late
1970s to evaluate bulk underground mining of the deposit was abandoned due to
geotechnical problems and other factors, such as copper price, water availability, and
10
project economics) (J. E. Gerwe, pers. comm., 2006). The Lone Star deposit, which was
discovered by Bear Creek Mining Co. (a Kennecott subsidiary) in the mid-1950s and
studied as a potential in situ leaching project (Robinson and Cook, 1966; Anonymous,
1973; D’Andrea et al., 1974), was acquired by Phelps Dodge in 1986. Drilling resumed at
Dos Pobres in early 1990, this time focused on the supergene mineralization; by 1991, a
leachable resource was delineated. Phelps Dodge purchased the nearby San Juan deposit
in 1992, in 1994 initiated permitting to put both Dos Pobres and San Juan into production
as a single leach operation, and then in 1995 purchased the Sanchez deposit. Freeport
McMoRan acquired Phelps Dodge in 2007.
Production from the leachable part of the Dos Pobres deposit commenced in late
2007, and the combined Dos Pobres-San Juan leach operation at the end of 2007 carried a
proven and probable ore reserve of 549 million metric tonnes at 0.36% Cu (weighted
average of crushed and run-of-mine leach ore, FMI 2007 10-K Report). The sulfide
portion of the Dos Pobres deposit contains 211 million metric tonnes of mineralized
material at an average grade of 0.73% Cu (FMI 2007 10-K Report). There are no
published figures for the sulfide portion of the San Juan deposit. FMI is actively
exploring the Lone Star deposit and currently considers that the deposit contains 1,451
metric tonnes of leachable mineralized material at an average grade of 0.38% Cu (FMI
2007 10-K Report). FMI does not currently quote a size or grade of the sulfide portion of
the Lone Star deposit, but Williams and Forrester (1995) published a sulfide resource of
~4,300 million metric tonnes at an average grade of 0.47% Cu. Sanchez contains 209
million metric tonnes of mineralized material at an average grade of 0.29% Cu (FMI
11
2007 10-K Report), and there are no published estimates regarding the sulfide portion of
the deposit.
Previous Work
Published reports on the Safford district are few despite its long history of mineral
exploration and its huge mineral resource. Robinson and Cook (1966) were the first to
present a detailed study of the geology of the area; they focused on the Lone Star and San
Juan deposits and comparisons between them. Blake (1971) described the structure,
alteration, and mineralization of the surface exposure of the San Juan deposit. Bolin
(1976) compared the major element whole-rock geochemistry of the Lone Star and San
Juan rock suites with several other barren and mineralized intrusive complexes in
Arizona. Dunn (1978) examined and interpreted the structure of the district. Langton and
Williams (1982) published the first description of the structure, alteration, and
mineralization at the Dos Pobres deposit. Lang and Titley (1998) published major- and
trace-element data as well as Sm-Nd and Rb-Sr isotopic data from Safford and other
districts. Wilson (2004) mapped and interpreted different styles of leached capping
present at Dos Pobres, concluding that the supergene zone may be the product of more
than one cycle of weathering.
Synopsis of Safford District Ore Deposits
The Dos Pobres orebody is centered on a swarm of east-northeast-trending
porphyry dikes of quartz monzodioritic composition and is broadly domal in form.
Bornite-chalcopyrite mineralization and biotitic alteration dominates the core of the
12
orebody, magnetite is widespread, and the overall deposit is relatively poor in
molybdenum and rich in precious metals (Langton and Williams, 1982; this study).
Sericitic alteration is poorly developed and discontinuous in the sulfide zone and only
somewhat better developed at higher levels, consistent with the relatively high oxide
copper grades and moderate development of chalcocite enrichment (Langton and
Williams, 1982; Wilson, 2004; this study).
Each of the other three deposits, Lone Star, San Juan, and Sanchez, is centered on
near-vertical intrusions that are hosted by intermediate to mafic volcanic rocks,
apparently localized along east-northeast trending faults or shear zones (Robinson and
Cook, 1966; Dunn, 1978; Dreier, 1994). The names used to classify the intrusions seem
to imply that the compositions of stocks at certain deposits, such as Lone Star (Robinson
and Cook, 1966), may be more silicic than at Dos Pobres, but Dunn (1978) noted that the
main intrusions at each deposit “are nearly identical in composition and texture.” Several
of the deposits contain crosscutting dikes, breccia pipes, and pebble dikes.
The three deposits other than Dos Pobres also have limited published information
on their alteration-mineralization characteristics. Robinson and Cook (1966) describe a
central area of intense sericitic alteration that is partially superimposed on a large area of
biotitization. The only sulfides that Blake (1971) reported at the San Juan deposit are
chalcopyrite and pyrite. At Lone Star, Robinson and Cook (1966) report that chalcopyrite
is much more common than bornite, that magnetite is fairly common; and that
molybdenite occurs in quartz veins and is more abundant in the deeper sulfide zones.
Maps of the distribution of Mo, Au, and Ag grades, presented by Langton and Williams
13
(1982) for Dos Pobres, have not been published for the other deposits. Moreover, the
average grades of elements other than Cu have not been published for any deposit and
may not be available considering that the development focus has been mostly on
supergene mineralization.
It remains to be seen whether potential differences between deposits are within
the range observed in other tonalitic-granodioritic porphyry Cu-(Au-Mo) deposits
(Seedorff et al., 2005), or whether some of the deposits may be gold-poor and related to
more silicic intrusions, such as the quartz monzodioritic-granitic porphyry Cu-(Mo)
deposits of the nearby Morenci district, which is permitted by the petrologic information
presented below.
Geology
Stratigraphy
The known stratigraphy in the Safford district is composed entirely of Late
Cretaceous and younger volcanic and volcaniclastic rocks overlain by basin-filling
sediments (Fig. 1B, C). The oldest rocks exposed are the Safford Volcanics (“older
volcanics” of Robinson and Cook, 1966), which comprise >1,300 m of basaltic to dacitic
volcanic and volcaniclastic rocks (Langton and Williams, 1982; Houser et al., 1985).
Near the Dos Pobres and San Juan deposits, these are dominantly basaltic
(trachy)andesites (see Fig. 2A below). Andesite hosting the Dos Pobres system has been
dated at 73.3 ± 1.0 Ma (U-Pb, Appendix A), and stratigraphically higher andesite near
14
San Juan yielded 67.6 ± 1.4 Ma (Ar-Ar on hornblende, Houser et al., 1985). Their total
thickness is unconstrained. The nearest Paleozoic rocks are ~25 km northwest of Dos
Pobres in the Gila Mountains; the nearest exposure of Precambrian rocks is ~50
kilometers to the southwest in the Pinaleño Mountains, a metamorphic core complex.
Xenoliths of presumably Precambrian schist, granite, and gneiss are present in the
Safford Volcanics. Quartzite xenoliths are also present, which resemble the Precambrian
Coronado Quartzite exposed near Morenci (Robinson and Cook, 1966).
Rock fragments in the andesites vary considerably in their appearance. Most
fragments are andesitic in composition, with noticeable differences in color (shades of
gray to black) and phenocryst size and abundance. Phenocryst contents in the Safford
volcanics range from near zero to ~50 vol percent. They consist dominantly of
plagioclase (An20-An80, avg. An55) and range in size from <1 to 5 mm, with most between
1-3 mm. Hornblende or pyroxene phenocrysts are common (up to ~5 vol %) with most 2
mm or less in length; near Dos Pobres shreddy biotite replaces most mafics. Magnetite is
present as an accessory phase, usually containing <0.1 wt percent Ti. Individual units
within the andesites differ greatly in the types, sizes, and abundances of fragments and
phenocrysts present, but the units are intercalated and too altered to attempt correlation of
units between drill holes.
Langton and Williams (1982) distinguish a younger, somewhat less altered
sequence of andesitic agglomerates, flow breccias, and lithic tuffs that they term the
Baboon Volcanics. Freeport geologists believe that the Baboon andesites should be
considered part of the Safford Volcanics, since they differ only in their alteration and may
15
interfinger with them (Bill Stavast, pers. comm., 2008). Dikes, sills, and plugs of
hornblende andesite intrude both the Safford and Baboon volcanics and appear to be
related to the extrusion of the Baboon sequence (Langton and Williams, 1982).
Regardless of affiliation, the older volcanic rocks are overlain by the Miocene-Pliocene
(?) Gila Volcanics, which consist of a bimodal sequence of basalts, tuffs, rhyolites, and
agglomerates. The Gila Volcanics locally exceed 1 km in thickness and form the spine of
the Gila Mountains. Middle Tertiary to Recent variably indurated gravels, finer-grained
clastic rocks, and local evaporites fill valleys and partially cover the older units (Houser
et al., 2004).
Intrusive Rocks
The largest known intrusive body in the Safford district is the Lone Star stock.
Numerous smaller intrusive bodies crop out in the district such as the San Juan stock and
intrusive rocks near the Sanchez deposit.
The main intrusive phases known at Dos Pobres are Paleocene (57.1 Ma, U-Pb,
Appendix A) porphyries of quartz monzodioritic to low-silica granodioritic composition
(see Fig. 2E below). These occur as east-northeast trending dikes which, on the 2,000-ft
level (~600 m a.s.l.), range from ~150-300 m in length and ~15-100 m in width (Fig.
1D); the ENE orientations are typical of Laramide-age intrusive in this region (Rehrig
and Heidrick, 1972; Titley and Heidrick, 1982). The fresh rock (see Fig. 5A below) is
medium gray in color with obvious plagioclase and biotite phenocrysts. Plagioclase
(An35-An60, avg. An40) is the most common phenocryst mineral; abundances range from
16
~20-50 vol percent. Crystal sizes range from <1 to about 10 mm, most commonly
between 3 and 6 mm. Equant biotite phenocrysts are abundant, typically ranging from 2
to 5 mm, rarely up to 10 mm; abundances range from <1 to ~10 vol percent, but typically
are
~5
vol
percent.
Hornblende
phenocrysts
(altered
to
biotite
± magnetite ± rutile) typically compose ~5 vol percent and are typically <5 mm in the
long dimension. Quartz phenocrysts are generally absent, though they are locally present
(at ~5 vol %) and range from 3 to 6 mm. They are well rounded and partially resorbed.
The groundmass consists typically of fine, 0.05-0.1 mm plagioclase and biotite with
quartz, K-feldspar, magnetite, sphene, and rare anhydrite. Anhydrite typically occurs as
<0.1 mm grains scattered in the groundmass; however, two larger (~1 cm) crystals also
were noted (see Fig. 5B below). Magnetite is present as an igneous phase and very rarely
shows evidence of hematite exsolution; Ti contents are typically <0.1 wt percent. Chilled
margins are locally observed at contacts with andesite.
Igneous Geochemistry
Appendix B summarizes whole-rock major- and trace-element data for Dos
Pobres. The compositions of various units are shown in Figures 2 and 3 below. The
Safford andesites are of continental affinity (Fig. 2B) and are metaluminous to weakly
peraluminous (Fig. 2D). The freshest andesites cluster in the high-K calc-alkaline field on
a K2O vs. SiO2 diagram (Fig 2C), but several lie in the shoshonite field due to
K2O metasomatism. IUGS and chondrite-normalized REE plots are shown in Figures 2E
and 2F. The two freshest porphyry samples plot within the quartz monzodiorite field near
17
the boundary with granodiorite (Fig. 2E); the other four samples plot in the granite field
principally due to K2O metasomatism and quartz veining but with a possible contribution
from original igneous variability. Similar trends representing addition of K-feldspar and
quartz are visible in Fig. 2A, C, and D.
Several porphyry and andesite samples from Langton and Williams (1982) and
Lang and Titley (1998) are also plotted in Figures 2A, C, and E, as well as in Figure 4A
below. The compositions of their samples plot with those analyzed in this study, with two
exceptions: the “porphyry with secondary biotite” has an exceptionally low silica content
for a porphyry (56 wt %) and based on the geochemistry is probably an intensely altered
andesite; the “porphyry altered to quartz-sericite” has been subjected to more intense
hydrolytic alteration than any samples collected during this study (see Fig. 4A below).
Analyses of Safford Volcanics provided by Blake (1971) and Bolin (1976) are similar to
those plotted. Also plotted are compositions for the Lone Star stock, Lone Star
porphyries, Baboon volcanics, and hornblende andesite dikes from Lang and Titley
(1998).
Chondrite-normalized REE patterns (Fig. 2F) of samples of the Safford Volcanics
show a small positive Eu anomaly. The porphyries at Dos Pobres show more pronounced
positive Eu anomalies; REE concentrations are reduced with increasing alteration
intensity. Samples from the seemingly barren Lone Star stock and the porphyries from the
Lone Star deposit show slightly negative Eu anomalies (Lang and Titley, 1998). The
Baboon volcanics show a similar distribution pattern to the Safford Volcanics but with
18
slightly higher REE concentrations. The hornblende andesite dike material is similar to
the Safford Volcanics.
Additionally, porphyries at Dos Pobres have a more primitive Nd signature (-3.2)
than those at the Lone Star deposit (-8.7) and all other Laramide porphyries sampled by
Lang and Titley (1998).
Structure
The Safford district lies between the highly extended Pinaleño core complex to
the southwest and the Mogollon Rim (the edge of the undeformed Colorado Plateau) to
the
northeast.
The
(Gila
Volcanics
in
the
Safford
district
are
tilted
10-15° NE; the deposits and their host rocks are interpreted by previous workers to have
experienced the same amount of tilting. Several sets of faults have been observed and
documented in the Safford district. Langton and Williams (1982) describe a north-south
trending fault set; they also mapped several low-angle faults near the Dos Pobres orebody
but did not speculate on their significance. Structural maps published by Robinson and
Cook (1966) and Langton and Williams (1982) illustrate that all four deposits in this
district are situated along ENE-trending shear zones. Robinson and Cook (1966) report
that the shear zones at San Juan and Lone Star have uncertain displacements (possibly as
much as 250 m combined) and dip vertically or steeply to the north. The shearing does
not affect the Gila Volcanics. Langton and Williams (1982) also describe numerous faults
that strike east-northeast.
19
The dominant structures in the district are the Butte and Red Dyke faults, which
are normal faults that strike northwest and have down-to-the-southwest offset. Dunn
(1978) reports that the Butte fault has ~1,200 m of dip-slip displacement and an
unspecified amount of left-lateral offset where it cuts the Dos Pobres system. Drilling
data indicate that where the Butte fault cuts the southwestern portion of the Dos Pobres
system, it juxtaposes barren Tertiary basaltic andesites and basalts in the hanging wall
and mineralized andesites in the footwall from the surface down to a depth of at least 800
m (Dunn, 1978). Movement on these and other normal faults in the region has tilted the
post-mineral volcanics 10-15° to the northeast, and this appears to be the total tilt in the
district (Dunn, 1978). However, the intense deformation in the Pinaleño Mountains to the
southwest coupled with the observations of low-angle faults in and near Dos Pobres
suggests that the geologic setting may be more complicated than has been previously
appreciated.
Alteration Types
Sulfide minerals, veins, and alteration envelopes are interrelated features. At Dos
Pobres, alteration occurs generally as envelopes on veins and veinlets which commonly
partially coalesce but may be truly pervasive. Moreover, multiple vein types may
contribute to a single alteration type. Sulfide minerals occur in both the vein fillings and
the alteration envelopes. Here, we first describe the alteration types. Then we describe the
veins separately, albeit linking their envelopes to the earlier description of alteration
types. The veins also provide the best evidence for the relative ages of events
20
(paragenesis). We then describe the sulfide mineralogy, including the occurrence of
precious metals. The sulfide mineralogy is organized by vein type, which in turn can be
tied to alteration. Finally, we summarize the spatial distributions of veins and associated
alteration and synthesize the temporal relationships.
There are several groups of alteration assemblages present at Dos Pobres. One of
the goals of this study is to construct a map of the zoning of hydrothermal alteration
around the porphyry dikes at Dos Pobres using observations from core logging and
petrography. Alteration types and individual assemblages are summarized in Table 1.
Potassic Assemblages
Quartz + K-feldspar + Magnetite + Biotite Alteration
The earliest and most intense alteration observed occurs at the locus of intrusion
and consists of quartz, K-feldspar, magnetite, and biotite (Table 1). In andesitic rocks, this
alteration is typically texturally destructive, replacing the original rock with irregular
masses of quartz, K-feldspar, and magnetite and lacing the rock with veins of identical
mineralogy (see Fig. 5C below). The same alteration minerals are present in the
porphyries, where igneous textures are typically preserved.
Biotite + K-feldspar + Magnetite Alteration
The dominant alteration assemblage at Dos Pobres consists of biotite, K-feldspar
and magnetite (Fig. 3E, F, G, H, K, L, M). This type contains more biotite and less
quartz, K-feldspar, and magnetite than the previous type; biotite is modally the most
abundant mineral. Even in the most intense examples of this alteration type, magnetite
21
and K-feldspar form in mineral sites, as opposed to irregular masses, and igneous texture
is preserved. This alteration is present with variable intensity in all logged intervals at
Dos Pobres, such that the effects of lower-temperature alteration types such as hydrolytic
and propylitic (see descriptions below) are always superimposed this biotite-dominated
alteration.
In andesite, this assemblage consists of biotite, magnetite, K-feldspar, quartz,
rutile, and anhydrite. Mafic phenocrysts are completely replaced by biotite ± magnetite ±
rutile. Ilmenite is uncommon; when present it occurs with biotite and magnetite in mafic
sites. Plagioclase phenocrysts are partially to completely replaced by K-feldspar ± biotite
± magnetite. Where biotite and magnetite occur in plagioclase, they typically occur as
tiny specks scattered throughout the phenocryst, but uncommonly biotite replaces
selected zones that reflect original zoning in the plagioclase. Anhydrite is not abundant,
but where present it occurs as tiny (0.1-0.5 mm) equant grains disseminated in the
groundmass or with biotite and magnetite in mafic sites. The groundmass is flooded with
biotite, and the rock thus appears dark gray to black in hand specimen (see Fig. 5F, L, M,
O below). Fragments in the andesites show marked differences in their susceptibility to
alteration; they are typically less susceptible than the groundmass. Igneous magnetite
may be rimmed with biotite. Hydrothermal magnetite is abundant (3-10 vol %) and
contains up to 0.5 wt percent Ti, higher than typical igneous values (<0.1 wt %).
In the porphyries, K-feldspar dominates the potassic assemblage, commonly
tingeing plagioclase phenocrysts pink and flooding the groundmass. Plagioclase
phenocrysts are partly to completely replaced by K-feldspar but generally lack the
22
speckling of biotite and magnetite that is commonly present in the andesites. Magnetite is
far less abundant than in the andesites (typically <5%). Some secondary biotite is present
in the groundmass, and biotite phenocrysts may show thin rims of very fine (<20 μm)
secondary biotite. In some areas, biotite alteration of porphyry is so intense that only the
ghosts of biotite phenocrysts enable it to be distinguished from biotitized andesite
(Langton and Williams, 1982). Mafic phenocrysts are completely replaced by the same
minerals as in the andesites. Anhydrite is more common than in the andesites, and occurs
mainly as 0.1-0.5 mm grains scattered in the groundmass.
The intensity of this alteration varies, and the characteristics of biotite show these
differences clearly. The grain size of secondary biotite in andesite tends to increase with
increasing intensity; it is megascopically visible in the most intensely altered samples. In
thin section, there are noticeable color differences in biotite; in intensely altered rocks,
biotite is dark reddish brown, whereas in weakly altered rocks it assumes a tan or
greenish color. These color differences correlate with the TiO2 content of the biotite; as
indicated by microprobe analyses, biotite from weakly altered rocks generally has
TiO2 contents between 1.5 and 3 wt percent, whereas igneous biotite and biotite from
intensely altered rocks have TiO2 contents up to 4.5 wt percent (see Fig. 3B below).
Biotite + Amphibole ± Magnetite Alteration
This uncommon mineral assemblage resembles biotite-dominated alteration in
hand sample (see Fig. 5N below) but differs in thin section (see Fig. 5D below). Biotite
and amphibole occur together in mafic sites whereas feldspars are partially replaced by
K-feldspar, biotite, and magnetite. The groundmass is typically clouded by very fine (<10
23
μm) magnetite grains though they are not always present. Exceptionally anorthitic
plagioclase (up to An95) is uncommonly present with this alteration; it is unknown if this
plagioclase is igneous or hydrothermal.
Amphibole compositions obtained by electron microprobe are plotted in Fig. 3A
below. Less silica in the tetrahedral site (lower TSi) indicates a higher crystallization
temperature. Relict igneous hornblende is locally present at Dos Pobres, comprising the
scattering of data in the magnesio-hornblende field. Hydrothermal hornblende plots in the
actinolitic hornblende to actinolite fields with TSi values that indicate a lower
crystallization temperature.
Hydrolytic Alteration
Hydrolytic alteration is spatially widespread but volumetrically minor in the
sulfide portion of Dos Pobres. It is easily recognized in the porphyry dikes, where
feldspars are destroyed by sericite and quartz and biotite (primary and secondary) is
altered to sericite ± chlorite. In the andesites, chlorite is more abundant than
in the porphyries; feldspars are altered to sericite, and biotite is altered to chlorite and/or
sericite. Titanium-bearing minerals (sphene and/or rutile) are commonly present with
chlorite and sericite after biotite; rutile predominates in more intense alteration whereas
sphene is much more common in weakly altered areas. As a result, most Ti in porphyries
is present as rutile, whereas in andesite a greater fraction is present as sphene. Hydrolytic
alteration is easily recognized in the andesites where it is locally intense; however, weak
hydrolytic alteration in andesitic rocks can be difficult to resolve because chlorite
24
commonly
proxies
for
sericite
in
intermediate
to
mafic
rocks
(Seedorff
et al., 2005).
Propylitic Alteration
In the andesites, abundant chlorite and epidote characterize this association (see
Fig. 5C, I below); in the logged intervals, this alteration is typically superimposed on
biotitic alteration. Mafic sites are occupied by chlorite that may be accompanied by
epidote, calcite, sphene, and/or rutile; these minerals have replaced earlier hydrothermal
biotite and/or amphibole. Relict plagioclase phenocrysts and secondary K-feldspar may
be partially altered to fine-grained epidote, chlorite, sericite, and/or clay. In some drill
holes, texturally destructive patches of epidote ± chlorite ± magnetite are common (see
Fig. 5H below); this alteration may predate Cu mineralization (Langton and Williams,
1982). Sulfides are not typically associated with this alteration; where present, they
consist dominantly of pyrite with traces of chalcopyrite.
Propylitic alteration is weak to absent in the porphyry dikes. Where it is present, it
is most obviously manifested as the partial to complete replacement of igneous and
hydrothermal biotite by chlorite accompanied by epidote, calcite, and/or sphene. In some
samples, mafic minerals are replaced by apple-green intergrowths of epidote and calcite.
Epidote may attack feldspar (especially relict plagioclase phenocrysts), rarely causing a
greenish tinge in hand sample. Feldspars also may be partially converted to clays. No
epidote ± chlorite ± magnetite patches have been observed in the porphyry dikes.
25
Alteration Geochemistry
Selected whole-rock analyses (Appendix B) reported here and by Bolin (1976),
Langton and Williams (1982), and Lang and Titley (1998) parallel the mineralogical
patterns. In potassium silicate assemblages, addition of potassium and the correlated loss
of sodium and calcium drives the compositions upward in Figures 2A and 2C and
downward in Figure 2D. This common behavior is often misinterpreted as indicating
particularly K-rich igneous compositions (cf. Jensen and Barton, 2000). Plotting the CaO
+ Na2O, K2O, and Al2O3 molar proportions on a ternary diagram (Fig. 4A) shows that the
most samples have not been subjected to intense hydrolytic alteration, though “porphyry
altered to quartz-sericite” and “biotitized core zone” andesite from Langton and Williams
(1982) clearly show alkali loss. Elemental gains and losses associated with hydrothermal
alteration are shown in Figure 4B. Strong potassic alteration (quartz + K-feldspar +
magnetite + biotite alteration as described above) results in increased Si and K (and
possibly Fe) with corresponding decreases in Na, Ca, and Mg. Ore metals such as Cu, Au,
and Ag are also enriched (as evidenced by core logging and petrography), though these
increases are not quantifiable with data from this study.. This intense alteration removes
rare-earth elements and results in concentrations as low as ~25-50% of their levels in less
altered rocks (Fig. 2F). The most intense alteration results in significant iron addition
(Sample U-2, Fig 4B); most samples show little to no increase, indicating that their
magnetite either is indigenous or formed from the oxidation of ferrous iron in the original
mafic minerals. Andesite on the fringes of the deposit contains roughly 1.9%
K2O, whereas K2O concentrations in the core are nearly 4% (see Fig. 16.7, Langton and
26
Williams, 1982). While this is approximately 100% increase, it still represents a relatively
modest addition of only 2%. This addition of K is offset by a roughly equivalent decrease
in Na + Ca.
Less intense potassic alteration (biotite + K-feldspar + magnetite alteration)
results in increased Si, K, Rb, and Ba but decreased Fe. Geochemical data also shows that
biotitization does not necessarily correlate with strong potassium addition (Fig. 4B),
because nearly all of the samples have several tens of percent biotite, yet most do not
show pronounced addition of potassium.
Vein Types and Paragenesis
Hydrothermal veins at Dos Pobres are diverse. The observed veins have been
divided into three groups based on the mineralogy of the veins and their associated
alteration envelopes; some of these groups contain several subtypes. Crosscutting
relationships have enabled the construction of a timeline of the relative ages of veins.
Vein types are summarized in Table 2.
Veins Associated with Potassic Alteration
The greatest number and diversity of veins are associated with potassic alteration.
They are most abundant proximal to the porphyry dikes but persist throughout the
observed extent of the deposit. They are divided into the following seven types (Table 2).
27
Hairline biotite - The earliest observed veins are hairline ( 1 mm thick) biotite
veins that are rare and typically contain small (<1 mm) clots of bornite, magnetite, and/or
anhydrite. These veins are only observed in intensely altered andesite in the core of Dos
Pobres.
Sugary quartz – The most abundant early vein type at Dos Pobres consists of
sugary-textured quartz with K-feldspar, bornite and chalcopyrite, magnetite, anhydrite,
and biotite, with envelopes of K-feldspar that may also contain biotite, anhydrite,
chalcopyrite, and/or bornite (Fig. 5D, E, G, H, O). The veins can be tens of centimeters in
thickness but typically are < 1cm. These veins are a significant host of Cu and Au. They
are abundant in the center of the deposit and gradually decrease in number and width
with increasing distance.
Comb quartz - These veins are distinguished by inward-growing quartz crystals
and centerlines of K-feldspar, chalcopyrite, bornite, and/or anhydrite (Fig. 5E). They may
contain chalcopyrite, bornite, and/or minor molybdenite intergrown with the quartz; the
veins are typically 1-10 mm in thickness. They commonly lack alteration halos, but
where present they consist of K-feldspar. These veins can be difficult to distinguish from
sugary quartz veins, and they are clearly cut by green mica veins. Their distribution is
similar to that of sugary quartz veins.
Complex biotite - These are thin ( 5 mm) rare veins dominated by biotite. The
vein fill consists of biotite, anhydrite, quartz, and K-feldspar. They have envelopes
containing biotite, magnetite, quartz, and sulfides (chalcopyrite > pyrite > bornite) that
are typically zoned from inner biotite + quartz + magnetite + sulfide to outer quartz
28
and alkali feldspar (Fig. 5F, M, L). These veins appear to cut sugary quartz veins, though
documented crosscutting relationships are few. They are present throughout the deposit,
but their scarcity makes their distribution and timing difficult to constrain.
Green mica - These are 1-5 mm thick veins containing biotite, sericite, bornite
and chalcopyrite, andalusite, and K-feldspar with thick (3-20 mm), zoned alteration
envelopes dominated by biotite (commonly replaced by chlorite) and sericite (Fig. 5G, I,
J). Monazite is uncommonly present as a trace constituent. Green mica veins are common
throughout the deposit, persisting well outside the significant Cu mineralization.
Proximal examples are Cu-rich (bornite- and/or chalcopyrite-bearing) whereas distal
veins are typically devoid of sulfides. They can be difficult to distinguish from complex
biotite veins, especially in the porphyry dikes. These veins clearly cut sugary quartz and
comb quartz veins.
Magnetite-dominated veins – These are deep veins that commonly contain
chalcopyrite, with some examples also containing biotite and/or anhydrite. They locally
have white envelopes consisting of quartz and alkali feldspar (Fig. 5K) but commonly do
not have envelopes. Typical widths are 2-5 mm. These were observed cutting complex
biotite veins, and they very commonly show evidence of superimposed low-temperature
alteration, typically consisting of pyrite, chlorite, epidote, and zeolite minerals (Fig. 5L).
Magnetite-dominated veins were observed only in the andesites and are especially
common in deep distal regions.
Molybdenite veins – These are rare planar veins continuous for several meters
consisting of molybdenite and lesser quartz with no alteration envelopes. Typical widths
29
are 2 mm (Fig. 5M). They have been observed cutting sugary quartz, comb quartz, and
complex biotite veins. Molybdenite from one of these veins yielded a Re-Os age of 60.9
± 0.3 Ma (Appendix A). They are quite rare, and thus their distribution is uncertain.
Veins Associated with Hydrolytic Alteration
Sulfide-sericite – Veins consisting of massive sulfide with strong sericite +
chlorite alteration envelopes are the most common type associated with sericitic
alteration (Fig. 5E, F, O). These veins typically are 2-5 mm thick. Chalcopyrite is the
most common sulfide mineral and minor bornite or pyrite is commonly present; bornite
and pyrite have never been observed in equilibrium. Minor sericite and chlorite are
commonly present in the vein fill, and molybdenite is typically a minor constituent.
Sericite and lesser chlorite dominate the envelopes, which are typically 3-5 times vein
width. These commonly reopen sugary and comb quartz veins. Molybdenite from one of
these veins yielded an age of 60.4±0.3 Ma (Appendix A). These veins are most common
in a ring-shaped zone surrounding the core of the deposit and are rarely present in the
deposit center or distally.
Clotty sulfide-chlorite – These are thin ( 2 mm) veins with clots of chlorite and
sulfide (chalcopyrite and/or pyrite) and sericitic (sericite ± chlorite) envelopes. These
may be thin equivalents of sulfide-sericite veins. These veins are common throughout the
deposit and cut all potassic veins.
Anhydrite-dominated veins – These veins are rare and are dominated by anhydrite
and quartz (Fig. 5K). Envelopes typically contain anhydrite, quartz, sericite, and chlorite;
30
these veins were only observed in andesite, and were only common in one drill hole in
the north-central portion of the deposit.
Veins Associated with Low-Temperature Alteration
Chlorite-pyrite veins – These veins are planar, have sharp edges and even widths,
and are dominated by chlorite with lesser pyrite (Fig. 5N). They are rare and have weakly
defined actinolite-bearing envelopes. Their distribution and timing is difficult to constrain
due to their rarity, but they likely represent a transition between hydrolytic and propylitic
alteration types.
Propylitic veins - Veins containing quartz, chlorite, pyrite (locally chalcopyrite),
epidote, and calcite are associated with propylitic alteration. These veins are common on
the fringes of the deposit but rare in the higher-grade portions. These veins typically vary
in thickness from 1-5 mm. They are mineralogically variable, but have distinctive white
and green speckled envelopes that may be weakly zoned from inner quartz to outer
chlorite (Fig. 5I, L). These also commonly reopen older veins.
Base-metal veins – Veins with Cu-Pb-Zn sulfides and no visible envelopes were
observed in one location (from the central bornite-dominated zone). The veins are 2-3
mm wide and consist dominantly of calcite with, sphalerite, chalcopyrite, galena, and
pyrite.
Zeolite-dominated veins - The latest veins observed are dominated by various
white to pink-orange zeolite minerals, which very commonly reopen, shatter, and cement
earlier veins or fill jagged fractures (Fig. 5J, O), indicating formation in open space.
31
Many zeolite species are present, but stilbite-stellarite and heulandite are most common;
calcite is variably present. Their thickness ranges from 1-10 mm. These veins are
ubiquitous but their abundance varies widely, ranging from nearly zero locally to
upwards of 10% in heavily fractured areas.
Mineralogy of Sulfides and Precious Metals
Sulfide minerals were observed and recorded during core logging and
petrography, and precious metal minerals were observed and recorded using petrography
and electron microprobe work involving mainly back-scattered electron (BSE) images
and energy-dispersive X-ray spectroscopy (EDS). Langton and Williams (1982) reported
the presence of precious metals as hessite (Ag 2Te) and sylvanite [(Au,Ag)2Te4] occurring
within bornite grains. Descriptions of sulfides and precious metals observed in each vein
type will be is followed by a synthesis of deposit-scale metal distributions
Potassic Veins
Based on observations during core logging and petrography, the group of veins
that exhibit potassic alteration envelopes host most of the copper and practically all of the
gold in Dos Pobres. The sulfides in these veins are dominated by bornite and chalcopyrite
and have not been observed containing any cogenetic pyrite, although local sulfidation of
bornite and chalcopyrite to pyrite is observed near later veins. In bornite-dominated
veins, the grains commonly show chalcocite-digenite with an exsolution texture (Fig. 6A,
B, D, F). The majority of precious metals that were observed occur in bornite-dominated
32
veins, with or without this exsolution texture. They occur as hessite, sylvanite, electrum
(~85:15 Au:Ag), and possibly calaverite (AuTe2) embedded in bornite; most grains are
10 m in diameter (Fig. 6A, B). Bornite in some green mica veins contains wittichenite
(Cu3BiS3) within the exsolved chalcocite (Fig. 6D), and certain chalcopyrite grains rarely
have associated acanthite (Ag2S). Galena (with up to ~20% Se) commonly forms in
fractures and on grain boundaries of sulfides and may have associated hessite (Fig. 6E,
G). Sylvanite does not occur in this manner. In one sample, magnetite pseudomorphing
specular hematite was observed intergrown with bornite-chalcocite (Fig 6F).
Hydrolytic Veins
Drill core observations show that these veins also host considerable Cu, largely as
chalcopyrite (Table 2), but microprobe study indicates that these veins contain very little
Au. Silver is present as evidenced by galena and minor hessite commonly present on the
edges of grains and in fractures. Although bornite does uncommonly occur in certain
hydrolytic veins, no precious metals were found in the bornite contained in these veins, in
contrast
to
bornite
contained
in
veins
that
exhibit
potassic
envelopes. Microprobe observations indicate that chalcopyrite in some sulfide-sericite
veins may have rare tiny (<10 μm) inclusions of unidentified Sn- or Zn-bearing nonsulfide minerals.
Low-Temperature Veins
Propylitic veins were observed in drill core to be only a minor host of Cu, which
occurs only as chalcopyrite and typically subordinate to pyrite. Microprobe analyses
33
shows that these veins do not carry gold, though galena and minor hessite are commonly
found on grain boundaries and in fractures, as in other vein types. Base-metal veins
contain Cu, Pb, and Zn, but no precious metals were observed.
Spatial Distribution of Alteration-Mineralization Features
Alteration and Vein Distribution
Distribution of alteration is shown in Fig. 7A and B. Potassic alteration is
overwhelmingly dominant, with propylitic alteration increasing distally. Potassic
alteration is locally overprinted by discontinuous patches of hydrolytic alteration; this
alteration type may be limited to vein envelopes. Biotite + amphibole alteration is
uncommonly present in outlying holes. The intensity of K-silicate alteration decreases
with distance from the locus of intrusion. Moderate to weak K-silicate alteration is
present in andesite for considerable distances (> 1,000 m), persisting far outside the limits
of significant known Cu mineralization. A small amount of biotite-cemented breccia was
observed at one location; the matrix consists of biotite, bornite, quartz, and zeolites, and
the clasts are andesite fragments altered to quartz + biotite.
Many of the vein types were not distinguished at the outset of core logging; some
were distinguished only after subsequent petrography; and certain types occur only
sparsely. Although qualitative observations on distribution and abundance have been
noted in the descriptions above (e.g., more abundant in proximal than distal locations,
etc.), estimates of abundance either are not available for most vein types or cannot be
34
confidently contoured in plan or cross section with the data gathered in this study.
However, semi-quantitative estimates of the abundance of quartz veins (combining
sugary and comb quartz veins) are shown in Figures 7 E and F. Quartz veins are most
abundant (~25 vol %) in the strong quartz + K-feldspar + magnetite + biotite alteration
zone in the core of the deposit. Their abundance decreases rapidly to <10% but remains
above 1% for several hundred meters.
Sulfide and Metal Zoning
The distribution of the dominant sulfide minerals is shown in Figures 7 C and D.
Bornite content increases with depth and proximity to the deposit center, thus bornitedominated veins form an inverted cone-shaped zone. Chalcopyrite content increases
outward, forming a zone of chalcopyrite-dominated veins that surrounds the bornite core
and gradually yields to pyrite. Veins with potassic (K-feldspar ± biotite) envelopes host
early Cu mineralization (primarily bornite + chalcopyrite), and veins with sericite ±
chlorite envelopes dominate late mineralization (chalcopyrite ± bornite or pyrite). Copper
grade contours (from Langton and Williams, 1982) are shown in Fig. 1D above; they
reach a maximum of approximately 2% Cu.
The highest molybdenum concentrations (~0.01 % MoS2) occur in a ring-shaped
zone that broadly coincides with the greatest intensity of hydrolytic alteration, with
Cu:Mo ratios ranging from >1000:1 in the Mo-poor core to ~35:1 in the areas with more
abundant sericitic veinlets (Fig. 16.6 of Langton and Williams, 1982).
35
Most precious metals at Dos Pobres are embedded in bornite grains, with textures
suggesting having been exsolution at high temperatures from a solid solution; therefore,
grades of Au and Ag are highest in the bornite-dominated core (Figs. 16.9 and 16.10 of
Langton and Williams, 1982). They are observed in most types of “potassic” veins
(excluding magnetite-dominated and molybdenite veins), but sugary quartz veins are the
dominant host due to their greater abundance. Gold content is highest in the core of the
deposit and decreases outward; silver follows the same distribution and Ag:Au ratios
range from ~10:1 in the Au-rich core to >100:1 in the fringes (Figs. 16.9 and 16.10,
Langton and Williams, 1982). Aside from occurrences related to potassic veins, silver
occurs on the edges of and in fractures in sulfide grains, perhaps deposited via adsorption
under hypogene conditions (e.g., Simon et al., 2000). The occurrence of precious metals
mainly within bornite and as small grains is metallurgically favorable because most
would report to the concentrate rather than be lost to the tailings.
Supergene Features
The Dos Pobres system has been thoroughly oxidized and partially leached to a
depth of ~350 m (Langton and Williams, 1982; Wilson, 2004). Wilson (2004) reports that
the leached capping at Dos Pobres is dominated by hematite; this is interpreted to be a
result of oxidation of iron-bearing mafic minerals in addition to hypogene metal sulfides.
Oxide copper minerals (neotocite [tenorite?], cuprite, and chrysocolla) are visible in the
center of the surface exposure but chalcocite is uncommon. Goethite-dominated capping
occurs in areas where oxidation of mafic minerals was minor; this capping style is
36
interpreted to represent oxidation of hypogene sulfide minerals only (Wilson, 2004). Due
to the low pyrite:(chalcopyrite + bornite) ratio of the ores and pH buffering capacity of
the wall rocks at Dos Pobres, mobilization of copper was limited. In the mixed oxidesulfide zone, native copper, chalcocite, and covellite are abundant (Langton and
Williams, 1982).
At the deeper levels examined in this study, supergene bornite and chalcocite
commonly partially replace hypogene sulfide grains, typically as thin rims
near zones of fracturing. Supergene bornite has only been observed replacing
chalcopyrite; supergene chalcocite replaces bornite and chalcopyrite. In local areas of
heavy fracturing, sulfides may be completely oxidized. Covellite is typically absent but is
locally abundant in the mixed oxide-sulfide zone and is associated with rare hawleyite
(CdS) (Fig. 6H).
Fluid Inclusion Observations
The petrographic characteristics of fluid inclusions were observed, but no heating
or freezing experiments were conducted. Diverse fluid inclusion types occur in
hydrothermal quartz as summarized in Table 3. Most inclusions are small ( 10 m).
Many are interpreted to be of secondary origin by the criteria of Roedder (1984), but a
significant fraction of equant (commonly exhibiting negative crystal forms) lack obvious
secondary characteristics and are irregularly scattered in unstrained quartz. An aqueous
liquid, lesser vapor, and – typically – one or more daughter minerals fill the inclusions.
Daughter minerals include equant salts (most commonly a single cubic crystal = halite)
37
and lesser opaque (triangles = chalcopyrite, red equant = hematite) and elongate
birefringent minerals.
Inclusions in early proximal veins associated with intense potassic alteration
contain abundant daughter minerals, including halite and other phases. The abundance of
opaque and birefringent daughter minerals decreases rapidly with distance from the
bornite-rich core of the deposit and in time, as inferred from paragenesis of vein types.
Halite-bearing inclusions are common in later and more distal veins such as those with
sericitic envelopes, but inclusions in propylitic (late and typically distal) veins have no
daughter minerals. Opaque minerals and elongate birefringent daughter minerals are
associated with the quartz-bearing potassic vein types (sugary quartz, comb quartz,
complex biotite). Quartz veins associated with sericitic alteration have more abundant
liquid-vapor inclusions, but halite and opaque-bearing inclusions are rarely present and
may indicate that the quartz containing those inclusions formed as part of an earlier vein
assemblage. Quartz in propylitic veins contains only liquid-vapor inclusions, many of
which have larger bubbles than those observed in other veins.
Time-Space Evolution
The porphyry dikes are sufficiently similar in appearance and composition that the
number of distinct intrusions is uncertain. The U-Pb ages are well within error (57.2 ±
0.9, 57.2 ± 1.2, 57.0 ± 1.1 Ma; Appendix A), but several factors point to more than one
intrusive event. The variable abundance of embayed quartz phenocrysts, the marked
differences in alteration intensity between dikes, and the observation of sugary quartz
38
veins truncated at contacts all require multiple intrusive events. The facts that no
truncated veins of other types were observed and that no reversals in offsetting vein
relationships (in the sense of Seedorff and Einaudi, 2004) were noted imply that the
intrusions were emplaced in fairly rapid succession, before lower-temperature
assemblages (e.g. quartz + sericite + chlorite + pyrite ± chalcopyrite) became stable. The
vein types observed thus appear to represent a single overall thermal event. With the rare
exception of sugary quartz veins truncated at intrusive contacts, there is no evidence of
hydrothermal reversals (multiple events with similar features).
The paragenesis of the ore mineralogy is also typical of many gold-bearing
porphyry copper deposits (Sillitoe, 2000). During early potassic alteration, bornite and
precious metals have a direct correlation (indicating deposition by the same fluid).
Chalcopyrite dominates the later moderate-temperature assemblages, which contain the
highest concentrations of molybdenum but have very low concentrations of precious
metals.
The ages of the porphyry dikes and andesites are well within the expected ranges
for this region. The difference between the ages of the porphyry dikes (~57.1 Ma) and the
host andesite (67 - 73 Ma) demonstrates that they are not coeval, as others have suggested
(Dunn, 1978; Langton and Williams, 1982). The Re-Os age of molybdenite
mineralization (60.4 ± 0.3 and 60.9 ± 0.3 Ma) is enigmatic, being older than the porphyry
dikes (~57 Ma). This is probably a result of disturbance in the Re-Os isotopic system.
This is not the only deposit in which molybdenite Re-Os geochronology has yielded ages
that are significantly older than those obtained by other methods (cf. Raul-Condestable,
39
Peru; De Haller et al., 2006). The two Re-Os dates overlap within error, even though their
rhenium concentrations differ by nearly a factor of 10 (Appendix A).
The presence of possible anhydrite phenocrysts in the porphyry dikes is
important, since their presence indicates that the magma had a high oxidation state. While
hardly common, anhydrite phenocrysts have been reported from a few other deposits,
including Santa Rita, New Mexico (Audétat et al., 2004) and Endeavour (Lickfold
et al., 2003).
A schematic cross section through the core of the deposit is shown in Figure 8
showing the time-space evolution of Dos Pobres. In panel A, porphyry dikes were
emplaced, causing intense potassic alteration and the formation of sugary quartz veins. In
panel B, the continued emplacement of dikes caused the continuation of sugary quartz
vein formation, along with weaker widespread potassic alteration and the formation of
the other potassic vein types. In panel C, as temperature drops, hydrolytic alteration is
superimposed on the earlier potassic. Later propylitic alteration weakly overprints the
entire system. Panel D shows the deposit in its current state, after faulting, tilting,
weathering, and erosion.
Discussion
Comparison of Alteration, Veins, and Ore Mineralogy
A distinctive K-rich, acid-poor alteration package has long been recognized as a
feature of many gold-rich porphyry deposits (Hollister, 1975; Sillitoe, 1979). Most have a
40
potassic (K-feldspar + quartz ± biotite) core, which grades outward into a propylitic halo.
Intense quartz + K-feldspar alteration similar to that present at Dos Pobres is reported
from the cores of many other deposits (Sillitoe, 1979), as is widespread biotitization of
mafic minerals (Seedorff et al., 2005). Propylitic alteration with similar features to that at
Dos Pobres has been described from many other deposits. Biotite-amphibole alteration
like that described here has not been distinguished in other deposits. It may represent a
transition between potassic and propylitic alteration, since it shows some features
common to both. The high TSi content of the amphiboles in this alteration requires a low
temperature of formation.
All of the vein types described in this study are similar to reports from other
deposits. Hairline biotite and sugary quartz veins represent the early vein stages at most
porphyry copper deposits (Seedorff et al., 2005). Comb quartz veins are similar to “B”
veins at El Salvador (Gustafson and Hunt, 1975), though at Dos Pobres they can be
difficult to distinguish from sugary quartz veins and could be combined into one category
(cf. “AB” veins of Clode et al., 1999, at Batu Hijau, Indonesia.) Veins similar to complex
biotite veins have been reported from several deposits, such as Butte, Montana (“EDM”
veins of Meyer, 1965; Brimhall, 1977), El Salvador, Chile (“C” veins of Gustafson and
Quiroga,
1995),
and
Los
Pelambres,
Chile
(“type
4”
veins
of Atkinson
et al., 1996). Green mica veins have been described from other deposits, such as Butte
(Brimhall, 1977), El Salvador (“EB” veins of Gustafson and Quiroga, 1995), and Los
Pelambres (Atkinson et al., 1996). Magnetite veins have been reported at several
deposits, notably Park Premier, Utah (John, 1989), and Island Copper, British Columbia
41
(Arancibia and Clark, 1996). These veins are interpreted to be of late magmatic age, but
magnetite veins at Dos Pobres clearly formed later. Veins with sericitic and propylitic
envelopes at Dos Pobres are unremarkable, displaying features observed at many other
deposits. Zeolite veins are common in deposits that occur in mafic host rocks (Seedorff
et al. 2005).
This diversity of vein types is probably not abnormal. Unfortunately, thorough
descriptions of veins and their relative ages are lacking in many deposits, with many
authors opting instead to group veins into broad categories that fail to capture critical
differences. Comprehensive descriptions of veins and their associated alteration
envelopes are necessary if one seeks to learn about the changes in hydrothermal fluid
chemistry with time. For example, rarely described vein types such as green mica veins
and complex biotite veins can contain mineral assemblages that provide constraints on
fluid chemistry. At Dos Pobres, the assemblage K-feldspar + biotite + andalusite +
muscovite
in
green
mica
veins
constrains
temperature
to
near
600°C.
Ore mineralogy in Dos Pobres is also typical of Au-rich porphyry deposits. Gold
is always associated with potassic alteration, as described in many deposits (cf. Gustafson
and Hunt, 1975; Cuddy and Kesler, 1982; Langton and Williams, 1982; Gustafson and
Quiroga, 1995, Sillitoe, 2000), and gold and copper contents vary sympathetically (cf.
Sillitoe, 1979). Electrum is the dominant gold mineral, and it is always associated with
bornite. The abundance of precious metal tellurides is unusual, but there are other
documented examples of this style of mineralization, such as Granisle and Bell, British
42
Columbia, Canada (Cuddy and Kesler, 1982), Almalyk, Pakistan (Shayakubov
et al., 1999), Bingham, Utah (Redmond and Einaudi, 2000), Goonumbla, New South
Wales, Australia (Heithersay and Walshe, 1995), and numerous other deposits for which
mineralogic studies have been conducted on concentrates (Tarkian and Stribrny, 1999).
Minerals containing other uncommon elements, such as the Bi and Sn that were noted in
this study of Dos Pobres, are common in the base-metal lode environment of porphyry
systems (e.g., Meyer et al., 1968; Einaudi, 1982; Takagi and Brimhall, 1999), but trace
occurrences of such phases occasionally are reported from porphyry deposits worldwide
that lack advanced argillic alteration (e.g., Tarkian and Stribrny, 1999; Redmond and
Einaudi, 2000).These rare occurrences are of geochemical curiosity but generally have
little practical (e.g., metallurgical) consequence.
Although Dos Pobres is the best documented Cu-(Au-Mo) porphyry deposit in
Arizona, there are some Arizona deposits with which it shares some characteristics. The
Ajo deposit has a strongly biotitized core with bornite-chalcopyrite mineralization
(Gilluly, 1946; Dixon, 1966), with a reported mill production of 399 million metric
tonnes at 0.80 percent Cu, 0.005 percent Mo, and 0.34 g/t Au (Long, 1995). However,
extremely coarse-grained (~1 cm) hydrothermal biotite is present in the core of the Ajo
deposit, whereas the coarsest hydrothermal biotite at Dos Pobres is barely megascopic.
Additionally, magnetite at Ajo is seemingly less common than at Dos Pobres. Gold also
has been produced from the Bisbee deposits and the Courtland-Gleeson mining district
(Lang et al., 2001; Stegen et al., 2005), but only from carbonate replacement bodies
peripheral to the porphyry deposits themselves.
43
Comparison with Porphyry Cu-Mo systems
The porphyry Cu-Mo class includes most of the world’s largest known deposits,
such as Chuquicamata, Chile, Morenci, Arizona, and Resolution, Arizona, as well as
many of the smaller porphyry deposits in southwestern North America (Seedorff
et al., 2005). They are most commonly associated with quartz monzodioritic to granitic
intrusions. Chalcopyrite is the most common copper mineral (bornite is absent in some
districts), and hydrolytic alteration is typically intense and voluminous. Molybdenum is
much more abundant in these deposits, and precious metals (especially gold) are much
less abundant than in Cu-(Au-Mo) deposits.
Since the recognition of the geologically real difference between Mo- and Au-rich
porphyry copper deposits (Kesler, 1973), there have been many hypotheses concerning
the differences in the origins of the two deposit types. The observation that porphyry
deposits formed in island arc environments tend to be Au-rich while deposits formed in
continental arcs are typically Mo-rich was made early in the discussion (Kesler, 1973).
This observation led to the hypothesis that the composition of the crust through which the
magmas traveled and in which they are emplaced influences the abundance of these
metals. As noted by Gustafson (1978) and others, many deposits (including Dos Pobres)
do not follow this trend, and this idea was dismissed by Sillitoe (1979). Emplacement
depth and wall-rock permeability were also hypothesized to have some effect (Kesler,
1973), though these have also since been ruled out. Titley (1982) proposed that the two
deposit types simply represent different levels of exposure in broadly similar systems, but
this view has also been dismissed based on greater vertical exposure at many deposits of
44
both types (Sillitoe, 2000). Composition of the mineralizing intrusions is important
(Seedorff et al., 2005), but observations of closely associated compositionally identical
plutons with different styles of mineralization (i.e., Saindak, Pakistan; Sillitoe, 1979), as
well as substantial compositional overlap between classes (Fig. 8C, Seedorff et al., 2005)
imply that this is not the sole factor. In light of all of these observations, igneous rock
composition coupled with complex geochemical processes during the production,
emplacement, and crystallization of the productive magmas (as suggested by Sillitoe,
2000) appear to control the style of mineralization.
While little is known about the sulfide portions of Lone Star, San Juan, and
Sanchez, what information is available suggests that there may be significant differences
between them and Dos Pobres. Thus as the Safford district is further explored, it may
present an uncommon opportunity to study the relationships between Cu-Au and Cu-Mo
porphyry systems. All four deposits certainly formed in a continental arc environment,
and there is no evidence to suggest that the deposits were emplaced or are exposed at
significantly different levels. Geochronologic and field evidence suggest that the deposits
all were emplaced within a few million years of each other, attesting that the source
magmas traveled through the same underlying crust and likely have a shared origin.
Similarly, we can rule out the possibility of influence from wall-rock chemistry or
permeability since the Safford Volcanics host all four deposits. However, further
speculation is impractical until more information becomes available.
There are also other variables to consider. An injection of mafic magma into a
silicic magma chamber may affect the type of mineralization formed, such as at Bingham
45
(Keith et al., 1997). Many volcanic arcs show evolution from mafic to felsic over time,
and produce different mineralization types at different stages (Barton, 1990; 1996); this
factor may be particularly important, since Dos Pobres is slightly older than the other
deposits in the Safford district (M. D. Barton, unpub. data). The more primitive Nd
value for the Dos Pobres porphyry relative to the porphyries at the Lone Star deposit also
is interesting (Lang and Titley, 1998). It seems that some fundamental change may have
taken place in the Safford district, in which the magmas changed from the more primitive
type present at Dos Pobres to the more evolved type seen in the other deposits.
Comparison with Fe-oxide(-Cu-Au) Systems
Selected shared features between Au-rich porphyry systems and andesite-hosted
iron-oxide(-Cu-Au) (IOCG) systems, such as Candelaria, Chile, have stimulated
comparisons (e.g., Ryan et al., 1995; Barton and Johnson, 2000). Indeed, the abundance
of magnetite in many Au-bearing porphyry deposits coupled with scattered reports of
sodic- and potassic-calcic alteration (e.g., Dilles et al., 1995; Lang et al., 1995) has led
some to speculate a genetic link between this deposit type and IOCG deposits (Marschik
and Fontboté, 2001). However, the differences between the two deposit types are more
significant than their similarities. By definition, porphyry deposits show a clear genetic
relationship with intrusive rocks, whereas the link between magmatism and IOCG
deposition is not fully understood. IOCG deposits typically have extensive sodic- and/or
potassic-calcic alteration, whereas such alteration in porphyry deposits (such as Dos
Pobres) is commonly absent and limited in scope where present. IOCG deposits
46
commonly are enriched in cobalt, nickel, and REE, while Dos Pobres shows no such
enrichment. Quartz veins are abundant in nearly all porphyry deposits, whereas
hydrothermal quartz in IOCG deposits is comparatively sparse. Most IOCG deposits
contain several tens of percent iron oxide, but magnetite content in porphyry deposits
rarely reaches 10%. In light of these observations, the resemblance between Cu-Au-Mo
porphyry deposits and IOCG deposits appears to be only superficial.
Conclusions
Dos Pobres is a typical Cu(-Au-Mo) deposit. Its alteration assemblages and
mineralization styles are typical of the deposit type, as outlined by Sillitoe (2000). The
ore deposit was formed by the devolatilization of porphyry dikes and the subsequent
cooling of those magmatic fluids, resulting in deposition of voluminous quartz veins and
Cu-Fe sulfide minerals. We expect that as more deposits are discovered and described,
the characteristics of Dos Pobres will closely resemble many more Cu-Au-Mo deposits
worldwide.
Acknowledgments
This work was undertaken as the senior author’s Masters Thesis at the University
of Arizona guided by committee members Mark Barton, Eric Seedorff, and Jon Patchett.
Primary funding for this project and permission to publish this report were provided by
Phelps Dodge, now a part of Freeport-McMoRan Copper and Gold, Inc., and are
gratefully acknowledged. Related work was funded through NSF grant EAR 02-30091,
47
the U.S. Geological Survey Porphyry Copper Life Cycle Project, and the University of
Arizona-U.S.G.S Center for Mineral Resources. We thank Jeff Gerwe, Ralph Stegen, and
Bill Stavast for providing access to drill core and relevant data as well as support and
ideas throughout the process; we also appreciate their reviews of this manuscript.
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Titley, S.R., 1978, Copper, molybdenum, and gold content of some porphyry copper
systems of the southwestern and western Pacific: ECONOMIC GEOLOGY, v. 73, p.
977-981.
56
Williams, S.A., and Forrester, J.D., 1995, Characteristics of porphyry copper deposits:
Arizona Geological Society Digest 20, p. 21-34.
Wilson, A.J., Cooke, D.R., and Harper, B.L., 2003, The Ridgeway gold-copper deposit: A
high-grade alkalic porphyry deposit in the Lachlan fold belt, New South Wales,
Australia: ECONOMIC GEOLOGY, v. 98, p. 1637-1666.
Wilson, B., 2004, Characterization of leached capping at the Dos Pobres copper
porphyry, Graham County, Arizona: Unpublished M.S. thesis, Tucson, Arizona,
University of Arizona, 91 p.
57
Figure Captions
Fig. 1: Location maps. (A) Arizona, showing location of the Safford mining district. (B) Enlargement of the Safford
mining district (modified from Langton and Williams, 1982). The town of Safford is 13 km SSW of Dos Pobres.
(C) Surface map of Dos Pobres (modified from Langton and Williams, 1982). (D) 2000 ft (600 m) level map of Dos
Pobres showing grade contours from Langton and Williams (1982).
Fig. 2: Rock geochemical plots. Triangles are Safford andesites, circles are porphyries. Gray symbols represent
intense alteration; black symbols are data from Langton and Williams (1982) or Lang and Titley (1998). (A) Total
alkali vs. silica plot, showing fields of Le Maitre et al., (1989) and approximate composition of Safford andesites
before the intrusion of the porphyry. (B) La/Yb vs. Sc/Ni andesite discrimination plot showing Safford andesites
and classification fields of Bailey (1981). (C) K2O vs. silica plot showing alteration type paths and fields of
Rickwood (1989). (D) A/(N+K) vs. A/(C+N+K) plot. (E) IUGS diagram showing normative compositions of
Safford rocks and fields of Streckheisen (1974). The gray shaded area in the lower right is the basalt/andesite field.
(F) Chondrite-normalized REE plots of Safford district rocks, using the normalization of Anders and Grevesse
(1989).
Fig. 3: Mineral composition plots. (A) Amphibole compositions, showing fields from Leake (1978). Higher
tetrahedral silicon (TSi) indicates lower crystallization temperature. Samples with lower TSi may be relict igneous
hornblende. (B) Biotite compositions, markers corresponding to the alteration packages with which the samples are
associated.
Fig. 4: Alteration geochemical plots: (A) Al2O3-Na2O+CaO-K2O ternary plot (molar proportions) showing ‘fresh’
rock compositions (gray oval). Inset shows alteration type paths. (B) Spider diagram showing the effect of
alteration on chemical components in the porphyry dikes. Samples are normalized to
Al2O3 in the least-altered porphyry. Samples U-2 and U-3 have intense potassic alteration; the other Dos Pobres
samples have weak-moderate potassic alteration. One sample is “porphyry altered to quartz-sericite” from Langton
and Williams (1982), which shows hydrolytic alteration superimposed on potassic.
Fig. 5: Photos of rocks, veins, and age relationships. Scale bar is 1 cm except where noted. Vein and envelope
terminology is: vein mineral(s)//envelope mineral(s); i.e. a quartz + bornite vein with a biotite envelope is qtz-bn//
bio. (A) Least altered porphyry, with weak biotitic and later weak chl + ep ± cal alteration. Mafic minerals are
converted to biotite (some to chl + ep) and feldspars are partially altered to sericite+clay. (B) Porphyry showing
weak hydrolytic alteration and a possible anhydrite phenocryst. (C) Intense qtz + kfs + mt alteration in andesite.
Groundmass is replaced by irregular masses of K-feldspar and magnetite which are cut by sugary quartz (qtz-kfsmt//-) veins. (D) Photomicrograph (crossed polarizers) of biotite-amphibole-magnetite alteration developed in
amygdaloidal (?) andesite. “Amygdule” is filled with biotite and amphibole and cut by a sugary quartz (qtz-anh//
bio) vein; the groundmass is darkened by fine magnetite. (E) Sugary quartz (qtz-bn//kfs) veins developed in
porphyry cut by a comb quartz (qtz-cpy-anh-bn//-) vein, which is in turn cut by a sulfide-sericite (cpy-serbn//ser+chl) vein. (F) Complex biotite (bio-qtz-mt-kfs-bn-cpy-cal-zeol//bio-qtz-kfs) vein cut by a sulfide sericite
(cpy-ser-chl-anh//ser-chl) vein that has reopened a sugary quartz (qtz+bn//bio) vein in andesite. (G) Green mica
(bio-ser-cpy-bn-mt//bio-ser-kfs) vein cutting a sugary quartz (qtz-kfs-bn-bio//-) vein in fragmental andesite. (H)
Propylitic alteration in andesite, with patches of intense epidote alteration. A narrow sugary quartz veinlet (qtz//bio)
is reopened by zeolites. (I) Green mica (?) (chl[after bio?]-cpy-ser//ser) vein cut by propylitic (cpy-qtz-cal-chlzeol//qtz-chl-ep-ser) vein in andesite. (J) Green mica (?) (bio-cpy-kfs//bio) vein cut by numerous zeolite veins in
andesite. (K) Anhydrite-dominated (anh-qtz-cpy) vein with zoned (inner qtz, outer chl) envelope cuts (cross cutting
58
relationship not shown) a magnetite-dominated (mt-anh-cpy-bio//qtz) vein in andesite. (L) Complex biotite (biokfs-qtz-cpy-cal-chl[after bio]//bio-qtz) vein cut by a magnetite-dominated (mt-cpy-qtz-zeol-cal//qtz) vein in
andesite. A propylitic (cpy-qtz-chl-ep//qtz-chl-ser) vein is shown in the corner of the sample. (M) Molybenite
(moly-qtz//-) vein cuts complex biotite (qtz-bio-cal-kfs-cpy-bn//qtz-bio) and comb quartz (qtz-cpy-kfs//-) veins in
andesite. (N) Chlorite-pyrite (chl-pyr-qtz//bio-amph) vein cuts quartz veinlets in andesite with biotite + amphibole
+ magnetite alteration. (O) Complex cross cutting relationship in andesite with a sulfide-sericite (cpy-moly//?) vein
that has reopened a sugary quartz (qtz-bn//-) vein, and has been reopened by zeolites which fracture and embed
fragments of the earlier veins. Amph = amphibole, anh = anhydrite, bio = biotite, bn = bornite, cal = calcite, chl =
chlorite, cpy = chalcopyrite, ep = epidote, kfs = K-feldspar, mt = magnetite, moly = molybdenite, pyr = pyrite, qtz =
quartz, ser = sericite, zeol = zeolite minerals.
Fig. 6: Ore photos: (A) and (B) Bornite (Bn) with bluish gray exsolved chalcocite (Cc) and native gold (Au). (C)
Bornite with gold and sylvanite (Sylv, [Au,Ag]2Te4). (D) Bornite with chalcocite and wittichenite
(Cu3BiS3). (E) Hessite (Hess, Ag2Te) and galena (Gal) deposited on the edge of chalcopyrite (Cpy). (F) Bornite with
chalcocite and associated magnetite (Mt) pseudomorph after hematite (Hm). (G) Back-scattered electron (BSE)
image of galena and hessite deposited along a grain boundary between bornite and chalcopyrite. (H) BSE image of
chalcocite and covellite (Cov) with associated hawleyite (CdS).
Fig. 7: Plan maps and cross sections. Gray bars in cross sections are logged intervals, vertical scale is elevation in
feet. (A) and (B) Plan map and cross section showing dominant alteration type. (C) and (D) Plan map and cross
section showing dominant sulfide mineral. (E) and (F) Plan map and cross section showing quartz vein abundance.
Fig. 8: Cartoon cross section showing formation of hydrothermal features and subsequent faulting and tilting at Dos
Pobres. (A) Intrusion of early porphyry dikes into andesite and development of intense potassic alteration. (B)
Intrusion of later dikes and widespread weaker potassic alteration. (C) Formation of weak hydrolytic (sericitic) and
propylitic alteration. (D) Faulting, tilting, weathering, and erosion.
Figure 1
59
60
Figure 2
61
Figure 3
62
63
Figure 4
64
Figure 5
65
Figure 6
66
Figure 7
67
Figure 8
68
Table 1: Summary of Alteration Assemblages in Porphyry Dikes and Andesites
Typ
e
Host
Feldspar
sites
Mafic
sites
Andesite
kfs
bio, mt
Porphyry
kfs
bio, mt
Andesite
kfs, bio,
mt
shreddy
bio (high
Ti) ± Mt
Porphyry
kfs
Andesite
± kfs
Porphyry
± kfs
Andesite
kfs ± mt,
bio
Porphyry
-
-
-
Andesite
ser ± chl
ser ± chl
ser, chl
Porphyry
ser
ser ± chl
ser
Andesite
ser ± chl
chl ± ser
chl
Porphyry
ser
chl ± ser
ser ± chl
Andesite
± ep, chl,
cal, clay
Porphyry
± ep, chl,
cal, clay
Andesite
± ep, chl,
cal, clay
Porphyry
± ep, chl,
cal, clay
Assemblage
Potassic
associations
Quartz + K-feldspar
+ Magnetite ± Biotite
(intense)
Biotite + K-feldspar +
Magnetite (intense)
Biotite + K-feldspar +
Magnetite (weak)
Biotite + Amphibole +
Magnetite
shreddy
bio (high
Ti) ± Mt
shreddy
bio (low
Ti), mt
shreddy
bio (low
Ti), mt
act, bio
(low Ti),
mt
Groundmass
Associated vein
types (see Table 2)
qtz, kfs, mt,
bio
qtz, kfs, mt,
bio
Sugary Quartz
kfs, bio, mt
qtz, kfs, mt,
bio, anh
bio, mt
bio
mt, bio
Hairline Biotite,
Sugary Quartz,
Comb Quartz,
Magnetite-Dominated
(?), AnhydriteDominated (?)
Sugary Quartz,
Comb Quartz, Green
Mica, Complex
Biotite
Magnetite-dominated
(?), Chlorite-Pyrite (?)
Hydrolytic
associations
Sericite-Chlorite
(intense)
Sericite-Chlorite
(weak)
Sulfide-Sericite,
Clotty SulfideChlorite, Base Metal
Propylitic association
Propylitic (intense)
Propylitic (weak)
chl, ep,
sph, cal
[bio]
chl, ep,
sph, cal
[bio]
chl, ep,
sph, cal
[bio]
chl, ep,
sph, cal
[bio]
chl, ep
chl, ep
Propylitic, Zeolite
chl, ep
chl, ep
K-feldspar ± quartz ± biotite ± anhydrite [ Sugary-textured quartz-K-feldspar veins with disseminated bornite, minor biotite and anhydrite, and
± chlorite ± sericite]
rare chalcopyrite. Envelopes most commonly consist of K-feldspar, though biotite and/or K-feldspar
Table 2: Summary of Dos Pobres Vein Types
Table 3: Summary of Fluid Inclusion
Observations
Minerals present
description
Vein type
Vein Fill
Envelope
Environment
L-V
L-V-H
L-V-H-Op
Complex
Comments
Potassic
Quartz
veins
Common biotite Common
Common
Common
Inclusions with daughter
biotite ± quartz ± bornite ±magnetite
Very thin ( 1 mm), brown to black, appearing as dark lines along hairline fractures
Hairline Biotite
assoc-iated with
secondary
minerals usually have
strong
alteration
negative crystal forms
Sugary K
Quartz
quartz + K-feldspar + Cu-Fe-sulfide ±
magnetite ± anhydrite ± biotite ±
Abundance
Cu
Mo
Abundance in
Deposit
69
Observed Timing Relationships
A
-
-
R
C
R
C
Cut complex biotite, sugary quartz,
and comb quartz veins
Cut complex biotite veins (one
example), cut by anhydrite-dominated
veins (one example).
Cut sugary quartz and comb quartz
veins; cut intrusive contacts (one
example).
Cut sugary quartz veins; intrusive
contacts not observed.
Cut hairline and complex biotite veins
and sugary quartz veins, commonly
reopened by green mica and sulfidesericite veins. Cut intrusive contacts
where observed.
Cut by all other veins; intrusive
contacts not observed.
R
-
T
Cut all potassic veins; relationships
with other sericite-chlorite veins are
uncertain. Cut all intrusive contacts.
T
R
A
A
Same as above
-
-
R
C
Cut magnetite-dominated veins (one
example)
T
A
-
T
Cut sugary quartz veins (one
example), cut by propylitic veins (one
example)
A
C
-
T
T
quartz + Cu-Fe-sulfide + chlorite ± sericite sericite + quartz ± Cu-Fe-sulfide ± chlorite Most commonly occur as thin (<3mm) quartz veins with clots of sulfides and chlorite, with envelope
width approximately 3 times vein width.
± anhydrite
T
-
Cut all veins except zeolite. Not
observed in porphyry dikes.
C
Planar veins of variable width with distinctive envelopes zoned from inner quartz to outer chloritesphene
T
C
Cut sugary quartz veins
Cut hairline and complex biotite veins,
cut by all other veins; occasionally
truncated at intrusive contacts.
quartz + anhydrite + sericite + chlorite
Thin (<3 mm), planar, straight-sided veins dominated by chlorite with quartz and intermittent pyrite
and actinolite envelopes.
-
T
Cut all veins wherever present.
T
anhydrite + quartz + chalcopyrite
chlorite + actinolite
R
-
C
C
Clotty Sulfide-Chlorite
chlorite + pyrite ± quartz ± sericite
Quite variable in appearance, speckled green and white envelope can be confused with that of other
types. Commonly observed reopening earlier veins, leading to complex relationships.
C
-
molybdenite [ ± chlorite ± sericite ±
envelopes may be present in andesitic host rocks. Several observed examples are cut by breccias
Quartz veins
Common
Common
Rare
as above;
sphene ± rutile]
and
porphyry. Similar to "A"Rare
veins of Gustafson and Hunt Same
(1975).
associated with
secondary
inclusions in distal veins
Comb Quartz
quartz + K-feldspar + Cu-Fe-sulfide ±
K-feldspar ± quartz ± biotite ± anhydrite [ Dominated by inward-growing quartz with scattered sulfides, K-feldspar, and biotite. They show
weak
K
alteration
have
fewer
biotite
±
anhydrite
±
molybdenite[±
poorly- to well-defined centerlines of K-feldspar, chalcopyrite,
and/or
bornite.daughter
If present, envelopes
±
chlorite
±
sericite]
chlorite ± sericite ± calcite ]
are similar to 2b veins but not as intense. K-feldspar envelopes in andesitic host rocks are easily
minerals
overlooked in hand sample but distinctive when stained. Similar to "B" veins of Gustafson and Hunt
(1975)Rare
Quartz veins
Common
Common
Very
Very Rare
Some inclusions with
associated
with
primary
minerals may
Complex Biotite
biotite + quartz + Cu-Fe-sulfide
± K- andbiotite + Cu-Fe-sulfide + quartz ±
Very thin veins dominated by biotite with envelopesdaughter
zoned from inner biotite-quartz-sulfide
with minor
feldspar ± anhydrite [ ± chlorite ± sericite] magnetite [ ± chlorite ± sericite]
secondary chlorite-sericite to outer quartz. Possibly similar to "C" veins of Gustafson and Quiroga
sericitic alteration
secondary
be related to earlier
(1995) or "type 4" veins of Atkinson et al. (1996).
events
Green Mica
biotite + muscovite + Cu-Fe-sulfide + K- biotite + muscovite + K-feldspar + Cu-Fe- Thin (<5mm) mineralogically complex veins with lumpy irregular envelopes
zoned from inner biotite
feldspar ± anhydrite ± andalusite [ +
sulfide ± anhydrite [ + chlorite + rutile +
(usually replaced by chlorite, rutile, and titanite), sericite, and K-feldspar to outer K-feldspar. Sulfides
Quartz veins
Common
Absent
Absent
Absent
Only
inclusion
chlorite + rutile ± titanite
± epidote]
titanite ± epidote]
are commonly scattered throughout
the envelope. Possibly
similarL-V
to "green
mica" veins of Brimhall
(1977).
associated with
primary and
observed;
these are late
Magnetite-Dominated
magnetite ± pyrite ± chalcopyrite ± quartz quartz ± alkali feldspar
Wavy to planar veins up to 1 cm thick, dominated by large magnetite grains with other minerals
propylitic ± anhydrite ± actinolitesecondary,
and mostly distal veins
± epidote ±
interstitial. Common in deep distal zones
alterationchlorite
some have
Molybdenite
molybdenite ± quartz
none
Thin (<2 mm) planar veins that are continuous for several meters. Common in deep flanking zones.
large bubbles
Hydrolytic
Complex
inclusions contain elongate birefringent daughter minerals
Cu-Fe-sulfide ± quartz ± sericite ±
sericite ± chlorite ± Cu-Fe-sulfide ± quartz Typically consist of massive chalcopyrite, commonly reopening or filling residual open spaces in
Sulfide-Sericite
(anhydrite?) chlorite ± anhydrite
± molybdenite
earlier veins. Envelopes consist of coarse sericite and chlorite, in rare cases zoned from chlorite
inner to sericite (±K-feldspar) fringes. Similar to "D" veins of Gustafson and Hunt (1975).
L = liquid, V = vapor, H = halite, Op = opaques
Anhydrite-Dominated
quartz + Cu-Fe-sulfide + chlorite ± calcite quartz + chlorite + epidote ± titanite ±
± epidote ± zeolites ± amphibole
albite ± K-feldspar
Very rare veins with Zn-Pb-Cu mineralization and intense sericitic envelopes.
-
Zeolite-Dominated
Low-Temperature
Chlorite-Pyrite
Propylitic
calcite + sphalerite + chalcopyrite +
galena + pyrite + sericite
Occur as both planar and irregular veins, very commonly reopening earlier veins of all types.
Stellarite, heulandite, and phillipsite are common. Envelopes are rare; where present they consist of
clays and very fine zeolites. Commonly reopen, shatter, and cement earlier veins, hence appearing
to be Cu-Mo bearing.
sericite + chlorite
Base Metal
stellarite ± heulandite ± phillipsite ± stilbite fine-grained zeolites, clays
± laumontite ± gonnardite(?) ± analcime ±
calcite
Estimation of overall vein abundance (VA), and Cu and Mo abundance in each vein type: A = abundant, C = common, R = rare, T = trace, - = not present
Appendix A: Geochronology
70
U-Pb analyses were performed at the Arizona LaserChron Center, using a Multicollector Inductively Coupled Plasma Mass
Spectrometer (GVI Isoprobe) coupled to a 193 nm Excimer laser ablation system (New Wave Instruments and Lambda
Physik).
Re-Os analyses were performed by Fernando Barra at the University of Arizona.
Sample
Number
U-Pb (zircon)
Method
73.3+1.0/-0.72
Age (Ma)
Andesite, weak-moderate biotite
alteration with partial propylitic
overprint. Age based on 8 usable
zircons.
Description/Comments
Table A1: Summary of Geochronology
S-2
Porphyry, intense quartz +
feldspar + magnetite alteration
Porphyry, bornite-chalcopyrite
mineralization with sugary quartz+Kfeldspar veins.
57.2±1.2
Porphyry, feldspars altered to clay,
zeolite veins common
57.0±1.1
U-Pb (zircon)
57.7±0.65
U-Pb (zircon)
S-7
U-Pb (zircon)
60.4±0.3
S-5
S-16
Re-Os
(molybdenite)
60.9±0.3
K-
RL-2
Re-Os
(molybdenite)
2 mm molybdenite-quartz vein,
observed cutting sugary quartz,
comb quartz, and complex biotite
veins (Fig. 5M).
~0.5 cm pyrite-molybdenite vein
cutting across core; paragenetic
relationships unknown
S-10
83
81
79
77
Fig. A2: Individual laser spots for sample S-5.
Fig. A1: Individual laser spots for sample S-2.
67
69
71
73
75
AGE
S-2
AGE = 73.4 +2.6/-1.7 Ma
(2
71
68
64
60
S-7
AGE = 57.2±1.2 Ma
Mean = 57.2±0.7
MSWD = 2.3
)
(2
Fig. A3: Individual laser spots for sample S-7.
44
48
52
56
AGE
72
63
61
59
AGE
57
55
53
51
49
S-16
AGE = 57.2±0.9 Ma
Mean = 57.19±0.44
MSWD = 1.00
)
(2
Fig. A4: Individual laser spots for sample S-16.
73
Pb/238U
0.24
0.20
0.16
0.12
0.08
0.04
0
100
0.00
300
500
700
1
900
1100
207
2
1300
U
RL-2 2016
S-10 2017
Sample No.
0.054
0.053
0.065
Weight (g)
120.1
118.4
900.1
Total Re
(ppm)
75.5
74.5
565.9
187 Re
(ppm)
75.9
75
574.7
187 Os
(ppb)
60.3
60.4
60.9
Age
(Ma)
0.3
0.3
0.3
Error (Ma)
(2 sigma)
3
Intercepts at
60±2 & 1238±89 Ma
MSWD = 0.41
data-point error ellipses are 68.3% conf
235
Pb/
RL-2 2016
Table A2: Analytical results from Re-Os geochronology.
Fig. A5: Concordia plot for sample S-16 showing zircon inheritance.
206
4
74
75
Appendix B: Whole-Rock Geochemistry
Table B1: Descriptions of Samples for Whole-Rock Geochemistry
Name
Rock Type
Alteration
andesite
weak potassic
RL-2 1997-1998.5
andesite
weak potassic
RL-5 2033-2035
andesite
weak potassic
RL-6 2028-2030
andesite
weak potassic
RL-8 2054
andesite
weak potassic
RL-9 2014-2016
andesite
biotite-amphibole
RL-10 1613-1615
andesite
weak potassic
RL-10 2033-2035
andesite
biotite-amphibole
RL-14 2075-2077
andesite
weak potassic
S-2 1245-1246
andesite
weak potassic
S-9 2113-2114
andesite
weak potassic
S-13 2022.5-2023.5
andesite
weak potassic
S-14 1966-1968
andesite
weak potassic
S-15 2133.5-2135
andesite
strong potassic
S-17A 2066-2069
andesite
weak potassic
S-18 1996.5-1997.5
andesite
weak potassic
S-19 2041-2042.3
andesite
weak potassic
U-1 495-496
porphyry
weak potassic
RL-1 2033-2034
porphyry
weak potassic
RL-26 2015.5-2017.5
porphyry
weak potassic
S-8 1764-1765
porphyry
very weak potassic
S-8 2064-2065.5
porphyry
strong potassic
U-2 467-469
porphyry
strong potassic
U-3 481-482
76
Sample #
Rock type
SiO2 (wt%)
Al2O3 (wt%)
Fe2O3 (wt%)
MnO (wt%)
MgO (wt%)
CaO (wt%)
Na2O (wt%)
K2O (wt%)
TiO2 (wt%)
P2O5 (wt%)
LOI (wt%)
Total (wt%)
8
0.5
<2
561
1
<2
<1
< 0.5
12
4
2
2090
1.1
<1
<5
25
2
5
60
0.345
< 0.2
5.1
<3
651
<1
1.5
0.8
RL-2
andesite
59.61
18.82
5.72
0.05
1.7
5.07
3.76
2.7
0.597
0.28
1.5
99.8
50
1.7
<2
290
1
<2
<1
< 0.5
18
19
2.4
2620
1.4
<1
<5
21
15
<5
70
0.132
< 0.2
15.4
<3
746
<1
1.1
0.6
RL-5
andesite
53.81
18.15
9.14
0.06
2.89
6.44
2.92
2.13
0.917
0.35
2.39
99.19
32
2.5
<2
392
1
<2
<1
< 0.5
18
6
1.9
5750
1.7
<1
<5
30
6
8
80
1.72
< 0.2
8
<3
672
<1
1.2
< 0.5
RL-6
andesite
55.56
17.9
7.24
0.04
1.95
6.22
3.18
2.14
0.877
0.35
3.45
98.9
7
0.5
<2
296
1
<2
<1
< 0.5
13
4
3.1
799
1.9
<1
<5
4
3
<5
80
0.093
0.5
6.8
<3
790
<1
2.1
0.6
RL-8
andesite
56.49
19.34
7.19
0.04
2.4
5.69
4.04
1.86
0.777
0.23
1.14
99.19
<5
< 0.5
<2
228
1
<2
<1
< 0.5
17
7
2.2
585
1.9
<1
<5
9
6
12
50
1.14
< 0.2
9.2
<3
780
<1
1.4
0.7
RL-9
andesite
54.71
18.85
8.36
0.05
2.45
6.22
3.85
1.73
1.058
0.41
2.3
99.98
11
1
<2
184
1
<2
<1
< 0.5
29
7
5.2
1610
0.9
<1
<5
23
8
13
40
3.95
0.3
8.7
<3
764
<1
1.7
1.2
RL-10 A
andesite
52.34
17.75
9.45
0.05
3.14
5.12
3.4
1.56
0.777
0.18
4.84
98.6
20
1
<2
722
1
<2
<1
< 0.5
32
<1
2.5
1950
1.9
<1
<5
16
6
73
90
0.793
< 0.2
9.3
<3
610
2
2.8
1
RL-10 B
andesite
58.84
17.64
6.24
0.04
2.26
4.34
3.27
2.98
0.832
0.3
3
99.73
Table B2: Whole-rock geochemical analyses
Au (ppb)
Ag (ppm)
As (ppm)
Ba (ppm)
Be (ppm)
Bi (ppm)
Br (ppm)
Cd (ppm)
Co (ppm)
Cr (ppm)
Cs (ppm)
Cu (ppm)
Hf (ppm)
Hg (ppm)
Ir (ppb)
Mo (ppm)
Ni (ppm)
Pb (ppm)
Rb (ppm)
S (wt%)
Sb (ppm)
Sc (ppm)
Se (ppm)
Sr (ppm)
Ta (ppm)
Th (ppm)
U (ppm)
77
V (ppm)
W (ppm)
Y (ppm)
Zn (ppm)
Zr (ppm)
La (ppm)
Ce (ppm)
Nd (ppm)
Sm (ppm)
Eu (ppm)
Tb (ppm)
Yb (ppm)
Lu (ppm)
85
4
15
50
78
10.2
19
9
2.5
1.1
< 0.5
1.5
0.23
214
<3
13
83
67
10
19
8
2.5
0.9
< 0.5
1.3
0.19
121
3
14
64
71
10.1
20
12
2.5
1.1
< 0.5
1.5
0.22
106
<3
12
46
101
12.1
22
11
2.7
1.1
< 0.5
1.3
0.2
143
<3
15
31
78
8.9
20
13
2.6
1.1
< 0.5
1.6
0.24
125
4
9
46
65
10
19
10
2.3
0.8
< 0.5
0.9
0.13
131
5
18
44
106
13.7
25
10
3.2
1.2
< 0.5
1.8
0.26
78
Sample #
Rock type
SiO2 (wt%)
Al2O3 (wt%)
Fe2O3 (wt%)
MnO (wt%)
MgO (wt%)
CaO (wt%)
Na2O (wt%)
K2O (wt%)
TiO2 (wt%)
P2O5 (wt%)
LOI (wt%)
Total (wt%)
<5
0.9
<2
164
2
<2
<1
< 0.5
25
15
3.6
1530
1.4
<1
<5
7
15
<5
60
0.2
< 0.2
17.3
<3
485
<1
1.3
< 0.5
RL-14
andesite
52.51
17.89
10.55
0.06
3.53
7.32
2.6
1.73
1.003
0.3
1.49
98.98
37
1.4
<2
169
1
<2
1
0.6
16
7
2.5
3470
1.8
<1
<5
10
8
9
90
0.391
< 0.2
9.9
<3
629
1
2
< 0.5
S-2
andesite
54.57
18.82
8.06
0.03
3.71
4.17
3.29
2.67
0.833
0.22
3
99.38
91
1.7
<2
209
1
<2
<1
< 0.5
21
31
2.7
2610
1.3
1
<5
6
19
<5
40
0.11
< 0.2
18.8
<3
551
<1
1.4
< 0.5
S-9
andesite
54.52
17.78
8.68
0.05
4.19
5.38
2.97
2.57
0.927
0.29
2.25
99.61
9
1.7
<2
323
1
<2
<1
< 0.5
27
<1
4.2
3860
1.9
<1
<5
14
3
<5
100
0.55
< 0.2
8.2
<3
681
1
1.8
< 0.5
S-13
andesite
55.38
18.55
6.47
0.04
2.39
5.34
3.01
2.36
0.981
0.31
4.23
99.05
<5
0.9
<2
180
1
<2
<1
< 0.5
21
20
4.8
1710
1.8
<1
<5
40
18
<5
100
0.895
< 0.2
18.5
<3
475
<1
2.2
1.1
S-14
andesite
50.92
17.45
11.28
0.06
4.02
7.21
2.51
2.31
1.1
0.42
1.93
99.22
14
1.3
<2
217
1
<2
<1
< 0.5
28
19
3.1
2790
1.6
<1
<5
15
13
<5
70
0.362
< 0.2
17.2
<3
824
<1
1.6
< 0.5
S-15
andesite
53.12
18.4
8.6
0.06
4.38
6.1
2.46
2.8
0.971
0.37
2.21
99.47
13
1.8
<2
1500
1
<2
<1
< 0.5
26
19
6.6
5180
1.6
<1
<5
21
20
<5
160
0.551
< 0.2
16.9
<3
810
<1
1.3
< 0.5
S-17A
andesite
53.14
17.96
8.4
0.04
4.98
2.86
2.73
5.35
1.024
0.31
2.5
99.31
Table B2 (continued)
Au (ppb)
Ag (ppm)
As (ppm)
Ba (ppm)
Be (ppm)
Bi (ppm)
Br (ppm)
Cd (ppm)
Co (ppm)
Cr (ppm)
Cs (ppm)
Cu (ppm)
Hf (ppm)
Hg (ppm)
Ir (ppb)
Mo (ppm)
Ni (ppm)
Pb (ppm)
Rb (ppm)
S (wt%)
Sb (ppm)
Sc (ppm)
Se (ppm)
Sr (ppm)
Ta (ppm)
Th (ppm)
U (ppm)
79
S-19
andesite
53.08
17.92
9.04
0.06
4.7
5.76
2.66
2.81
1.023
0.32
2.14
99.51
138
7
12
49
77
11.7
22
12
2.6
0.9
< 0.5
1.2
0.17
131
6.2
<2
323
1
11
<1
< 0.5
22
16
3.5
9210
1
<1
U-1
andesite
53.58
17.4
8.52
0.05
4.47
4.01
3.29
3.38
1.005
0.28
2.48
98.47
249
<3
12
76
55
8.8
16
9
2.4
0.9
0.5
1.1
0.2
14
1.2
<2
848
1
<2
<1
< 0.5
8
14
1
2250
2.2
<1
RL-1
porphyry
66.46
15.79
3.2
0.04
1.78
2.45
3.38
4.65
0.479
0.13
1.9
100.3
133
5
16
26
82
11.9
24
14
3
1.2
< 0.5
1.7
0.27
165
3.4
<2
775
<1
3
<1
< 0.5
9
27
1.7
5750
2.5
<1
RL-26
porphyry
66.31
14.78
3.5
0.04
2.36
2.23
2.55
4.57
0.547
0.14
2.44
99.47
212
7
14
50
90
10.5
21
12
2.8
1
< 0.5
1.5
0.23
35
< 0.5
<2
417
2
<2
<1
< 0.5
13
36
2.9
285
2.2
<1
S-8 A
porphyry
59.88
16.71
5.41
0.04
4.2
3.48
3.72
2.11
0.783
0.19
3.96
100.5
212
<3
12
81
66
10
18
10
2.6
0.9
< 0.5
1.4
0.23
117
2.3
<2
678
1
<2
<1
< 0.5
9
24
1.2
4520
2.4
<1
S-8 B
porphyry
63.73
16.15
4.01
0.03
2.37
3.58
3.81
3.17
0.579
0.16
2.48
100.1
230
<3
11
43
66
7.8
17
6
2.3
0.9
< 0.5
1.2
0.2
223
<3
12
49
69
7.4
13
7
2.2
0.8
< 0.5
1.2
0.18
55.26
17.79
8.38
3.7
5.67
2.66
2.69
1.008
0.31
1.71
99.22
58
1.7
<2
229
1
<2
<1
0.6
24
16
4.7
2580
1.6
<1
V (ppm)
W (ppm)
Y (ppm)
Zn (ppm)
Zr (ppm)
La (ppm)
Ce (ppm)
Nd (ppm)
Sm (ppm)
Eu (ppm)
Tb (ppm)
Yb (ppm)
Lu (ppm)
Sample
Rock type
SiO2 (wt%)
Al2O3 (wt%)
Fe2O3 (wt%)
MnO (wt%)
MgO (wt%)
CaO (wt%)
Na2O (wt%)
K2O (wt%)
TiO2 (wt%)
P2O5 (wt%)
LOI (wt%)
Total (wt%)
101
3.6
<2
367
1
<2
<1
< 0.5
22
13
3.3
7100
1.2
<1
S-18
andesite
Table B2 (continued)
Au (ppb)
Ag (ppm)
As (ppm)
Ba (ppm)
Be (ppm)
Bi (ppm)
Br (ppm)
Cd (ppm)
Co (ppm)
Cr (ppm)
Cs (ppm)
Cu (ppm)
Hf (ppm)
Hg (ppm)
80
Ir (ppb)
Mo (ppm)
Ni (ppm)
Pb (ppm)
Rb (ppm)
S (wt%)
Sb (ppm)
Sc (ppm)
Se (ppm)
Sr (ppm)
Ta (ppm)
Th (ppm)
U (ppm)
V (ppm)
W (ppm)
Y (ppm)
Zn (ppm)
Zr (ppm)
La (ppm)
Ce (ppm)
Nd (ppm)
Sm (ppm)
Eu (ppm)
Tb (ppm)
Yb (ppm)
Lu (ppm)
<5
35
15
<5
100
0.452
< 0.2
16.8
<3
715
<1
1.2
0.7
221
<3
12
58
64
8.7
17
8
2.4
0.9
< 0.5
1.4
0.22
U-2
porphyry
69.9
10.57
7.27
0.04
1.98
1.55
1.75
4.07
0.509
0.13
1.22
98.99
307
U-3
porphyry
77.06
9.02
2.63
0.02
1.12
0.9
0.83
5.37
0.329
0.08
1.2
98.56
<5
16
17
<5
110
0.148
< 0.2
16
<3
499
<1
1.5
< 0.5
240
3
12
59
80
10.5
21
8
2.7
1
< 0.5
1.2
0.22
Sample
Rock type
SiO2 (wt%)
Al2O3 (wt%)
Fe2O3 (wt%)
MnO (wt%)
MgO (wt%)
CaO (wt%)
Na2O (wt%)
K2O (wt%)
TiO2 (wt%)
P2O5 (wt%)
LOI (wt%)
Total (wt%)
133
Table B2 (continued)
Au (ppb)
<5
34
17
<5
110
0.541
< 0.2
17.1
<3
559
<1
0.9
< 0.5
254
5
12
77
50
9.2
19
8
2.5
0.9
< 0.5
1.3
0.19
<5
7
14
7
80
0.228
0.3
5
<3
732
<1
6.1
2.5
73
<3
5
60
102
10.2
18
9
1.5
0.6
< 0.5
0.4
0.1
<5
15
16
16
110
0.45
0.2
6.1
<3
394
2
5.3
0.8
69
7
9
68
82
12.7
23
10
2.1
0.7
< 0.5
0.7
0.1
<5
3
25
<5
60
0.019
< 0.2
12.3
<3
543
<1
4.1
< 0.5
144
<3
10
67
89
14.9
29
12
2.8
0.9
< 0.5
1
0.16
<5
2
17
7
80
0.6
< 0.2
6.9
<3
576
<1
5.1
0.7
90
<3
7
46
98
13.9
26
10
2.3
0.8
< 0.5
0.8
0.12
81
Ag (ppm)
As (ppm)
Ba (ppm)
Be (ppm)
Bi (ppm)
Br (ppm)
Cd (ppm)
Co (ppm)
Cr (ppm)
Cs (ppm)
Cu (ppm)
Hf (ppm)
Hg (ppm)
Ir (ppb)
Mo (ppm)
Ni (ppm)
Pb (ppm)
Rb (ppm)
S (wt%)
Sb (ppm)
Sc (ppm)
Se (ppm)
Sr (ppm)
Ta (ppm)
Th (ppm)
U (ppm)
V (ppm)
W (ppm)
Y (ppm)
Zn (ppm)
Zr (ppm)
La (ppm)
Ce (ppm)
Nd (ppm)
Sm (ppm)
Eu (ppm)
Tb (ppm)
Yb (ppm)
Lu (ppm)
2.1
<2
625
<1
<2
<1
< 0.5
12
15
1.7
3430
1.1
<1
<5
4
15
7
70
0.19
0.5
8.4
<3
190
<1
1.6
< 0.5
132
<3
3
63
41
3.9
8
<5
0.8
0.3
< 0.5
0.3
0.07
8.6
<2
712
<1
30
<1
< 0.5
7
18
1.2
11500
1.5
<1
<5
33
10
12
90
0.703
0.8
4
5
173
<1
3.1
< 0.5
65
4
1
49
57
3.7
7
<5
0.6
0.4
< 0.5
0.2
0.06
Appendix C: Microprobe Analyses
82
Electron microprobe analyses were performed at the University of Arizona.
RL-4
2117.5
RL-4
2117.5
RL-4
2117.5
RL-4
2117.5
RL-4
2117.5
RL-4
2117.5
Table C1: Feldspar analyses
RL-2
1982
7.10
RL-2
1982
5.69
0.13
RL-2
1982
8.23
0.19
57.32
RL-2
1982
8.96
0.14
54.53
27.48
Sample #
10.33
0.28
60.47
29.21
0.06
8.70
plag.
10.12
0.10
62.02
25.46
0.05
10.67
plag.
10.11
0.17
65.36
24.20
0.01
6.36
plag.
8.47
0.15
65.20
21.94
0.01
4.85
plag.
4.35
0.34
66.57
22.42
0.00
2.65
plag.
6.99
0.10
61.97
21.10
0.01
2.64
plag.
0.12
52.90
24.04
0.01
1.51
plag.
Na2O
60.93
29.96
0.00
4.77
plag.
K2O
24.87
0.02
12.06
plag.
SiO2
7.55
plag.
Al2O3
0.02
mineral
CaO
0.00
99.56
0.00
0.03
99.60
0.00
0.12
0.01
99.62
0.08
0.79
0.20
0.01
100.72
0.13
0.00
0.03
0.79
0.20
0.01
100.54
0.06
0.03
0.05
0.64
0.34
0.02
100.50
0.12
0.00
0.05
0.57
0.42
0.01
101.08
0.01
0.01
0.40
0.35
0.64
0.01
100.83
0.12
0.04
0.32
0.45
0.54
0.01
101.08
0.11
0.00
0.18
TiO
BaO
100.62
0.01
0.34
0.86
0.09
0.15
Total
0.01
0.72
0.63
0.00
2
Or
0.51
0.27
0.16
FeO
An
0.49
MnO
Ab
0.10
8.81
RL-10
1610
5.60
60.24
RL-10
1610
0.08
RL-10
1610
7.23
53.75
RL-10
1610
0.08
RL-10
1610
8.68
57.70
RL-10
1610
0.08
RL-10
1610
4.06
60.01
RL-10
1610
0.22
RL-10
1610
9.63
60.33
RL-4
2117.5
0.18
Sample #
8.93
62.43
plag.
0.14
25.10
plag.
6.22
61.46
29.09
plag.
0.10
26.81
plag.
8.87
54.60
24.31
plag.
0.14
25.11
plag.
4.15
58.95
23.19
plag.
0.10
24.07
plag.
Na2O
51.74
28.34
plag.
K2O
25.88
plag.
SiO
31.20
mineral
2
CaO
2
0.06
13.26
0.43
0.04
6.78
0.00
0.07
10.30
0.19
0.00
4.82
0.27
0.01
4.15
0.15
0.03
5.72
0.21
0.06
5.57
0.25
0.03
7.99
0.90
0.03
10.99
0.14
0.01
5.88
Al O
TiO2
0.33
3
FeO
83
Ab
An
Or
Total
BaO
MnO
0.24
0.75
0.01
100.90
0.05
0.00
0.57
0.42
0.01
101.10
0.00
0.00
0.38
0.61
0.01
99.70
0.07
0.00
0.65
0.34
0.01
99.62
0.00
0.02
0.70
0.29
0.01
99.88
0.01
0.00
0.41
0.56
0.03
95.63
0.01
0.00
0.61
0.38
0.01
98.97
0.03
0.02
0.48
0.51
0.01
100.14
0.03
0.00
0.34
0.65
0.01
100.44
0.00
0.00
0.60
0.39
0.01
100.32
0.00
0.03
Table C1 (continued)
0.23
8.83
RL-10
1836.5
8.57
61.11
RL-10
1836.5
0.15
RL-10
1836.5
11.34
60.39
RL-10
1836.5
0.48
RL-10
1836.5
5.80
66.09
RL-10
1836.5
0.16
RL-10
1836.5
5.88
55.00
RL-10
1610
0.09
RL-10
1610
7.68
66.63
RL-10
1610
0.12
Sample #
3.89
59.91
plag.
0.34
24.70
plag.
8.57
50.90
25.34
plag.
0.14
21.60
plag.
8.35
59.16
27.26
plag.
0.12
20.75
plag.
8.02
59.69
25.45
plag.
0.13
33.48
plag.
Na2O
59.11
22.74
plag.
K2O
24.97
plag.
SiO
25.72
mineral
2
Total
BaO
MnO
FeO
TiO2
CaO
2
0.01
99.76
0.05
0.04
0.18
0.03
6.48
0.40
0.01
99.04
0.00
0.03
0.05
0.00
5.82
0.33
0.01
95.40
0.00
0.00
0.28
0.03
4.48
0.63
0.03
97.00
0.00
0.03
0.54
0.26
7.57
0.44
0.01
99.74
0.02
0.01
0.05
0.02
6.48
0.50
0.49
0.01
99.38
0.00
0.01
0.12
0.02
5.89
0.43
0.56
0.01
96.33
0.00
0.00
0.25
0.03
7.82
0.87
0.08
0.04
100.82
0.03
0.04
0.10
0.01
1.13
0.58
0.40
0.01
100.71
0.03
0.01
0.06
0.00
6.17
0.61
0.37
0.02
100.52
0.00
0.03
0.05
0.00
5.57
Al O
Or
0.43
0.55
3
An
0.34
RL-14
1985
0.66
RL-14
1985
0.59
RL-14
1985
0.56
RL-14
1985
Ab
RL-14
1985
RL-10
2140.7
RL-14
1985
RL-10
2140.7
RL-14
1985
RL-10
2140.7
Sample #
84
1.33
0.02
1.14
0.03
2.09
45.52
0.03
1.30
46.68
0.02
1.67
plag.
5.63
0.07
47.19
34.40
plag.
4.98
0.13
44.83
35.43
16.85
plag.
4.99
0.10
46.53
33.81
18.30
plag.
4.91
0.20
54.58
35.99
16.66
plag.
9.17
0.20
53.65
33.30
18.51
0.00
plag.
0.27
51.27
29.25
17.37
0.01
plag.
2
54.06
29.82
11.12
0.02
plag.
KO
62.41
28.16
11.21
0.02
plag.
2
29.33
10.96
0.02
plag.
SiO2
24.10
11.06
0.00
mineral
Al2O3
4.90
0.00
Na O
CaO
0.04
0.00
0.05
0.01
0.06
0.00
0.00
0.00
100.29
TiO2
0.01
0.18
101.11
0.00
0.60
0.00
0.00
100.80
0.00
0.91
0.50
0.03
0.11
101.02
0.00
0.93
0.09
0.82
0.03
0.00
99.48
0.00
0.88
0.07
0.50
0.04
101.32
0.00
0.94
0.12
0.74
0.10
100.06
0.01
0.92
0.06
0.58
0.11
96.46
0.01
0.65
0.07
0.21
0.00
100.22
0.01
0.68
0.34
0.73
BaO
100.95
0.01
0.67
0.31
0.50
Total
0.02
0.67
0.32
0.11
Or
0.33
0.31
FeO
An
0.65
MnO
Ab
S-2
2085.4
S-2
2085.4
Table C1 (continued)
S-2
2085.4
5.42
S-2
2085.4
10.76
0.11
S-2
2085.4
9.40
0.25
52.06
S-2
2085.4
5.92
0.13
64.04
29.82
S-2
1182.5
4.65
0.13
62.39
22.05
11.26
S-2
1182.5
6.14
0.23
55.29
24.17
2.25
0.01
RL-26
2001
6.74
0.26
51.89
29.10
4.55
0.01
0.15
RL-14
1985
6.53
0.15
53.89
30.61
9.99
0.03
0.06
0.00
Sample #
9.96
0.12
56.75
28.13
12.40
0.00
0.16
0.02
0.03
plag.
6.42
0.15
57.17
27.53
9.67
0.02
0.29
0.03
0.21
98.87
plag.
Na2O
0.10
65.83
27.03
9.04
0.02
0.31
0.01
0.00
99.65
plag.
K2O
56.64
22.44
8.87
0.02
0.58
0.00
0.00
100.86
plag.
SiO2
27.87
2.58
0.02
0.43
0.00
0.12
100.73
plag.
Al2O3
9.28
0.00
0.32
0.01
0.03
100.25
plag.
CaO
0.04
0.05
0.00
0.00
98.73
plag.
TiO2
0.80
0.08
100.68
plag.
FeO
0.02
0.00
100.14
plag.
MnO
0.00
101.02
plag.
BaO
101.19
mineral
Total
85
Ab
An
Or
0.41
0.58
0.01
0.79
0.20
0.01
S-2
2085.4
0.43
0.56
0.01
S-2
2085.4
0.43
0.56
0.01
S-2
2085.4
0.39
0.59
0.02
S-2
2085.4
0.28
0.71
0.02
S-2
2085.4
0.38
0.61
0.01
S-2
2085.4
0.67
0.31
0.01
S-2
2085.4
0.82
0.16
0.02
S-2
2085.4
0.33
0.66
0.01
4.55
S-2
2085.4
9.55
0.16
S-2
2085.4
6.11
0.11
52.64
Sample #
5.84
0.15
62.65
30.82
plag.
10.16
0.11
54.47
23.77
0.02
12.29
plag.
9.18
0.12
54.42
29.06
0.02
4.28
plag.
5.52
0.34
63.28
29.57
0.03
10.44
plag.
6.31
0.11
61.99
23.25
0.02
10.75
plag.
5.29
0.19
54.25
23.57
0.02
3.73
plag.
5.60
0.16
55.81
29.44
0.03
4.37
plag.
Na2O
0.08
52.96
28.70
0.04
10.89
plag.
K2O
53.26
29.40
0.00
9.82
plag.
SiO2
29.08
0.00
11.25
plag.
Al2O3
0.01
10.78
mineral
CaO
An
Or
Total
BaO
MnO
FeO
0.35
0.65
0.01
99.02
0.00
0.00
0.19
0.32
0.66
0.01
99.28
0.00
0.03
0.19
0.39
0.59
0.01
101.06
0.04
0.00
0.19
0.34
0.65
0.01
100.71
0.05
0.00
0.40
0.67
0.31
0.03
99.55
0.01
0.00
0.06
0.73
0.26
0.01
100.58
0.00
0.00
0.02
0.36
0.63
0.01
100.87
0.00
0.00
0.15
0.37
0.62
0.01
100.57
0.08
0.00
0.25
0.69
0.30
0.01
100.51
0.02
0.00
0.11
0.27
0.71
0.01
100.72
0.00
0.00
0.23
TiO
2
Ab
Sample #
plag.
S-2
2085.4
plag.
S-2
2085.4
plag.
S-2
2085.4
plag.
S-5
2003
plag.
S-5
2003
plag.
S-5
2003
plag.
S-5
2003
plag.
S-5
2003
plag.
S-5
2003
plag.
S-7
1537
Table C1 (continued)
mineral
86
2
0.29
7.95
0.20
10.21
0.17
6.69
0.26
7.59
0.27
8.61
0.18
8.85
61.41
0.24
8.11
54.90
0.18
5.60
58.78
0.18
7.90
51.80
0.06
4.13
Na O
KO
60.91
12.73
60.90
6.92
0.02
59.92
9.79
0.00
0.18
55.16
5.25
0.08
0.97
0.02
63.44
5.74
0.01
0.59
0.00
0.08
57.24
5.07
0.01
0.19
0.00
0.00
100.02
2
5.33
0.00
0.15
0.04
0.00
100.80
0.00
SiO
9.72
0.01
0.18
0.00
0.00
99.40
0.01
0.74
30.99
3.41
0.00
0.28
0.00
0.00
99.91
0.01
0.45
0.25
26.04
Al2O3
7.33
0.00
0.28
0.00
0.01
100.90
0.02
0.62
0.53
28.25
CaO
0.01
0.06
0.05
0.00
99.35
0.01
0.38
0.37
24.66
TiO2
0.29
0.04
0.03
97.81
0.02
0.38
0.60
25.06
FeO
0.02
0.00
100.76
0.02
0.35
0.61
24.32
MnO
0.02
100.36
0.01
0.39
0.62
24.43
BaO
99.31
0.02
0.58
0.58
28.65
Total
0.02
0.24
0.41
23.01
Or
0.46
0.74
26.16
An
0.52
2
Ab
5.89
S-7
1537
0.25
S-7
1537
5.58
53.62
S-7
1537
0.16
29.25
S-7
1537
5.66
54.65
S-7
1537
0.23
29.19
S-7
1537
4.53
54.13
S-7
1537
0.12
29.30
S-7
1537
5.21
52.61
S-7
1537
0.12
30.64
S-7
1537
5.92
53.95
Sample #
0.20
29.22
plag.
4.49
55.47
plag.
0.19
28.59
plag.
9.49
52.96
plag.
0.25
30.73
plag.
4.45
64.73
plag.
0.11
23.47
plag.
4.70
51.86
plag.
0.09
30.72
plag.
Na2O
52.09
plag.
K2O
30.75
mineral
SiO2
FeO
CaO
2
2
0.00
0.23
0.03
12.44
0.00
0.02
0.20
0.03
12.51
101.87
0.00
0.00
0.27
0.01
3.64
0.01
100.61
0.00
0.00
0.17
0.03
12.03
0.01
100.76
0.04
0.01
0.43
0.02
10.08
0.01
99.86
0.06
0.03
0.39
0.00
10.86
0.01
100.47
0.09
0.01
0.32
0.01
12.14
0.02
100.42
0.00
0.01
0.21
0.03
10.83
0.01
100.29
0.05
0.01
0.17
0.01
10.47
0.02
100.34
0.00
0.04
0.49
0.00
10.80
Al O
MnO
0.07
99.91
0.02
3
BaO
100.40
0.01
TiO
Total
0.01
Or
87
Ab
An
0.28
0.71
0.27
0.72
0.71
0.26
0.28
0.71
0.37
0.61
0.33
0.66
0.28
0.72
0.35
0.64
0.35
0.64
0.36
0.63
Table C1 (continued)
S-10
2121.5
8.41
S-7
1537
0.23
S-7
1537
5.43
62.73
S-7
1537
6.28
0.10
24.78
S-7
1537
6.54
0.13
54.32
5.41
S-7
1537
0.15
55.04
29.66
0.01
S-7
1537
6.83
55.38
28.68
0.01
10.81
S-7
1537
0.12
28.34
0.02
10.01
S-7
1537
8.84
57.48
9.74
S-7
1537
0.27
28.17
0.01
Sample #
7.40
63.41
9.24
plag.
2.05
23.17
0.00
plag.
9.90
64.99
3.92
plag.
0.35
21.84
0.01
plag.
7.81
63.72
2.02
plag.
0.24
23.05
0.00
0.20
plag.
5.20
59.53
3.74
0.13
plag.
Na2O
0.16
25.55
0.01
0.29
plag.
K2O
53.10
6.71
0.35
plag.
SiO2
30.90
0.02
0.28
plag.
Al2O3
0.01
11.73
0.25
mineral
CaO
0.22
Or
Total
BaO
MnO
FeO
0.68
0.01
101.41
0.04
0.04
0.44
0.02
100.13
0.00
0.01
0.26
0.03
101.15
0.09
0.00
0.17
0.20
98.95
0.24
0.05
0.29
0.02
100.03
0.10
0.02
0.56
0.01
101.99
0.02
0.00
0.58
0.01
100.47
0.10
0.00
0.60
0.01
100.43
0.00
0.01
0.25
0.65
0.01
100.56
0.00
0.02
0.21
0.38
0.02
101.85
0.01
0.26
TiO
2
An
0.61
RL-2
1982
0.34
RL-2
1982
0.39
RL-2
1982
0.41
RL-2
1982
0.43
S-16
2056
0.68
S-16
2056
0.64
S-16
2056
0.71
S-15
2041
0.54
S-15
2041
0.31
S-10
2121.5
Ab
Sample #
0.28
K-feld.
0.51
10.22
K-feld.
0.91
15.40
K-feld.
0.89
14.33
K-feld.
9.42
12.97
plag.
8.99
0.48
plag.
11.08
0.37
plag.
1.11
0.02
plag.
3.70
0.09
plag.
7.60
0.06
plag.
Na2O
0.17
mineral
K2O
88
7.08
24.70
53.21
14.65
32.45
49.70
0.00
18.26
35.63
45.31
0.04
0.00
2.37
21.90
64.93
0.12
0.00
4.63
23.90
62.36
0.08
0.00
2.45
23.87
62.58
0.00
0.00
0.06
13.00
39.61
0.06
0.00
0.06
19.16
65.15
0.06
0.01
0.00
17.44
56.83
4.17
0.21
0.00
30.89
47.51
SiO
2
0.00
0.23
2
CaO
0.00
0.12
Or
Total
BaO
0.47
0.01
93.43
0.11
0.21
0.79
0.00
100.69
0.01
0.06
0.94
0.01
100.63
0.00
0.83
0.17
0.00
100.51
0.16
0.00
0.65
0.32
0.03
100.56
0.13
0.04
0.76
0.19
0.04
98.93
0.03
0.00
0.06
0.00
0.94
66.96
0.43
0.05
0.00
0.94
100.04
0.36
0.03
0.00
0.97
91.02
0.78
0.02
0.00
0.98
93.33
0.03
Al O
TiO2
0.56
3
FeO
An
0.52
MnO
Ab
CaO
Al2O3
SiO2
K2O
Na2O
mineral
Sample #
0.00
0.00
18.63
63.39
15.15
0.86
K-feld.
RL-2
1982
0.02
0.10
19.25
64.50
15.25
0.55
K-feld.
RL-4
2117.5
0.00
0.00
18.87
64.99
16.23
0.04
K-feld.
RL-4
2117.5
0.07
1.01
20.33
62.55
10.87
2.19
K-feld.
RL-4
2117.5
0.00
0.00
18.97
63.99
16.04
0.40
K-feld.
RL-10
1836.5
0.00
0.00
18.71
63.80
16.49
0.34
K-feld.
RL-10
1836.5
0.02
1.09
20.59
64.26
7.66
5.17
K-feld.
RL-10
1836.5
0.01
0.00
18.73
63.91
15.79
0.56
K-feld.
RL-10
1836.5
0.00
0.03
18.60
63.67
15.93
0.27
K-feld.
RL-10
1836.5
0.00
0.00
19.52
63.09
15.81
0.56
K-feld.
RL-10
1836.5
Table C1 (continued)
TiO2
0.00
0.34
0.00
0.05
0.01
0.02
0.23
99.38
0.01
0.00
0.16
98.76
0.27
0.01
0.16
99.19
0.01
0.04
0.03
99.21
0.00
0.00
0.01
99.39
0.03
0.00
2.47
99.46
0.09
0.06
0.07
99.51
0.02
0.09
100.30
0.00
0.28
99.85
FeO
BaO
98.31
MnO
Total
89
TiO2
CaO
Al2O3
SiO2
2
KO
mineral
Sample #
Ab
An
Or
2
0.05
0.00
0.05
19.43
67.00
15.97
0.22
K-feld.
RL-10
2140.7
0.05
0.00
0.95
0.01
0.00
0.02
19.05
65.35
15.92
0.42
K-feld.
RL-10
2140.7
0.03
0.01
0.96
2.10
0.01
1.09
34.96
46.31
10.71
0.11
K-feld.
RL-14
1985
0.00
0.00
1.00
1.02
0.02
0.21
36.99
46.88
10.74
0.09
K-feld.
RL-14
1985
0.14
0.06
0.79
0.51
0.02
0.78
18.40
63.41
16.13
0.32
K-feld.
RL-14
1985
0.02
0.00
0.98
0.19
0.08
0.09
19.37
62.53
14.87
0.50
K-feld.
RL-14
1985
0.02
0.00
0.98
2.30
0.00
0.21
35.01
47.23
10.49
0.07
K-feld.
RL-14
1985
0.35
0.07
0.58
0.02
0.00
0.00
12.18
41.57
12.93
0.50
K-feld.
RL-26
2001
0.03
0.00
0.97
0.05
0.04
0.00
18.84
64.57
15.70
0.47
K-feld.
RL-26
2001
0.01
0.00
0.98
0.10
0.00
0.21
18.50
60.51
15.76
0.50
K-feld.
S-2
2085.4
0.03
0.00
0.97
Total
BaO
0.99
102.88
0.16
0.00
0.98
100.78
0.00
0.01
0.08
0.91
95.31
0.00
0.01
0.01
0.02
0.98
95.95
0.00
0.00
0.02
0.04
0.94
99.63
0.03
0.00
0.03
0.01
0.97
100.22
2.58
0.00
0.01
0.02
0.98
95.30
0.00
0.00
0.03
0.00
0.97
67.41
0.21
0.03
0.00
0.97
99.93
0.27
0.03
0.01
0.96
96.09
0.51
Na O
FeO
Or
0.00
0.02
S-2
2085.4
K-feld.
S-2
2085.4
0.75
K-feld.
S-2
2085.4
0.86
K-feld.
S-2
2085.4
1.27
K-feld.
S-5
2003
1.06
K-feld.
S-7
1537
0.77
K-feld.
S-7
1537
0.91
K-feld.
S-7
1537
1.08
K-feld.
S-7
1537
1.57
K-feld.
S-7
1537
0.00
An
0.01
MnO
Ab
Sample #
K-feld.
0.59
Table C1 (continued)
mineral
1.03
Na2O
90
SiO
2
KO
19.08
63.06
15.44
19.23
62.64
15.34
18.88
63.76
15.14
18.97
63.52
15.15
23.04
62.07
7.85
18.93
64.42
15.43
18.16
62.23
14.94
18.83
63.98
15.48
18.93
64.02
15.36
19.08
64.37
13.92
Total
BaO
MnO
FeO
TiO2
CaO
2
0.94
98.97
0.27
0.00
0.06
0.01
0.02
0.97
98.28
0.24
0.04
0.19
0.00
0.00
0.96
99.16
0.56
0.00
0.06
0.00
0.00
0.00
0.95
99.05
0.33
0.01
0.21
0.00
0.00
0.25
0.65
98.04
0.16
0.00
0.12
0.00
3.51
0.00
0.94
100.01
0.03
0.00
0.11
0.02
0.00
0.00
0.96
96.62
0.22
0.01
0.26
0.01
0.00
0.00
0.95
99.69
0.35
0.01
0.10
0.04
0.00
0.00
0.94
99.83
0.24
0.04
0.10
0.02
0.05
0.00
0.91
99.23
0.07
0.00
0.16
0.02
0.04
Al O
2
3
Or
0.00
S-8
1686.8
0.00
S-7
1537
K-feld.
0.00
S-7
1537
K-feld.
0.82
An
S-7
1537
K-feld.
0.95
15.46
0.09
S-7
1537
K-feld.
0.62
15.57
64.04
0.06
S-7
1537
K-feld.
1.21
16.02
64.39
0.05
S-7
1537
K-feld.
0.74
14.90
63.99
0.04
S-7
1537
K-feld.
1.30
15.78
64.07
0.06
S-7
1537
K-feld.
1.02
14.94
63.50
0.09
S-7
1537
K-feld.
0.55
15.29
64.06
0.05
Sample #
K-feld.
0.61
15.94
64.18
0.04
mineral
0.52
15.62
63.95
0.03
Na2O
15.52
63.66
0.00
18.68
0.06
K2O
64.55
0.00
18.99
Ab
SiO2
0.00
18.86
0.03
0.04
0.04
0.07
18.89
0.02
0.28
0.08
0.04
0.23
18.66
0.00
0.15
0.03
0.16
0.03
0.00
0.26
0.05
0.14
99.26
18.90
0.02
0.03
0.02
0.15
100.39
0.95
0.03
0.00
0.08
0.00
0.13
99.93
0.95
0.00
18.97
0.01
0.00
0.01
0.33
99.45
0.97
0.00
0.00
0.00
0.11
0.03
0.27
99.35
0.93
0.00
18.68
0.05
0.00
0.32
99.53
0.96
0.00
0.00
2
0.00
0.16
99.93
0.93
0.00
18.78
FeO
0.00
0.16
99.29
0.94
0.00
0.02
MnO
0.08
98.96
0.97
0.00
18.73
BaO
99.47
0.97
0.00
Al2O3
Total
0.97
0.00
CaO
Or
0.00
TiO
An
91
Ab
0.03
0.03
Sample #
K-feld.
S-15
2041
0.80
K-feld.
S-15
2041
15.48
0.24
K-feld.
S-15
2056
63.62
14.84
0.48
K-feld.
S-15
2056
15.29
49.81
14.77
0.69
K-feld.
S-15
2056
19.15
11.06
35.72
11.17
0.02
K-feld.
S-15
2056
0.00
15.37
49.79
14.81
0.50
K-feld.
S-15
2056
0.07
mineral
0.65
15.55
62.71
18.60
0.00
0.04
Na2O
15.86
64.25
18.93
0.09
0.07
K2O
65.11
18.98
0.08
0.06
SiO2
19.05
0.00
0.25
0.02
0.03
Al2O3
0.04
0.00
0.01
Table C1 (continued)
CaO
0.13
0.00
0.00
0.00
0.54
0.06
0.00
0.21
81.28
0.00
0.01
0.52
77.36
0.97
0.06
0.00
0.17
81.20
0.40
0.00
0.01
1.44
97.88
0.96
0.60
0.03
0.11
0.16
98.94
0.97
0.00
0.00
0.02
0.07
99.86
0.98
0.01
0.04
0.15
BaO
100.95
0.96
0.00
0.03
0.03
Total
0.96
0.00
0.01
TiO2
Or
0.00
0.04
FeO
An
0.04
MnO
Ab
0.03
0.05
0.05
92
93
RL-10
2140.7
RL-10
2140.7
RL-10
2303
RL-10
2303
Table C2: Oxide mineral analyses
RL-10
1610
0.04
RL-10
1610
0.01
0.01
RL-10
1610
0.55
0.00
0.02
RL-10
1610
0.80
0.01
0.11
92.91
RL-10
1610
0.00
0.03
0.16
92.95
0.05
RL-10
1610
0.10
0.02
0.27
93.52
0.05
0.02
Sample #
0.00
0.00
0.04
93.74
0.07
0.26
0.00
magn.
0.04
0.00
0.05
86.78
0.01
0.12
0.05
0.15
magn.
0.00
0.00
0.04
92.40
0.01
0.12
0.04
0.43
magn.
0.08
0.02
0.05
93.48
0.06
0.13
0.02
0.18
magn.
SiO2
0.00
0.05
93.41
0.02
0.02
0.04
0.14
magn.
MgO
0.05
93.82
0.02
0.04
0.04
0.16
93.18
magn.
Al2O3
93.58
0.01
0.02
0.02
0.14
93.85
magn.
FeO
0.06
0.08
0.02
0.17
94.64
magn.
MnO
0.04
0.03
0.23
95.12
magn.
TiO2
0.04
0.18
87.19
magn.
Cr2O3
0.14
92.81
mineral
V2O3
93.78
S-5
2003
93.79
S-5
2003
94.20
S-5
2003
94.00
RL-14
1985
Total
RL-14
1985
4.20
RL-14
1985
0.08
0.16
RL-14
1985
0.10
0.01
1.22
RL-14
1985
0.02
0.01
0.06
79.79
RL-14
1985
0.09
0.01
0.04
94.06
0.03
RL-14
1985
0.02
0.00
0.08
93.57
0.02
0.07
Sample #
0.03
0.00
0.05
93.28
0.05
0.04
0.39
magn.
0.22
0.00
0.08
91.75
0.19
0.99
0.03
0.46
magn.
0.02
0.02
0.14
93.74
0.02
0.06
0.03
0.40
magn.
0.05
0.00
0.10
93.31
0.03
0.00
0.02
0.40
magn.
SiO2
0.00
0.11
92.50
0.03
0.05
0.04
0.20
magn.
MgO
0.07
93.41
0.04
0.10
0.02
0.21
magn.
Al2O3
92.29
0.06
0.32
0.05
0.25
magn.
FeO
0.10
0.38
0.17
0.23
magn.
MnO
0.19
0.05
0.26
magn.
TiO2
0.02
0.29
magn.
Cr2O3
0.27
mineral
V2O3
S-14
1942.5
86.32
S-14
1942.5
magn.
94.70
S-10
2121.5
magn.
95.20
S-10
2121.5
magn.
93.87
S-10
2041
magn.
92.16
S-10
2041
magn.
94.20
S-7
1537
magn.
93.88
S-7
1537
magn.
93.63
S-7
1537
magn.
94.33
S-7
1537
magn.
93.00
Sample #
magn.
Total
mineral
94
Cr O
TiO2
MnO
FeO
Al2O3
MgO
SiO2
0.14
0.03
0.05
0.07
92.83
0.08
0.03
0.06
0.08
0.01
0.03
0.04
92.20
0.10
0.13
0.36
89.86
0.00
0.00
0.37
0.00
84.90
0.82
0.04
3.73
94.07
0.16
0.01
0.05
0.00
93.76
0.04
0.01
0.03
95.44
0.12
0.00
0.10
0.05
95.03
0.13
0.00
0.00
94.92
0.25
0.07
0.07
0.01
94.42
0.08
0.01
0.02
92.16
0.58
0.03
0.05
0.02
91.39
0.08
0.00
0.01
92.32
0.29
0.03
0.04
0.00
91.85
0.07
0.02
0.03
92.82
0.16
0.01
0.07
0.07
92.37
0.09
0.00
0.04
93.42
0.27
0.10
0.52
0.07
92.36
0.05
0.00
0.07
V2O3
3
92.94
2
93.29
Total
RL-4
2117.5
RL-4
2117.5
RL-4
2117.5
Table C2 (continued)
RL-4
2117.5
0.00
S-14
1942.5
0.00
0.00
S-10
2041
0.00
0.01
0.02
RL-10
2303
0.31
0.06
0.02
1.17
RL-10
2140.7
0.25
0.01
0.13
3.86
0.01
S-16
2056
0.08
0.04
0.04
1.21
0.00
94.78
S-16
2056
0.00
0.02
0.18
1.69
0.05
86.57
0.05
Sample #
0.01
0.07
0.00
47.20
0.00
93.60
0.14
0.65
rutile
0.16
0.05
0.01
47.31
3.08
92.39
0.06
1.34
96.67
rutile
0.01
0.20
0.00
48.29
2.67
45.25
0.25
0.76
91.95
rutile
0.00
0.14
44.16
2.88
44.21
0.00
0.94
95.87
rutile
0.04
92.71
2.23
38.67
0.18
0.27
95.65
ilmen.
SiO2
92.05
0.02
47.18
0.01
0.36
96.27
S-7
1537
ilmen.
MgO
0.01
0.68
0.02
0.37
94.82
S-5
2003
rutile
ilmen.
Al2O3
0.13
0.50
0.27
90.31
S-5
2003
rutile
ilmen.
FeO
0.46
0.13
93.92
S-2
1182.5
rutile
magn.
MnO
0.27
94.53
S-2
1182.5
rutile
magn.
TiO2
92.97
S-2
1182.5
rutile
mineral
Cr O
S-2
1182.5
rutile
V2O3
MgO
SiO2
0.02
0.00
0.03
0.99
0.06
0.02
0.27
0.90
0.04
0.01
0.12
1.01
0.08
0.02
0.06
1.34
0.01
0.00
2.87
0.55
0.03
0.01
0.15
1.10
0.53
0.00
1.17
Total
Al2O3
0.51
3
Sample #
rutile
2
mineral
FeO
95
Total
V2O3
Cr2O3
TiO2
MnO
98.13
0.44
0.01
97.08
0.03
98.09
0.60
0.04
96.09
0.02
97.90
0.67
0.09
96.08
0.00
95.84
0.64
0.36
93.66
0.00
99.25
0.60
0.02
94.41
0.00
97.42
0.69
0.10
95.89
0.00
97.96
0.50
0.00
94.66
0.00
RL-10
1610
amph.
RL-10
1610
amph.
RL-10
1610
amph.
RL-10
1610
Table C3: Other analyses
amph.
0.25
RL-10
1610
0.29
0.00
amph.
0.71
0.03
0.13
RL-10
1610
0.36
0.05
0.09
15.91
amph.
0.32
0.04
0.54
16.22
4.35
RL-10
1610
0.60
0.11
0.36
15.66
4.11
0.01
amph.
0.21
0.00
0.22
15.89
6.24
0.01
51.51
RL-10
1610
0.26
0.00
0.52
14.93
5.31
0.00
51.67
amph.
0.24
0.00
0.15
12.84
4.45
0.02
47.77
RL-10
1610
0.27
0.00
0.12
17.62
7.02
0.00
50.24
amph.
0.00
0.05
17.01
2.62
0.00
50.08
RL-10
1610
F
0.11
17.60
3.70
0.00
46.60
amph.
K2O
16.74
2.48
0.00
52.97
Sample #
MgO
3.84
0.00
51.49
mineral
Al2O3
0.00
53.59
Na O
P2O5
52.06
2
SiO2
96
MnO
FeO
SO2
2
0.00
0.26
10.33
0.00
0.23
0.09
12.43
96.60
0.04
0.23
9.65
0.03
0.12
0.00
12.55
95.52
0.02
0.20
10.00
0.00
0.26
0.03
12.43
95.70
0.00
0.21
9.23
0.00
0.23
0.06
12.39
96.09
0.02
0.30
15.49
0.00
0.32
0.14
12.26
95.95
0.00
0.28
12.70
0.00
0.36
0.05
12.45
96.65
0.03
0.19
11.33
0.00
0.34
0.10
12.42
96.12
0.01
0.26
11.61
0.00
1.46
0.14
11.66
95.13
0.03
0.24
10.02
0.02
0.24
0.06
12.09
93.74
0.00
0.13
9.76
0.02
0.22
0.04
11.41
CaO
BaO
96.37
TiO
Cl
Total
0.52
0.14
0.56
0.05
0.91
0.09
0.73
0.05
0.34
0.80
0.18
0.81
10.42
1.26
0.14
0.90
RL-14
1985
0.00
0.10
12.76
RL-14
1985
0.54
0.51
16.03
11.89
RL-14
1985
0.00
0.64
13.68
10.44
0.00
RL-14
1985
0.36
0.46
15.39
4.77
0.00
41.46
RL-14
1985
0.00
0.29
14.95
7.04
0.00
44.27
12.05
RL-14
1985
0.24
0.25
17.32
8.42
0.02
51.01
12.29
0.31
RL-10
1610
0.16
0.09
15.43
6.99
0.03
48.67
12.45
0.17
1.10
RL-10
1610
0.10
17.02
3.96
0.03
46.90
12.54
0.04
0.74
0.00
RL-10
1610
Na2O
17.06
5.33
0.03
48.41
12.66
0.10
0.47
0.00
17.35
RL-10
1610
KO
F
2
3.60
0.03
51.00
12.70
0.09
0.36
0.02
14.53
0.21
Sample #
MgO
2.83
0.01
49.44
11.78
0.05
0.98
0.00
11.38
0.20
0.00
amph.
Al2O3
0.00
51.55
12.40
0.13
0.48
0.02
14.06
0.35
0.00
97.10
amph.
P2O5
52.42
12.24
0.04
0.68
0.00
10.96
0.22
0.03
97.19
amph.
SiO2
12.44
0.05
0.36
0.00
12.63
0.21
0.00
97.06
amph.
CaO
0.02
0.28
0.00
9.85
0.29
0.00
98.02
amph.
Cl
0.21
0.01
12.15
0.31
0.00
97.26
amph.
TiO2
0.03
10.18
0.26
0.00
97.70
amph.
SO2
10.09
0.20
0.00
95.89
amph.
FeO
0.30
0.00
96.23
amph.
MnO
0.00
95.58
amph.
BaO
95.89
mineral
Total
Table C3 (continued)
97
0.27
S-14
1942.5
1.02
0.07
amph.
3.64
0.05
0.15
S-14
1942.5
0.25
0.00
0.47
17.01
amph.
0.37
0.14
5.74
14.50
S-14
1942.5
0.51
0.00
0.13
4.06
3.66
amph.
0.58
0.00
0.17
17.51
8.19
0.01
S-14
1942.5
0.61
0.00
0.23
15.02
23.21
0.03
52.38
amph.
0.23
0.00
0.38
15.82
3.32
0.00
52.40
12.28
S-10
2041
0.28
0.12
0.48
14.46
3.44
0.02
53.85
11.29
0.03
amph.
0.12
0.06
12.77
5.84
0.00
53.33
3.56
0.04
0.33
RL-14
1985
0.13
16.84
7.38
0.03
49.48
12.60
0.02
0.30
0.01
amph.
17.10
8.62
0.03
50.36
12.51
0.03
0.50
0.01
10.32
RL-14
1985
KO
F
2
3.48
0.03
48.21
12.45
0.08
0.43
0.01
11.59
0.28
amph.
MgO
3.20
0.01
46.38
12.61
0.05
0.00
0.01
5.31
0.24
0.00
RL-14
1985
Al2O3
0.00
52.66
12.14
0.07
0.52
0.00
9.74
0.04
0.00
amph.
P2O5
53.23
12.61
0.10
0.40
0.00
12.37
0.23
0.00
RL-14
1985
SiO2
12.70
0.04
0.40
0.02
11.56
0.43
0.00
96.79
amph.
CaO
0.02
0.21
0.04
13.33
0.37
0.00
100.14
RL-14
1985
Cl
0.19
0.00
14.92
0.24
0.14
99.96
amph.
TiO2
0.01
10.87
0.23
0.00
97.76
Sample #
SO2
10.33
0.28
0.00
93.87
mineral
FeO
0.28
0.00
97.89
Na O
MnO
0.08
97.70
2
BaO
96.73
0.04
97.42
0.00
97.67
0.01
0.00
Total
0.00
S-14
1942.5
0.00
0.00
S-14
1942.5
0.06
RL-4
2117.5
0.04
0.00
RL-4
2117.5
0.06
RL-4
2117.5
0.05
0.02
RL-4
2117.5
0.00
S-14
1942.5
0.04
0.02
S-14
1942.5
0.13
S-14
1942.5
0.25
0.04
0.00
S-14
1942.5
0.07
0.00
0.01
Sample #
0.20
0.07
0.00
0.02
0.05
anhyd.
0.00
0.00
0.02
0.06
0.04
anhyd.
0.30
0.12
0.00
0.00
0.08
0.08
anhyd.
0.07
0.00
0.01
0.06
0.06
anhyd.
1.99
0.09
17.18
0.04
0.06
0.06
anhyd.
0.12
16.72
3.25
0.07
0.12
anhyd.
0.18
15.97
2.96
0.00
0.20
amph.
8.41
4.47
0.00
53.33
amph.
14.78
0.00
51.83
amph.
Na2O
0.07
50.63
amph.
KO
53.72
mineral
2
3
MgO
F
2
5
SiO2
11.12
12.20
12.13
12.54
43.16
43.71
43.63
43.60
43.52
40.75
PO
Al O
2
CaO
98
MnO
FeO
2
2
0.07
0.15
5.80
0.00
0.25
0.03
95.35
0.00
0.32
10.78
0.01
0.45
0.05
94.02
0.06
0.32
9.29
0.00
0.36
0.02
97.72
0.00
0.34
10.22
0.00
0.44
0.03
76.36
0.00
0.00
0.27
32.41
0.00
0.00
83.35
0.04
0.02
0.01
39.30
0.00
0.00
80.91
0.07
0.02
0.08
36.84
0.00
0.01
80.04
0.00
0.04
0.01
36.17
0.00
0.00
81.25
0.00
0.00
0.09
37.47
0.00
0.00
81.99
0.00
0.00
0.34
40.75
0.00
0.00
Cl
BaO
96.71
SO
TiO
Total
Table C3 (continued)
2.35
0.02
0.00
1.10
0.02
0.00
1.88
0.03
0.22
1.74
0.01
0.15
2.03
0.02
0.02
0.17
0.03
RL-14
1985
0.31
0.00
0.00
RL-14
1985
0.58
0.00
0.01
RL-14
1985
0.17
0.05
0.00
0.05
0.03
RL-14
1985
0.70
0.00
0.09
41.75
RL-14
1985
0.03
0.01
0.00
0.01
38.32
0.06
RL-14
1985
1.28
0.00
0.00
41.83
0.17
50.18
RL-10
1836.5
0.00
0.00
0.00
0.01
39.33
1.16
56.03
0.01
RL-10
1610
0.48
0.00
1.78
40.39
0.13
53.85
0.61
0.00
RL-10
1610
0.01
0.00
0.01
38.75
0.09
55.47
0.97
0.00
0.28
RL-10
1610
0.00
0.02
40.66
0.11
53.90
1.13
1.32
0.01
0.02
Sample #
Na2O
0.01
41.83
0.89
54.42
1.77
0.00
0.04
0.24
0.01
apat.
KO
41.66
0.16
51.92
0.86
0.02
0.06
0.21
0.03
0.00
apat.
2
3
MgO
F
2
0.37
53.95
0.97
0.01
0.02
0.32
0.03
0.15
50.83
apat.
P2O5
0.12
55.21
1.05
0.04
0.04
0.74
0.07
0.00
101.24
apat.
SiO2
56.05
0.18
0.00
0.60
0.33
0.04
0.00
98.00
apat.
CaO
0.15
0.03
0.02
0.36
0.13
0.02
100.94
apat.
Cl
0.00
0.00
0.17
0.09
0.00
97.05
apat.
TiO2
0.00
0.04
0.09
0.04
98.68
apat.
SO2
0.28
0.02
0.03
96.37
apat.
FeO
0.05
0.01
97.02
apat.
MnO
0.00
99.03
mineral
BaO
98.82
Al O
Total
99
0.00
1.21
0.35
S-7
1537
0.25
1.67
0.04
S-7
1537
0.14
1.23
0.00
0.00
S-7
1537
0.10
1.36
0.01
0.00
0.00
S-5
2003
0.05
1.79
0.14
0.00
0.01
39.81
S-5
2003
0.01
0.90
0.12
0.00
0.02
41.74
0.38
S-2
2085.4
0.00
0.36
0.01
0.00
0.03
41.10
0.26
0.69
53.75
S-16
2056
0.08
1.79
0.00
0.00
0.09
41.27
0.25
0.10
55.29
0.02
S-14
1942.5
0.03
2.40
0.31
0.00
0.00
38.64
0.25
0.56
54.94
0.00
0.38
S-14
1942.5
2.21
0.02
0.00
0.00
40.66
0.31
0.59
54.26
0.00
0.01
0.30
S-14
1942.5
0.21
0.00
3.13
35.08
0.08
0.83
51.37
0.02
0.06
0.00
Sample #
0.36
0.09
36.91
0.30
0.10
55.02
0.01
0.12
0.23
0.28
apat.
0.51
41.49
0.74
0.58
53.45
0.00
0.11
0.33
0.08
0.05
apat.
Na2O
39.55
0.34
0.62
52.76
0.00
0.02
0.28
0.22
0.00
97.27
apat.
K2O
1.46
0.52
55.94
0.01
0.00
0.00
0.16
0.00
99.15
apat.
MgO
0.53
53.79
0.15
0.03
0.10
0.17
0.00
98.88
apat.
Al2O3
0.38
0.00
3.16
0.00
0.00
98.68
apat.
P2O5
0.08
0.24
0.07
0.00
93.83
apat.
SiO2
0.65
0.17
0.00
96.84
apat.
2
CaO
F
2
0.12
0.08
89.94
apat.
FeO
0.07
0.04
99.71
apat.
MnO
0.00
101.43
mineral
BaO
99.84
SO
TiO
Cl
Total
Table C3 (continued)
0.10
0.11
8.17
0.24
0.06
RL-10
2140.7
0.06
6.39
RL-10
1836.5
0.10
RL-10
1836.5
0.05
7.53
RL-10
1610
0.10
RL-10
1610
0.09
8.89
S-8
1833
0.04
S-8
1833
0.10
6.39
S-8
1833
1.63
S-7
1537
0.31
0.00
11.89
S-7
1537
3.72
8.82
16.65
Sample #
0.24
0.26
9.05
26.70
0.90
biot.
2.43
11.75
18.22
0.00
35.69
biot.
0.13
0.17
8.74
12.27
0.01
39.06
biot.
1.97
0.10
18.46
0.00
37.59
biot.
1.16
0.03
0.13
0.06
0.00
28.16
biot.
0.95
0.05
0.09
41.49
48.54
apat.
0.03
0.00
0.03
39.36
0.20
apat.
0.00
0.00
40.04
0.35
apat.
5.90
41.86
0.18
apat.
Na2O
30.20
0.04
apat.
KO
11.77
mineral
2
3
MgO
F
2
5
SiO2
44.56
55.01
52.95
52.81
55.58
0.11
0.05
0.46
0.84
0.85
PO
Al O
2
CaO
100
MnO
FeO
2
2
0.00
0.18
0.35
0.11
0.00
0.58
99.73
0.00
0.24
0.17
0.07
0.03
0.19
98.14
0.00
0.28
0.84
0.24
0.05
0.64
98.89
0.01
0.30
0.82
0.08
0.04
0.59
99.96
0.00
0.26
0.24
0.04
0.05
0.22
93.92
0.00
0.10
11.39
0.02
0.02
0.01
78.87
0.00
0.13
14.91
0.02
2.38
0.16
91.29
0.00
0.09
16.12
0.01
1.89
0.15
96.36
0.00
0.16
12.37
0.03
1.66
0.11
95.52
0.00
0.14
18.34
0.04
2.46
0.09
Cl
BaO
95.80
SO
TiO
Total
0.11
9.27
0.18
0.10
15.80
12.50
9.62
0.11
0.12
35.95
0.02
16.44
13.57
7.65
0.00
0.00
0.09
0.06
39.97
0.00
14.91
12.50
8.72
0.22
0.03
0.03
2.95
0.16
0.16
38.73
0.00
16.85
12.95
8.48
0.22
0.18
0.03
2.86
0.17
0.12
33.53
0.01
15.82
11.62
9.15
0.20
0.07
S-10
2121.5
0.24
13.13
0.01
0.07
2.28
S-10
2121.5
0.12
9.26
15.96
37.61
0.12
0.03
RL-4
2117.5
0.15
12.92
0.03
0.16
2.17
RL-4
2117.5
0.08
8.82
16.18
37.54
0.15
0.02
RL-4
2117.5
0.13
12.31
0.05
0.36
2.42
RL-4
2117.5
0.06
7.77
16.14
37.10
0.15
0.05
RL-4
2117.5
0.02
13.39
0.00
0.33
2.49
RL-2
1982
9.05
16.22
37.13
0.15
0.02
16.12
RL-10
2303
Na2O
11.19
0.02
0.07
2.46
16.31
RL-10
2140.7
F
16.79
36.12
0.21
0.03
16.99
0.19
Sample #
K2O
0.00
0.56
2.46
17.08
0.14
0.00
biot.
MgO
36.43
0.14
0.02
16.35
0.16
0.00
89.88
biot.
Al2O3
0.22
2.39
16.85
0.20
0.00
97.17
biot.
P2O5
0.14
0.03
15.83
0.14
0.00
95.96
biot.
SiO2
2.34
16.60
0.16
0.00
93.28
biot.
CaO
0.01
17.66
0.22
0.00
95.05
biot.
TiO2
18.27
0.15
0.00
96.24
biot.
SO
Cl
2
0.15
0.00
94.88
biot.
FeO
0.10
0.00
94.19
biot.
MnO
0.00
94.67
biot.
BaO
94.61
mineral
Total
Table C3 (continued)
101
0.25
0.15
14.19
9.09
0.35
0.14
0.00
15.72
12.22
9.09
0.39
0.18
0.25
28.57
0.00
14.13
12.00
7.25
0.06
1.18
0.15
0.24
31.87
0.03
14.82
13.59
9.03
0.08
0.10
0.16
0.08
37.15
0.00
15.19
14.06
8.55
0.09
0.11
S-5
2003
0.15
8.50
14.28
35.30
0.09
S-5
2003
0.30
10.72
0.00
0.03
S-5
2003
0.07
7.48
12.49
36.20
0.14
S-16
2056
0.26
14.42
0.00
0.01
S-16
2056
0.09
7.34
15.58
28.15
0.15
S-16
2056
0.00
12.47
0.02
0.04
S-16
2056
0.03
9.05
16.41
37.19
0.15
3.04
S-14
1942.5
0.00
13.30
0.00
0.08
2.47
0.03
S-14
1942.5
6.16
15.26
26.77
0.09
1.88
0.01
15.26
S-10
2121.5
13.24
0.00
0.68
3.34
0.00
13.59
Sample #
17.30
37.23
0.16
4.01
0.00
11.75
0.07
biot.
Na2O
0.00
0.30
3.59
0.01
16.73
0.15
0.00
biot.
K2O
34.44
0.15
3.43
0.00
15.93
0.16
0.00
93.80
biot.
MgO
0.55
1.78
0.02
16.65
0.14
0.00
86.12
biot.
Al2O3
0.17
2.71
0.05
15.93
0.13
0.00
77.32
biot.
P2O5
3.02
0.00
14.93
0.15
0.16
93.31
biot.
SiO2
0.02
17.41
0.13
0.11
94.64
biot.
CaO
F
2
16.78
0.08
0.00
80.97
biot.
Cl
2
0.15
0.00
94.82
biot.
FeO
0.12
0.00
81.01
biot.
MnO
0.00
95.65
mineral
BaO
91.84
S-7
1537
S-7
1537
S-7
1537
SO
TiO
Total
S-7
1537
0.10
S-5
2003
0.06
0.06
S-5
2003
0.03
0.08
9.65
S-5
2003
0.11
0.11
9.69
12.22
S-5
2003
0.16
0.22
9.23
12.44
15.48
S-5
2003
4.46
0.20
9.35
12.14
15.62
0.00
S-5
2003
0.09
0.16
8.09
13.08
15.49
0.00
36.62
Sample #
0.10
0.19
5.19
13.90
15.59
0.00
37.82
0.01
biot.
0.11
0.07
6.74
11.94
15.28
0.00
37.75
0.02
0.17
biot.
0.25
0.09
8.48
14.87
17.90
0.01
37.66
0.03
0.00
biot.
Na2O
0.06
6.02
13.27
17.83
0.00
36.70
0.05
0.14
biot.
F
7.93
15.83
14.89
0.00
39.38
0.17
0.17
biot.
K2O
15.59
17.43
0.00
35.31
0.44
0.07
biot.
MgO
15.73
0.00
37.20
0.11
0.09
biot.
Al2O3
0.00
33.76
0.31
0.10
biot.
P2O5
36.82
0.13
0.16
biot.
SiO2
0.26
0.13
biot.
CaO
0.14
mineral
Cl
102
MnO
FeO
2
2
0.00
0.19
14.32
0.02
2.23
92.56
0.00
0.11
16.06
0.00
2.87
92.71
0.00
0.18
14.66
0.00
3.38
93.49
0.00
0.15
15.97
0.01
2.11
96.70
0.00
0.14
14.87
0.01
2.12
93.83
0.00
0.11
15.42
0.03
3.69
96.02
0.00
0.18
16.31
0.01
3.27
94.57
0.00
0.16
16.38
0.03
3.07
95.96
0.00
0.21
16.58
0.03
3.40
94.97
0.00
0.16
16.86
0.02
3.62
TiO
BaO
93.56
SO
Total
Table C3 (continued)
0.16
0.08
15.56
6.35
0.07
0.07
S-8
1833
0.21
9.65
S-8
1833
0.05
14.20
S-8
1833
0.22
8.92
S-8
1833
0.02
14.66
S-7
1537
0.08
8.86
S-7
1537
0.23
13.56
S-7
1537
0.12
9.58
S-7
1537
0.29
12.95
S-7
1537
0.10
7.67
S-7
1537
0.12
9.27
20.11
Sample #
0.14
9.28
18.78
0.02
biot.
0.31
12.59
15.24
0.00
34.46
biot.
0.13
7.49
15.06
0.01
36.09
biot.
0.16
14.41
16.24
0.00
37.71
biot.
0.11
8.96
10.09
0.00
37.30
biot.
0.22
11.17
15.13
0.00
38.45
biot.
9.27
16.93
0.00
24.49
biot.
12.41
18.91
0.00
36.66
biot.
15.31
0.00
36.74
biot.
0.00
38.58
biot.
Na2O
37.14
mineral
K2O
3
MgO
F
2
5
MnO
FeO
SO2
TiO2
Cl
CaO
SiO2
0.00
0.13
16.54
0.03
3.49
0.17
0.06
0.00
0.16
12.97
0.02
2.21
0.15
0.08
0.00
0.17
15.69
0.04
2.13
0.10
0.17
0.00
0.11
15.86
0.03
4.10
0.15
0.03
0.00
0.11
13.85
0.03
2.88
0.16
0.04
0.00
0.18
16.05
0.01
3.16
0.19
0.02
0.02
0.07
16.14
0.02
3.98
0.16
0.00
0.06
0.14
14.37
0.05
4.23
0.18
0.02
0.00
0.27
12.78
0.03
2.59
0.13
0.00
0.00
0.17
13.55
0.00
2.46
0.14
0.17
PO
Al O
2
BaO
93.12
S-7
1537
94.77
S-7
1537
95.84
S-7
1537
95.43
S-5
2003
97.14
S-2
1182.5
69.00
S-16
2056
94.16
RL-14
1985
94.32
S-8
1833
93.50
S-8
1833
94.87
S-8
1833
Total
Sample #
103
F
13.09
9.60
0.00
0.15
0.00
18.60
13.53
9.87
0.04
0.13
0.02
36.78
0.00
18.41
14.20
9.47
0.11
0.14
0.10
0.00
55.52
2.84
0.08
1.71
0.09
2.00
0.00
0.02
0.16
0.31
0.00
0.00
60.71
0.46
0.08
0.11
0.41
0.05
0.00
0.06
0.00
0.66
0.01
0.03
0.00
0.00
61.25
0.07
0.13
0.04
0.01
0.00
0.07
0.03
63.10
0.00
0.00
0.00
0.00
0.00
0.01
62.82
0.09
0.08
0.02
0.00
0.02
0.00
0.06
61.72
0.03
0.94
0.09
0.01
0.00
0.00
60.29
0.14
0.09
0.02
0.08
0.03
0.00
0.00
61.97
0.00
0.22
0.08
0.09
0.02
0.00
61.18
0.24
0.08
0.03
0.00
0.00
0.00
0.03
62.24
0.00
0.09
0.24
0.36
0.00
0.02
60.66
0.39
0.12
0.00
0.12
0.02
0.18
0.05
calc.
K2O
18.61
35.54
0.16
0.27
0.08
62.29
calc.
MgO
0.00
0.02
2.84
0.93
0.00
calc.
Al2O3
35.61
0.16
0.02
0.31
62.42
calc.
P2O5
0.03
2.51
14.15
0.00
calc.
SiO2
0.15
0.02
0.13
63.88
calc.
CaO
2.36
15.28
0.00
calc.
Cl
0.06
0.14
96.44
biot.
TiO2
15.25
0.00
biot.
SO2
0.09
95.85
biot.
FeO
0.00
mineral
MnO
95.00
Na O
BaO
2
Total
Table C3 (continued)
0.00
0.12
0.03
0.00
0.01
0.00
0.00
RL-4
2117.5
0.00
RL-4
2117.5
0.02
RL-4
2117.5
0.12
RL-4
2117.5
0.00
RL-4
2117.5
0.00
0.01
RL-4
2117.5
0.00
0.00
20.84
RL-4
2117.5
0.06
0.00
21.26
20.81
RL-4
2117.5
0.03
0.00
20.59
21.27
0.00
RL-4
2117.5
0.10
0.00
19.85
21.20
0.00
RL-2
1982
0.03
0.00
20.41
21.18
0.00
27.76
Sample #
0.00
0.00
20.57
20.80
0.00
27.55
0.01
chlor.
0.02
0.02
21.25
20.86
0.02
27.19
0.01
0.00
chlor.
0.00
0.01
21.20
21.74
0.00
26.68
0.04
0.00
0.06
chlor.
0.01
21.24
20.93
0.00
27.28
0.04
0.02
0.13
chlor.
15.67
20.98
0.01
27.28
0.02
0.00
0.07
chlor.
Na2O
18.57
0.00
27.49
0.03
0.02
0.08
chlor.
KO
0.00
27.64
0.01
0.01
0.08
chlor.
2
3
MgO
F
2
27.57
0.02
0.01
0.07
chlor.
P2O5
26.58
0.03
0.01
0.13
chlor.
SiO2
0.04
0.01
0.07
chlor.
CaO
0.01
0.06
mineral
Cl
0.01
Al O
TiO2
104
MnO
FeO
2
0.00
0.30
24.81
0.01
88.42
0.05
0.23
18.19
0.00
88.41
0.00
0.22
18.16
0.00
88.95
0.07
0.27
17.93
0.00
87.33
0.02
0.17
18.30
0.03
87.57
0.10
0.15
18.55
0.00
86.92
0.00
0.28
18.80
0.00
88.65
0.02
0.23
19.13
0.00
88.78
0.00
0.25
18.29
0.00
88.15
0.00
0.20
18.46
0.00
SO
BaO
86.03
S-16
2056
Total
S-16
2056
0.04
S-16
2056
0.06
0.00
S-16
2056
0.01
0.09
0.01
S-14
1942.5
0.20
0.07
0.02
16.09
S-14
1942.5
0.03
0.02
0.02
19.08
15.54
S-10
2121.5
0.02
0.06
0.00
18.86
18.29
0.00
S-10
2121.5
0.05
0.00
0.02
16.90
19.83
0.01
21.97
S-10
2041
0.00
0.04
0.02
18.05
17.62
0.01
27.51
0.07
S-10
2041
0.10
0.00
0.04
19.43
19.01
0.00
27.59
0.07
0.01
Sample #
0.00
0.02
0.05
17.65
18.31
0.00
25.84
0.11
0.00
0.06
chlor.
Na2O
0.00
0.03
17.97
18.80
0.00
23.82
0.25
0.01
0.04
0.00
chlor.
F
0.05
18.04
15.45
0.01
21.94
0.10
0.00
0.07
0.00
chlor.
K2O
13.77
20.90
0.00
28.19
0.12
0.01
0.03
0.03
chlor.
MgO
17.21
0.00
17.83
0.61
0.02
0.08
0.02
chlor.
Al2O3
0.00
25.98
0.07
0.11
0.06
0.00
chlor.
P2O5
22.22
0.01
0.00
2.60
0.05
0.25
21.42
chlor.
SiO2
0.15
0.02
0.17
0.02
0.25
20.40
chlor.
CaO
0.02
0.01
0.00
0.31
20.82
chlor.
Cl
0.00
0.01
0.20
23.83
chlor.
TiO2
0.00
0.20
18.40
mineral
SO2
0.22
0.04
17.26
0.00
75.51
0.11
0.00
85.82
18.86
0.00
87.75
0.16
0.02
84.91
15.21
0.00
79.79
0.27
0.00
77.45
22.95
0.00
87.09
0.56
0.00
66.91
25.90
0.11
88.35
FeO
BaO
79.99
MnO
Total
Sample #
chlor.
S-16
2056
chlor.
S-2
1182.5
chlor.
S-2
1182.5
chlor.
S-2
1182.5
chlor.
S-2
1182.5
chlor.
S-2
2085.4
chlor.
S-2
2085.4
chlor.
S-5
2003
chlor.
S-5
2003
chlor.
S-7
1537
Table C3 (continued)
mineral
105
MnO
FeO
SO2
TiO2
Cl
CaO
SiO2
P2O5
Al2O3
MgO
KO
F
2
0.00
0.15
18.77
0.01
1.94
0.08
0.50
31.50
0.01
16.83
15.07
1.69
0.00
0.07
87.60
0.02
0.15
18.99
0.00
0.08
0.01
0.04
25.87
0.03
22.78
19.57
0.01
0.04
0.00
87.53
0.00
0.16
19.55
0.00
0.10
0.03
0.05
26.48
0.00
21.88
19.27
0.02
0.00
0.00
89.00
0.04
0.16
19.50
0.01
0.07
0.01
0.04
26.29
0.00
23.02
19.85
0.00
0.00
0.02
87.59
0.00
0.21
20.77
0.00
0.10
0.00
0.01
26.61
0.00
21.54
18.33
0.01
0.00
0.00
86.93
0.00
0.24
22.98
0.02
0.09
0.01
0.09
26.18
0.00
19.66
16.87
0.62
0.13
0.04
87.79
0.00
0.19
22.80
0.00
0.25
0.00
0.11
27.27
0.00
19.49
17.46
0.03
0.14
0.06
85.72
0.00
0.26
16.29
0.01
0.02
0.01
0.18
27.39
0.00
20.40
21.10
0.00
0.04
0.01
86.13
0.00
0.21
16.79
0.01
0.03
0.01
0.09
27.48
0.00
20.52
20.95
0.02
0.00
0.02
87.14
0.00
0.25
20.59
0.00
0.15
0.00
0.11
29.71
0.00
17.55
18.51
0.17
0.10
0.00
Na O
BaO
86.61
2
Total
0.00
0.01
0.00
0.01
RL-10
2303
0.04
RL-10
1836.5
0.04
0.01
S-8
1833
0.10
S-8
1833
0.00
0.04
S-8
1833
0.00
0.11
0.00
S-8
1833
0.00
S-7
1537
0.04
0.01
S-7
1537
0.00
S-7
1537
0.01
0.02
0.00
S-7
1537
0.03
0.01
24.23
Sample #
0.04
0.02
24.03
23.41
0.04
epid.
0.09
22.95
20.89
0.03
37.58
epid.
0.03
0.00
20.96
19.30
0.00
37.26
chlor.
0.00
23.54
18.53
0.00
28.54
chlor.
0.01
0.91
14.58
20.82
0.01
29.12
chlor.
0.07
13.13
13.76
0.00
28.79
chlor.
0.00
18.05
13.32
0.00
28.19
chlor.
20.11
16.39
0.00
18.79
chlor.
20.81
0.00
17.48
chlor.
Na2O
0.00
29.93
chlor.
KO
27.42
mineral
2
3
MgO
F
2
5
TiO2
Cl
CaO
SiO2
0.01
0.07
0.00
0.03
0.00
0.83
0.03
0.19
0.03
0.03
0.00
0.02
0.00
0.04
0.01
0.03
0.00
0.03
0.01
0.08
0.01
0.10
0.00
0.06
0.02
0.08
0.00
0.03
0.00
0.07
0.00
0.00
0.01
0.35
0.00
23.04
0.00
0.04
0.00
23.07
PO
Al O
2
SO2
106
Total
BaO
MnO
FeO
87.50
0.12
0.29
18.57
87.12
0.00
0.17
20.58
62.68
0.06
0.25
18.21
64.85
0.00
0.24
17.32
86.22
0.13
0.33
13.04
88.26
0.00
0.14
19.63
86.83
0.07
0.23
14.91
87.55
0.00
0.26
13.56
96.30
0.00
0.11
12.01
96.86
0.00
0.26
11.61
RL-14
1985
RL-14
1985
RL-14
1985
RL-14
1985
RL-4
2117.5
S-10
2041
Table C3 (continued)
RL-14
1985
0.00
RL-14
1985
0.01
0.02
RL-14
1985
0.14
0.00
0.01
RL-14
1985
0.00
0.16
0.00
0.00
Sample #
0.00
0.12
0.50
0.01
0.03
21.69
epid.
0.02
0.08
0.05
0.00
0.22
24.96
epid.
0.00
0.00
0.11
0.00
0.03
31.27
epid.
0.03
0.05
0.06
0.00
0.03
23.69
epid.
0.02
0.00
0.00
0.00
0.01
23.75
epid.
0.00
0.07
0.00
0.00
0.04
25.95
epid.
0.00
0.01
0.00
0.06
29.49
epid.
Na2O
0.00
0.00
0.04
24.82
epid.
K2O
0.00
0.02
22.96
epid.
MgO
0.02
22.71
epid.
Al2O3
mineral
PO
F
5
FeO
SO2
TiO2
Cl
CaO
2
0.00
13.53
0.00
0.03
0.00
23.40
33.64
0.02
0.09
12.78
0.01
0.00
0.00
23.51
37.50
0.03
0.00
10.64
0.02
0.05
0.00
23.77
37.82
0.00
0.11
5.86
0.01
0.04
0.01
23.90
38.48
0.03
0.00
10.22
0.00
0.00
0.00
23.57
38.20
0.15
0.04
11.73
0.03
0.00
0.00
23.76
37.49
0.13
0.02
12.07
0.02
0.02
0.00
23.38
37.49
0.00
0.14
3.60
0.01
0.03
0.03
24.10
39.08
0.00
0.44
10.08
0.07
0.03
0.05
22.39
36.59
0.00
0.09
12.72
0.00
0.01
0.00
22.98
34.82
2
MnO
0.00
SiO
BaO
92.38
S-7
1537
94.86
S-7
1537
99.10
S-7
1537
97.03
S-2
2085.4
97.15
S-2
1182.5
98.10
S-16
2056
98.01
S-16
2056
97.22
S-16
2056
96.99
S-10
2041
93.33
S-10
2041
Total
Sample #
epid.
0.03
epid.
0.00
epid.
0.05
epid.
0.10
epid.
0.04
epid.
0.19
epid.
0.08
epid.
0.10
epid.
0.01
epid.
0.01
mineral
Na2O
107
Total
BaO
MnO
FeO
SO2
TiO2
Cl
CaO
SiO2
P2O5
Al2O3
MgO
KO
F
2
98.33
0.16
0.08
5.30
0.01
0.01
0.03
24.17
38.64
0.03
29.87
0.00
0.01
0.03
94.40
0.00
0.08
9.64
0.00
0.09
0.01
23.25
35.62
0.09
25.42
0.00
0.00
0.18
95.16
0.00
0.11
14.78
0.01
0.25
0.01
22.30
36.77
0.05
20.63
0.14
0.00
0.00
94.34
0.00
0.15
15.86
0.01
0.21
0.01
22.27
35.95
0.00
19.70
0.01
0.02
0.07
97.01
0.00
0.10
9.44
0.02
0.03
0.01
23.16
37.60
0.02
26.39
0.00
0.06
0.00
97.30
0.00
0.04
14.09
0.02
0.10
0.01
23.07
37.58
0.05
22.24
0.00
0.00
0.05
95.89
0.00
0.13
12.15
0.00
0.12
0.01
23.06
36.80
0.01
23.45
0.00
0.02
0.05
94.66
0.00
0.04
18.33
0.01
0.18
0.01
21.78
36.54
0.02
17.34
0.24
0.11
0.00
96.17
0.00
0.24
11.62
0.02
0.34
0.01
23.00
36.69
0.07
24.04
0.06
0.05
0.03
95.82
0.00
0.53
11.81
0.01
1.20
0.01
22.23
36.87
0.01
23.05
0.01
0.05
0.03
RL-10
2303
Table C3 (continued)
RL-10
2303
0.03
RL-10
1836.5
0.04
0.08
RL-10
1610
0.02
0.00
1.99
RL-10
1610
0.20
0.00
0.10
3.53
RL-10
1610
0.33
0.00
1.11
0.05
3.33
RL-10
1610
0.03
0.04
0.01
2.11
0.07
0.00
RL-10
1610
0.03
0.03
0.00
0.01
5.21
0.00
83.18
RL-10
1610
0.12
0.05
0.04
0.01
0.19
0.00
98.32
0.15
S-8
1833
0.19
0.00
0.01
0.00
0.03
0.00
84.42
0.01
0.05
Sample #
0.04
0.00
0.00
0.01
0.02
0.03
98.17
0.22
0.01
0.41
qtz.
Na2O
0.00
0.00
0.00
0.29
0.00
98.00
0.05
0.02
0.01
0.00
qtz.
F
0.05
0.00
0.39
0.00
98.67
0.11
0.00
0.40
0.01
qtz.
K2O
0.00
0.43
0.00
98.08
0.03
0.00
0.00
0.21
qtz.
MgO
24.43
0.00
97.92
0.12
0.00
0.08
0.00
qtz.
Al2O3
0.00
96.20
0.08
0.00
0.00
0.00
qtz.
P2O5
38.03
0.07
0.01
0.07
0.00
qtz.
SiO2
23.36
0.03
0.07
0.00
qtz.
CaO
0.00
0.02
0.00
qtz.
Cl
0.00
0.03
epid.
TiO2
0.02
mineral
SO2
108
Total
BaO
MnO
FeO
96.88
0.01
0.03
10.91
97.07
0.01
0.00
0.09
98.61
0.00
0.00
0.02
98.74
0.07
0.00
0.03
98.96
0.01
0.02
0.12
98.83
0.05
0.02
0.11
98.68
0.00
0.00
0.04
97.59
0.00
0.01
3.86
98.75
0.01
0.00
0.11
96.68
0.13
0.02
3.79
0.00
0.01
0.00
0.01
0.03
0.00
0.00
0.00
0.01
98.14
0.00
0.02
0.00
0.00
0.00
0.04
0.01
1.59
84.05
0.04
7.80
0.00
0.09
0.00
4.23
0.00
0.01
0.00
0.00
94.69
0.00
0.04
0.00
0.01
0.00
0.02
S-5
2003
0.00
0.00
0.00
0.01
0.10
0.00
S-2
2085.4
0.01
0.00
0.02
96.49
0.00
0.01
0.00
S-16
2056
0.00
0.00
0.00
0.02
0.04
0.03
0.00
S-14
1942.5
0.04
0.00
0.00
99.37
0.00
0.03
0.00
RL-4
2117.5
0.05
0.03
0.00
0.06
0.02
0.26
0.03
RL-4
2117.5
0.04
0.02
0.06
98.36
0.00
0.00
0.02
RL-4
2117.5
0.00
0.00
0.00
0.00
0.00
0.06
0.01
RL-14
1985
0.00
0.08
0.18
98.43
0.00
0.08
0.00
RL-14
1985
0.18
0.00
0.01
0.03
0.00
0.00
0.00
RL-10
2303
0.04
0.74
98.60
0.00
0.02
0.00
Sample #
F
0.00
0.00
0.10
0.02
0.21
0.01
qtz.
K2O
0.10
97.30
0.01
0.00
0.01
qtz.
MgO
0.00
0.15
0.01
0.17
0.01
qtz.
Al2O3
96.25
0.00
0.02
0.00
94.79
qtz.
P2O5
0.06
0.01
0.15
0.00
97.97
qtz.
SiO2
0.00
0.00
0.02
98.58
qtz.
CaO
0.01
0.21
0.00
96.65
qtz.
Cl
0.03
0.00
99.56
qtz.
TiO2
0.11
0.00
98.63
qtz.
SO2
0.01
98.75
qtz.
FeO
0.04
99.22
mineral
MnO
98.53
Na O
BaO
96.84
2
Total
Sample #
qtz.
S-7
1537
qtz.
S-7
1537
qtz.
S-7
1537
qtz.
S-7
1537
qtz.
S-7
1537
seric.
RL-26
2001
seric.
S-8
1686.8
sph.
RL-10
1610
sph.
RL-10
1610
sph.
RL-10
1610
Table C3 (continued)
mineral
109
FeO
SO2
TiO2
Cl
CaO
SiO2
P2O5
Al2O3
MgO
KO
F
2
0.00
0.17
0.00
0.04
0.00
0.01
99.71
0.01
0.01
0.01
0.02
0.00
0.04
0.01
0.01
0.05
0.01
0.00
0.01
0.00
89.73
0.00
0.02
0.00
0.02
0.00
0.00
0.00
0.04
0.00
0.02
0.02
0.00
0.00
98.61
0.00
0.09
0.00
0.00
0.00
0.04
0.03
0.02
0.00
0.02
0.02
0.00
0.00
98.02
0.00
0.04
0.01
0.01
0.00
0.00
98.95
0.08
0.00
0.02
0.02
0.02
0.00
0.01
98.71
0.00
0.04
0.00
0.00
0.03
0.04
77.04
0.09
0.02
1.39
0.01
0.52
0.00
0.03
36.02
0.00
27.80
1.78
8.98
0.07
0.31
98.28
0.08
0.04
1.09
0.02
1.36
0.00
0.01
49.46
0.00
35.71
1.21
9.16
0.00
0.14
97.26
0.00
0.03
1.70
0.01
37.06
0.00
27.91
29.60
0.05
0.89
0.00
0.01
0.00
0.02
97.07
0.00
0.12
1.22
0.00
37.38
0.00
27.38
29.59
0.09
1.17
0.00
0.02
0.03
0.06
98.21
0.00
0.02
1.86
0.00
38.09
0.02
27.35
29.42
0.07
0.92
0.00
0.04
0.37
0.06
Na O
MnO
0.00
98.16
2
BaO
98.82
0.01
89.86
0.07
100.04
0.04
0.00
Total
0.10
RL-4
2117.5
0.00
0.01
RL-4
2117.5
0.00
RL-2
1982
0.01
0.00
RL-14
1985
0.00
RL-14
1985
0.01
0.00
RL-14
1985
0.23
RL-14
1985
0.04
0.06
RL-10
2303
0.00
RL-10
1836.5
0.05
0.08
0.00
RL-10
1836.5
0.10
0.00
2.12
Sample #
0.00
0.02
0.00
3.53
0.06
sph.
0.13
0.00
2.19
0.25
30.39
sph.
0.03
0.45
1.27
1.13
0.10
30.50
sph.
0.12
0.00
1.19
0.08
25.49
sph.
0.07
0.09
0.00
0.72
0.06
30.52
sph.
0.17
0.11
1.62
0.06
32.25
sph.
0.02
0.00
1.15
0.09
30.42
sph.
0.00
3.35
0.03
30.37
sph.
2.85
0.03
30.62
sph.
Na2O
0.06
30.10
sph.
KO
30.34
mineral
2
3
MgO
F
2
5
TiO2
Cl
CaO
SiO2
0.00
35.54
0.00
28.65
0.00
34.29
0.00
28.25
0.01
37.81
0.00
28.01
0.00
36.00
0.00
28.33
0.00
38.29
0.00
28.65
0.01
35.07
0.00
27.18
0.01
37.52
0.01
28.40
0.00
33.62
0.00
26.52
0.00
32.56
0.01
28.69
0.00
36.03
0.00
28.75
PO
Al O
2
SO2
110
Total
BaO
MnO
FeO
98.42
0.00
0.02
0.68
96.97
0.00
0.00
0.70
99.38
0.00
0.03
1.03
98.79
0.00
0.01
2.19
99.40
0.00
0.00
1.13
98.87
0.00
0.03
1.50
98.77
0.00
0.00
1.08
89.07
0.00
0.04
1.11
97.18
0.00
0.02
1.48
98.41
0.00
0.06
0.92
Table C3 (continued)
0.09
0.03
0.40
0.05
4.15
0.01
0.02
0.35
0.03
0.07
4.30
0.00
0.04
0.19
0.87
0.04
0.14
0.46
0.03
0.20
0.01
0.04
2.62
0.00
0.09
0.17
0.05
S-7
1537
0.07
0.00
0.00
S-5
2003
0.00
0.04
4.83
S-2
1182.5
0.00
0.33
0.03
S-16
2056
0.00
0.05
1.49
30.20
S-16
2056
0.01
0.16
0.04
0.04
30.30
28.27
S-14
1942.5
0.00
0.03
2.22
33.67
27.64
S-14
1942.5
0.00
0.00
0.05
0.05
23.50
26.08
0.00
S-14
1942.5
0.00
0.00
0.11
2.58
30.58
26.45
0.00
35.57
S-10
2041
0.04
1.06
31.03
28.60
0.00
39.12
0.00
RL-4
2117.5
Na2O
0.00
0.04
26.82
27.99
0.00
32.98
0.01
0.93
Sample #
K2O
4.50
30.65
26.68
0.00
28.43
0.03
0.34
0.03
sph.
MgO
0.47
30.32
28.51
0.00
32.69
0.00
0.72
0.03
0.00
sph.
Al2O3
30.69
28.39
0.01
36.61
0.00
2.31
0.02
0.00
97.98
sph.
5
28.87
0.00
32.87
0.00
0.83
0.00
0.00
98.33
sph.
PO
F
2
0.00
35.19
0.02
1.09
0.00
0.00
98.97
sph.
CaO
0.00
37.82
0.01
1.48
0.06
0.00
85.25
sph.
Cl
33.68
0.01
1.01
0.01
0.00
98.03
sph.
TiO2
0.00
0.95
0.03
0.00
98.84
sph.
SO2
0.29
0.07
0.00
90.24
sph.
FeO
0.00
0.00
98.34
sph.
MnO
0.00
98.66
mineral
BaO
98.55
S-7
1537
S-7
1537
S-8
1833
RL-10
1610
RL-10
1836.5
RL-10
1836.5
RL-10
1836.5
RL-10
2140.7
RL-10
2140.7
RL-10
2303
SiO
2
Total
Sample #
zeo/cly
9.79
zeo/cly
6.20
zeo/cly
1.42
zeo/cly
0.13
zeo/clyy
0.10
zeo/clyy
0.17
zeo/clyy
0.34
sph.
0.12
sph.
0.01
sph.
0.01
mineral
Na2O
111
Total
BaO
MnO
FeO
SO2
TiO2
Cl
CaO
SiO2
P2O5
Al2O3
MgO
KO
F
2
98.67
0.00
0.05
1.10
0.02
34.79
0.01
28.20
30.56
0.22
3.23
0.04
0.20
0.23
98.07
0.00
0.00
1.01
0.01
36.63
0.00
27.89
30.48
0.02
1.85
0.00
0.06
0.10
96.98
0.00
0.03
0.87
0.02
29.18
0.00
22.63
33.36
0.04
8.48
0.15
1.79
0.31
84.85
0.00
0.03
1.54
0.01
0.02
0.06
2.80
54.74
0.01
21.13
4.00
0.18
0.00
91.33
0.00
0.07
0.72
0.01
0.01
0.03
3.06
55.45
0.02
28.42
2.46
0.92
0.00
83.81
0.00
0.00
2.16
0.05
0.01
0.01
2.04
52.22
0.01
25.72
0.93
0.33
0.24
87.53
0.02
0.01
1.74
0.02
0.09
0.01
1.85
51.45
0.00
31.19
0.63
0.20
0.19
91.43
0.00
0.00
0.05
0.00
0.00
0.00
8.30
62.98
0.00
18.64
0.00
0.02
0.00
81.46
0.00
0.00
0.03
0.00
0.00
0.01
7.66
53.21
0.02
14.12
0.00
0.04
0.15
94.54
0.01
0.01
0.01
0.00
0.00
0.00
4.87
51.06
0.00
28.74
0.00
0.00
0.05
TiO2
Cl
CaO
SiO2
P2O5
Al2O3
MgO
K2O
F
Na2O
mineral
Sample #
0.00
0.00
0.01
8.52
64.68
0.02
18.74
0.00
0.06
0.03
0.12
zeo/cly
RL-10
2303
0.00
0.00
0.00
6.48
65.71
0.00
16.94
0.01
0.37
0.05
0.18
zeo/cly
RL-10
2303
0.00
0.01
0.00
4.00
50.96
0.00
31.03
0.00
0.00
0.00
7.62
zeo/cly
RL-10
2303
0.00
0.00
0.00
7.93
59.38
0.00
16.25
0.00
0.02
0.00
3.08
zeo/cly
RL-10
2303
0.00
0.00
0.00
6.30
59.22
0.02
16.91
0.00
0.43
0.13
0.54
zeo/cly
RL-10
2303
0.02
0.00
0.00
6.17
58.33
0.00
17.05
0.01
0.21
0.00
0.04
zeo/cly
RL-10
2303
0.02
0.00
0.02
2.16
43.20
0.00
31.03
0.72
1.41
0.27
0.17
zeo/cly
RL-14
1985
0.00
0.00
0.01
1.93
37.20
0.02
21.43
0.88
0.56
0.00
0.06
zeo/cly
RL-14
1985
0.00
0.03
0.01
11.09
35.60
0.00
22.10
0.19
0.53
0.08
2.78
zeo/cly
RL-14
1985
0.00
0.00
0.08
2.18
37.93
0.00
19.88
1.00
0.88
0.00
0.09
zeo/cly
RL-14
1985
Table C3 (continued)
SO2
112
FeO
0.32
0.01
0.04
0.00
0.01
0.00
1.21
0.02
0.31
0.00
0.30
0.02
0.34
S-16
2056
0.00
zeo/cly
0.00
S-16
2056
0.22
0.00
zeo/cly
0.00
0.04
S-16
2056
0.27
0.13
0.00
zeo/cly
0.00
2.39
0.00
S-16
2056
0.27
0.15
20.82
0.00
zeo/cly
0.14
2.58
0.01
MnO
S-16
2056
0.48
0.08
17.38
44.98
0.00
zeo/cly
0.02
3.08
0.00
2.76
0.02
S-16
2056
0.10
0.01
21.14
43.10
0.12
0.03
zeo/cly
0.00
0.00
0.01
3.16
0.01
0.03
S-16
2056
0.04
0.11
15.37
50.36
0.25
0.02
0.16
zeo/cly
0.00
2.71
0.01
3.62
0.01
0.85
0.12
S-10
2121.5
0.33
0.04
16.96
52.16
0.03
0.02
0.05
0.05
zeo/cly
0.19
0.02
0.01
8.26
0.01
0.58
0.03
0.10
S-10
2041
0.15
0.04
15.87
41.49
0.01
0.03
0.02
0.00
S-10
2041
zeo/cly
0.08
0.01
0.01
2.49
0.00
0.45
0.00
0.08
zeo/cly
1.76
0.86
14.86
60.93
0.18
0.01
0.01
BaO
1.60
0.00
1.48
0.00
8.75
0.01
0.02
0.01
62.41
Sample #
0.00
0.01
26.65
52.24
0.00
0.00
0.00
72.72
mineral
0.90
0.00
0.15
8.33
0.01
0.69
0.00
62.45
F
0.00
27.24
47.17
0.00
0.04
0.00
80.27
K2O
21.96
0.00
2.94
0.01
0.04
0.00
81.98
MgO
0.00
47.31
0.13
0.01
0.02
72.39
83.69
Al2O3
53.87
9.70
0.02
0.04
0.00
67.52
86.76
P2O5
9.43
0.00
0.07
0.00
79.24
93.76
SiO2
0.00
0.00
0.33
0.00
76.36
89.77
CaO
0.01
0.00
0.01
64.75
92.57
Cl
0.01
0.13
0.01
85.77
Total
TiO2
0.01
0.11
0.01
76.06
BaO
MnO
Na O
SO2
0.04
80.05
87.84
2
FeO
0.00
86.28
Total
Sample #
zeo/cly
S-16
2056
0.27
zeo/cly
S-16
2056
0.07
zeo/cly
S-16
2056
0.15
zeo/cly
S-2
1182.5
0.21
zeo/cly
S-2
1182.5
0.16
zeo/cly
S-2
1182.5
0.10
zeo/cly
S-2
1182.5
0.13
zeo/cly
S-2
1182.5
0.08
zeo/cly
S-2
1182.5
0.15
zeo/cly
S-5
2003
Table C3 (continued)
mineral
0.23
Na2O
113
FeO
SO2
TiO2
Cl
CaO
SiO2
P2O5
Al2O3
MgO
KO
F
2
0.00
0.02
0.00
0.00
7.32
42.09
0.00
10.88
0.00
0.05
0.00
0.03
0.00
0.00
0.00
7.80
58.29
0.03
16.29
0.00
0.00
0.00
1.12
0.01
0.02
0.14
2.37
39.54
0.00
18.33
1.67
0.07
0.00
1.52
0.02
0.01
0.01
2.56
54.10
0.00
23.57
3.06
0.69
0.10
0.01
0.01
0.01
0.00
0.02
5.33
55.67
0.00
17.07
0.48
0.29
0.03
0.02
1.83
0.03
0.01
0.03
2.37
56.38
0.02
25.57
3.20
0.84
0.12
0.01
0.68
0.02
0.01
0.02
2.38
50.59
0.01
30.42
2.20
0.89
0.00
0.00
0.67
0.02
0.03
0.02
2.89
44.79
0.01
27.88
1.82
0.83
0.00
0.00
0.69
0.05
0.02
0.03
2.59
49.03
0.03
32.71
2.77
0.81
0.00
0.00
0.64
0.01
0.02
0.04
2.71
31.06
0.01
17.97
0.07
0.46
0.00
S-8
1833
0.02
zeo/cly
0.00
S-7
1537
2.04
0.02
zeo/cly
0.05
0.00
S-7
1537
0.10
5.90
MnO
zeo/cly
0.20
1.87
0.00
S-7
1537
0.09
0.16
0.07
zeo/cly
0.16
3.15
0.00
S-7
1537
0.25
0.09
0.00
zeo/cly
0.07
3.34
0.00
S-7
1537
0.02
0.41
0.11
zeo/cly
0.07
3.09
0.11
S-5
2003
0.32
0.16
0.08
zeo/cly
0.00
5.29
0.16
S-5
2003
0.23
0.30
0.00
zeo/cly
0.09
3.50
19.16
BaO
S-5
2003
0.14
0.66
22.48
0.01
53.14
zeo/cly
0.00
2.97
23.34
0.02
49.73
88.88
S-5
2003
0.42
0.34
28.81
0.01
54.17
79.09
zeo/cly
0.00
3.29
25.59
0.00
53.74
87.34
0.23
2.07
23.46
0.02
50.93
90.59
0.00
1.39
14.09
0.00
52.40
79.22
0.34
18.51
0.01
50.97
85.94
1.43
32.49
0.01
31.26
63.43
Sample #
16.19
0.00
51.76
82.88
mineral
0.02
48.39
60.59
Na2O
37.13
Total
K2O
3
MgO
F
2
5
PO
Al O
2
SO2
TiO2
Cl
CaO
2
0.53
0.01
0.03
0.02
2.94
0.35
0.00
0.00
0.02
2.20
0.49
0.02
0.00
0.04
2.46
0.47
0.00
0.00
0.10
1.88
0.96
0.04
0.02
0.08
2.75
1.21
0.02
0.02
0.04
2.52
1.07
0.03
0.02
0.07
2.49
2.01
0.08
0.02
0.04
3.19
1.26
0.03
0.01
0.05
2.69
0.33
0.03
0.00
0.03
2.03
SiO
FeO
114
Total
BaO
MnO
58.99
0.10
0.02
87.35
0.00
0.00
77.08
0.00
0.00
51.77
0.00
0.02
82.43
0.01
0.00
87.37
0.02
0.00
87.33
0.09
0.00
86.15
0.00
0.04
84.35
0.00
0.00
81.22
0.03
0.00
BaO
MnO
FeO
SO2
TiO2
Cl
CaO
SiO
P2O5
Al2O3
MgO
K2O
F
2
Na2O
mineral
Sample #
84.49
0.03
0.02
0.80
0.02
0.05
0.04
3.14
53.38
0.03
23.54
3.09
0.23
0.00
0.12
zeo/cly
S-8
1833
85.81
0.00
0.01
0.52
0.03
0.02
0.02
3.49
53.55
0.00
24.73
2.64
0.20
0.13
0.48
zeo/cly
S-8
1833
Table C3 (continued)
Total
115
S-2
1718
S-2
2038
S-2
2038
S-2
2066
S-7
1518
S-7
1537
S-7
1537
S-8
1678
Table C4: Sulfide, telluride, and native metal analyses
S-11
2017
0.00
RL-7
1989.5
0.00
66.09
Sample #
0.00
71.06
8.13
born.
0.00
67.33
4.86
25.07
born.
0.01
58.09
5.71
22.80
0.00
born.
0.00
57.17
11.60
24.45
0.03
born.
0.00
62.48
11.20
27.21
0.00
born.
0.00
64.32
9.81
27.48
0.01
born.
0.00
62.78
6.99
26.01
0.02
born.
0.00
66.53
8.07
24.94
0.02
born.
As
64.01
5.93
26.31
0.02
born.
Cu
6.10
24.52
0.00
born.
Fe
28.78
0.00
mineral
S
0.00
0.00
Te
0.00
0.09
0.00
0.08
0.00
0.04
0.00
0.01
0.00
0.18
0.00
0.00
0.26
0.05
0.00
0.39
0.01
0.01
0.26
99.63
0.66
0.00
0.00
0.03
0.02
0.13
99.11
0.06
0.00
0.34
0.04
0.01
0.43
97.64
0.03
0.15
0.00
0.00
0.37
97.59
0.09
0.02
0.00
0.00
97.34
0.02
0.00
0.00
0.00
98.42
0.02
0.02
0.01
0.29
96.65
Ag
Ni
0.02
0.07
97.72
0.00
Co
0.00
97.07
Pb
Se
98.94
Au
Total
116
Sample #
S-8
1678
S-8
2592
S-8
2592
S-8
2592
S-8
2592
born.
U-2
445.7
born.
U-4
451
born.
U-4
451
chc.
RL-7
1989.5
chc.
RL-7
1989.5
0.00
born.
0.01
born.
0.00
born.
0.57
born.
0.00
born.
0.00
mineral
0.00
73.03
0.00
74.76
0.00
66.29
0.00
68.60
As
60.59
65.71
68.59
63.85
61.52
67.42
0.11
Cu
0.05
9.16
4.63
6.99
4.93
9.00
9.37
7.07
5.72
Fe
24.14
21.90
24.90
21.02
24.77
23.34
25.66
0.00
0.07
0.00
24.11
24.99
0.00
0.04
0.00
0.00
26.62
S
0.00
0.05
0.00
0.03
0.00
0.00
0.03
0.00
0.42
0.00
0.07
0.01
0.00
0.31
95.26
0.02
0.00
0.04
0.00
0.00
0.00
0.00
0.14
96.17
0.00
0.02
0.08
0.00
1.95
0.00
0.00
0.00
94.52
0.00
Te
0.07
0.00
0.06
0.01
0.00
0.00
98.28
0.00
Ag
0.00
0.31
0.01
0.00
0.22
96.68
0.00
Pb
0.00
0.00
0.00
0.00
98.71
0.10
Au
0.00
0.00
0.45
97.96
0.00
Ni
0.01
0.00
98.02
0.00
Co
0.71
98.90
S-7
1537
RL-10
2140.7
RL-10
2140.7
RL-10
2172.5
RL-10
2452
RL-9
2023
S-18
1995
S-18
1995
S-18
1995
0.18
Se
100.29
Total
S-11
2017
Table C4 (continued)
Sample #
0.02
cpyr.
0.00
33.81
cpyr.
0.01
31.64
cpyr.
0.00
34.03
cpyr.
0.02
33.59
cpyr.
0.04
33.19
cpyr.
0.01
33.08
cpyr.
0.01
42.56
cpyr.
0.00
33.36
chc.
0.00
76.35
chc.
As
75.95
mineral
Cu
117
S
Fe
20.46
0.49
21.85
0.74
34.35
30.19
0.00
31.67
24.66
0.02
34.33
29.32
0.00
34.34
28.83
0.03
34.27
29.21
0.01
34.10
29.77
0.01
34.07
25.14
0.00
34.73
30.06
0.00
0.01
0.00
0.06
0.00
0.00
0.00
0.01
0.02
0.00
0.00
0.00
0.00
Te
0.00
0.00
0.01
0.02
0.13
0.00
0.00
0.00
0.00
0.02
0.00
98.82
0.01
0.00
0.31
0.01
0.00
0.00
90.90
0.00
0.00
0.16
0.00
0.00
0.00
97.96
0.00
0.15
0.02
0.00
0.35
97.10
0.01
0.00
0.00
0.00
96.74
0.00
Pb
0.00
0.00
0.00
97.10
0.01
Au
0.00
0.02
0.07
99.09
0.02
Ni
0.00
0.31
98.15
0.02
Co
0.00
99.29
0.01
Se
96.92
Ag
Total
S-8
1678
0.02
S-7
1518
0.00
34.05
S-7
1518
0.00
33.66
29.67
S-2
2066
0.01
33.79
28.44
34.28
S-2
2038
0.00
32.80
30.13
33.75
0.00
S-2
1718
0.00
33.43
29.21
34.31
0.00
0.00
S-2
1601
0.03
33.36
29.17
33.98
0.03
0.00
0.00
S-2
1601
0.00
33.60
28.95
34.20
0.00
0.01
0.00
0.41
S-2
1601
0.00
34.28
29.27
33.43
0.01
0.00
0.00
0.18
0.00
S-18
1995
0.02
33.86
30.00
34.08
0.00
0.03
0.00
0.24
0.01
0.01
Sample #
As
33.73
29.41
34.40
0.00
0.01
0.00
0.17
0.00
0.00
0.36
cpyr.
Cu
29.66
33.91
0.02
0.02
0.00
0.33
0.01
0.01
0.00
98.80
cpyr.
Fe
34.58
0.05
0.01
0.00
0.00
0.02
0.00
0.76
96.05
cpyr.
S
0.01
0.07
0.00
0.00
0.00
0.00
0.12
99.27
cpyr.
Te
0.00
0.00
0.00
0.02
0.00
0.00
96.31
cpyr.
Ag
0.00
0.02
0.00
0.01
0.42
97.18
cpyr.
Pb
0.00
0.00
0.02
0.39
96.16
cpyr.
Au
0.02
0.00
0.04
97.42
cpyr.
Ni
0.00
0.19
98.75
cpyr.
Co
0.35
97.51
cpyr.
Se
98.36
mineral
Total
118
RL-7
2017.5
Table C4 (continued)
S-2
2038
0.00
S-18
1995
0.00
0.70
RL-7
2017.5
0.00
1.06
0.60
U-4
482.3
0.00
1.91
0.24
10.29
S-8
2592
0.05
0.13
0.07
0.18
0.05
S-8
2592
0.01
33.11
0.09
0.62
0.00
0.02
S-8
2592
0.00
33.35
28.18
0.05
0.02
13.33
82.38
S-8
1678
0.00
34.07
29.72
33.96
0.03
19.37
0.06
0.30
S-8
1678
0.00
33.44
29.20
34.31
0.00
13.61
0.00
86.27
0.00
Sample #
0.00
33.72
29.48
34.18
0.00
0.02
0.08
67.90
0.00
0.02
gal.
As
33.18
29.20
34.27
0.03
0.01
84.67
0.00
0.01
6.29
elec.
Cu
29.15
34.16
0.01
0.05
0.00
0.00
0.00
0.00
elec.
Fe
34.42
0.00
0.04
0.00
0.00
0.00
0.00
0.00
elec.
S
0.01
0.00
0.00
0.09
0.03
0.02
0.00
cpyr.
Te
0.02
0.00
0.22
0.00
0.00
0.37
cpyr.
Ag
0.00
0.00
0.00
0.00
0.20
cpyr.
Pb
0.25
0.00
0.00
0.28
cpyr.
Au
0.00
0.00
0.07
100.64
cpyr.
Ni
0.01
0.09
101.15
cpyr.
Co
0.22
89.88
mineral
Se
98.66
S-2
1601
95.70
RL-10
2452
97.62
RL-10
2172.5
97.89
RL-10
2172.5
97.51
RL-10
2140.7
97.17
RL-10
2140.7
97.28
S-7
1518
Total
S-7
1518
0.02
U-2
445.7
0.00
0.00
S-8
2592
0.00
0.08
45.86
Sample #
0.01
0.00
46.17
53.29
pyr.
0.01
0.03
45.99
53.47
0.03
pyr.
0.00
0.00
46.34
52.86
0.03
pyr.
0.00
0.04
46.58
52.99
0.00
pyr.
0.01
0.27
45.86
53.52
0.00
pyr.
0.00
0.37
0.01
53.40
0.03
pyr.
0.01
4.51
0.00
0.28
0.01
hess.
As
39.96
1.12
0.21
35.74
hess.
Cu
4.57
11.65
35.51
gal
Fe
19.87
0.09
gal
S
0.01
mineral
Te
119
Se
Co
Ni
Au
Pb
Ag
100.62
0.11
0.00
0.00
0.07
35.99
0.03
103.05
4.39
0.00
0.03
0.05
81.13
0.08
96.15
0.82
0.01
0.02
0.48
0.00
58.73
95.70
0.22
0.00
0.01
0.00
0.00
59.17
99.35
0.00
0.04
0.00
0.00
0.00
0.00
100.70
0.41
0.10
0.05
0.00
0.00
0.00
99.81
0.36
0.05
0.01
0.00
0.00
0.02
99.33
0.27
0.02
0.03
0.16
0.00
0.00
100.15
0.31
0.04
0.00
0.03
0.00
0.01
99.49
0.29
0.00
0.00
0.00
0.00
0.00
Total
Table C4 (continued)
Ag
Te
S
Fe
Cu
As
0.00
0.00
0.00
52.73
43.29
0.04
0.00
20.71
0.00
40.98
28.91
0.51
0.84
4.39
0.00
S-8
2592
Pb
0.06
0.00
S-2
1601
Au
0.00
0.00
Sample #
Ni
0.00
0.00
sylvan.
Co
0.27
96.33
pyr.
Se
96.40
mineral
Total
120
121