MINERALOGY AND GEOCHEMISTRY OF TOURMALINE IN CONTRASTING
HYDROTHERMAL SYSTEMS: COPIAPÓ AREA, NORTHERN CHILE
by
Ana C. Collins
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MASTER OF SCIENCE
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THE UNIVERSITY OF ARIZONA
2010
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_Dr. Eric Seedorff____________________________
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_Dr. Robert Downs___________________________
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2
Abstract
Tourmaline group minerals can be useful for petrogenetic studies due to their
refractory nature, chemical and isotopic variability, and widespread occurrence in many
geologic settings. Near Copiapó, Chile, tourmaline occurs in a wide range of igneousrelated hydrothermal systems with widely varying types of mineral assemblages and
chemical compositions, making this area an exceptional locality for studying controls on
tourmaline chemistry. Copiapó tourmalines cover the majority of known tourmaline
compositions excluding those associated with Li-rich pegmatites. Tourmaline formed in
multiple, complex stages and is commonly intermediate schorl-dravite with a general
progression in later tourmaline generations towards more Fe-rich and Al-deficient
compositions with a dominant substitution of Fe3+ for Al. This compositional trend, along
with the presence of several tourmaline generations, is consistent with time-varying,
relatively oxidizing, saline, acidic, boron-bearing fluids and reflects a greater host rock
influence with progressive hydrothermal alteration. Tourmalines from other saline
environments, both mineralized and otherwise, show similar compositional trends,
reflecting analogous tourmaline-forming fluid compositions. The correlation between
iron enrichment and highly saline fluids may reflect progressively more effective
leaching and transport of iron from the host rock with time. Boron isotope analyses of
tourmaline indicate a mixed fluid source, reflective of both magmatic and evaporitic
sources, and is consistent with previous fluid-related studies of mineralizing fluids
associated with iron oxide-copper-gold (IOCG) mineralization in the Candelaria-Punta
del Cobre district. The study of tourmaline in these settings has the potential to constrain
the origin(s) of this puzzling style of mineralization and can yield insights on the
diversity of conditions under which tourmaline forms.
Introduction
Tourmaline occurs in a variety of geological environments and is a common
accessory mineral in granitic pegmatites, low- to high-grade metamorphic rocks, and
clastic sedimentary rocks. However, hydrothermal environments comprise some of the
most common and diverse occurrences. Tourmaline’s complex composition reflects
changes in its chemical and physical environment which, combined with its refractory
3
nature and wide range of stability, make it well-suited to explore the conditions under
which it formed (Henry and Guidotti, 1985). Consequently, tourmaline has been the
subject of many studies and is useful for investigating differences between contrasting
hydrothermal systems.
Tourmaline is a complex borosilicate mineral group that has a general structural
formula of XY3Z6[T6O18](BO3)3V3W, where X = Na, Ca, K, and □, Y = Li1+, Mg2+, Fe2+,
Mn2+, Al3+, and Ti4+, Z = Al3+, Mg2+, Fe3+, V3+, and Cr3+, T = Si, Al, and B, V = OH, O,
and W = OH, O, and F (Dyar et al., 1998; Hawthorne and Henry, 1999). Usually
tourmaline is considered in terms of its end members, of which there are fourteen IMArecognized species (Table 1; Hawthorne and Henry, 1999). Solid solution in tourmaline is
ubiquitous as simple or coupled substitutions. Table 2 summarizes common exchange
vectors in tourmaline. Al, Fe, Na, Ca, and Mg comprise some of the most important
substituent elements. Li can be important in tourmalines from rare-metal granites and
pegmatites; however, it is minor or absent in most other types of settings (e.g., Henry and
Guidotti, 1985). Documenting and understanding variations in these constituents is
central to interpreting the significance of tourmaline in hydrothermal systems.
Tourmaline is commonly associated with and co-precipitated during the formation of
numerous types of mineral deposits, including copper, silver-gold, tin(-tungsten), massive
sulfide, and uranium deposits, and occurs as breccia cement and clasts, veins, alteration
envelopes and assemblages, and other metasomatic bodies (Slack et al., 1984; Pirajno and
Smithies, 1992; Slack, 1996; Xavier et al., 2008). Tourmaline is commonly the principal
host of boron in these deposits, and its durability allows it to preserve a detailed record of
its formation even when dispersed during weathering and erosion. Tourmaline chemistry
reflects the diverse compositions of both host rock and hydrothermal fluids, as well as
differences in temperature and pressure of formation. This compositional record provides
insight into mineralizing conditions, fluid flow, and possible sources of constituents in
hydrothermal systems (e.g., in magmatic-hydrothermal systems: Pirajno and Smithies,
1992; Mlynarczyk and Williams-Jones, 2006; Dini et al., 2008; those sourced from
external fluids: Palmer and Slack, 1989; Peng and Palmer, 2002; Xavier et al., 2008).
Major-element trends have been used as guides for exploration (i.e., Clarke et al., 1989).
For instance, Fe/(Fe+Mg) ratios in tourmaline vary systematically in Sn and Sn-W
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hydrothermal deposits, with ratios decreasing with increasing distance from the magmatic
source of mineralizing fluids and increasing interaction with the host rock (Pirajno and
Smithies, 1992). Boron isotopes in tourmaline have been used to fingerprint the source of
mineralizing fluids and can provide new insight as to the metallogenesis of various
hydrothermal deposits (Palmer and Slack, 1996; Xavier et al., 2008). The abundance of
tourmaline can also serve as a prospecting guide for undiscovered borate bodies and
stratabound mineral deposits (Peng and Palmer, 2002; Slack, 1982). Care must be taken
when using tourmaline as an exploration tool, as the compositions can be strongly
influenced by the composition of the host rock, and the final composition may reflect an
amalgamation of multiple sources and chemical interactions.
Relatively little work has been done on the mineralogy and stability of tourmaline in
many high-temperature hydrothermal systems, and tourmaline petrology and
geochemistry have only recently been considered in iron oxide-copper-gold (IOCG)
deposits (i.e., Xavier et al., 2008). IOCG systems are characterized by voluminous
magnetite and/or hematite, variable amounts of Cu- and Fe-sulfides, gold, and REE, and
low Ti contents compared to most igneous rocks (Hitzman et al., 1992; Barton and
Johnson, 1996; Williams et al., 2005). In contrast to porphyry-type systems, magmatic
compositions play only a secondary role on IOCG alteration mineralogy and elemental
abundances (Barton and Johnson, 1996). IOCG deposits are generated by hypersaline,
variably CO2-bearing, Cl-rich, and S-poor fluids, are formed at shallow to mid-crustal
levels, and are closely associated with variably intense and voluminous sodic(-calcic) and
potassic alteration. The origins of the ore-forming fluids are unsettled: they might be
exsolved from magmas (Marschik and Fontboté, 2001; Sillitoe, 2003; Pollard, 2006) or
be derived from external, evaporitic brines (Barton and Johnson, 1996; Xavier et al.,
2008). Thus, understanding tourmaline in these settings has the potential to elucidate and
constrain the origin(s) of this puzzling style of mineralization and, in well-chosen cases,
can yield an independent set of constraints on the diversity of conditions under which
tourmaline forms.
This study systematically looks at igneous-related tourmaline occurrences in the
Copiapó region of northern Chile, a part of the Chilean Iron Belt and one of the world's
classic areas for IOCG mineralization (Marschik and Fontboté, 2001; Sillitoe, 2003). This
5
area is also the locus for widespread, though economically unimportant, porphyry copper
mineralization (Maksaev et al., 2007). The first part of this project evaluates the
petrographic, chemical, and isotopic characteristics of tourmaline in the diverse
hydrothermal environments present near Copiapó, of which the IOCG systems in the
Candelaria-Punta del Cobre district are pre-eminent examples. We then use this record to
interpret the chemistry of the various hydrothermal fluids, the role of host rocks, and the
identity of potential fluid sources. This involves geochemical and simple thermodynamic
interpretations of the chemical and isotopic compositions in conjunction with ancillary
data from other studies. Finally, we compare the Copiapó tourmaline patterns to those of
tourmalines from other hydrothermal systems with the goal of gaining better insight into
the controls on tourmaline composition in various hydrothermal settings and its use for
interpreting their origins.
Tourmaline-bearing hydrothermal systems near Copiapó
Geologic context
Chilean Coastal Batholith and related hydrothermal systems: Northern Chile contains
a spatial and temporal progression of sub-parallel belts of iron, copper, and gold-rich
hydrothermal systems (Fig. 1). Within the westernmost portion of these belts, the Late
Jurassic to Early Cretaceous Coastal Batholith and related volcanic rocks of northern
Chile host numerous hydrothermal systems, which fall mainly along the Chilean Iron
Belt and can be divided into deposits affiliated with the IOCG class (Marschik and
Fontboté, 2001; Sillitoe, 2003) or deposits of the porphyry copper family (e.g., Maksaev
et al., 2007). Although the abundance of tourmaline within the Chilean Iron Belt and in
younger porphyry copper deposits has long been recognized (e.g., Sillitoe and Sawkins,
1971), little detailed work has been done with regard to tourmaline geochemistry and its
genetic implications in this region or elsewhere.
The Chilean Iron Belt occurs principally along the long-lived Atacama fault system
and its various splays. Hydrothermal alteration of sodic(-calcic), potassic, and hydrolytic
types is nearly ubiquitous (Barton et al., 2005: unpublished mapping). The porphyry
copper hydrothermal systems are present in association with the most felsic intrusive
centers (tonalite to granodiorites), whereas IOCG deposits form independently of
6
magmatic composition and occur mainly in intrusive and volcanic rocks with
intermediate compositions (e.g., diorites, tonalites, andesites) and to a lesser extent in the
broadly coeval clastic to carbonate sedimentary rocks of the Early Cretaceous
Chañarcillo Group (Marschik and Fontboté, 2001; Williams et al., 2005). Deposits range
from magnetite-rich accumulations mined solely for iron with but minor amounts of
copper mineralization to those with variable but typically abundant hematite (or
magnetite replacing hematite) that commonly have more abundant copper, locally present
in economic quantities (Sillitoe, 2003; Williams et al., 2005).
Candelaria-Punta del Cobre district: The Candelaria-Punta del Cobre district is
located in the Chilean Coastal Cordillera about 20 km south of Copiapó and contains a
number of deposits that are classic examples of the IOCG family (Fig. 1; Williams et al.,
2005)). The Candelaria deposit has proven reserves of 368 Mt at 0.55 percent Cu, 0.11
percent Au, and 1.97 percent Ag and probable reserves of 23 Mt at 0.54 percent Cu, 0.11
percent Au, and 1.91 percent Ag (Freeport-McMoran, 2009). The combined deposits
from the Punta del Cobre district contain reserves of >120 Mt at 1.5 percent Cu, 0.2 – 0.6
g/t Au, and 2 – 8 g/t Ag (Marschik and Fontboté, 2001). Smaller, vein-hosted deposits
occur elsewhere in the region, the largest of which contains upwards of 10 Mt of ore with
grades of >1.5 percent Cu.
The Candelaria and Punta del Cobre deposits are hosted by volcanic and
volcaniclastic rocks of the Punta del Cobre Formation, that underlie evaporite-bearing,
carbonate-dominated sedimentary rocks of the Chañarcillo Group (Marschik and
Fontboté, 2001). The deposits contain chalcopyrite, magnetite, hematite, and pyrite as the
principal ore minerals, with minor sphalerite and, at Candelaria, metamorphic pyrrhotite.
The andesites of the Punta del Cobre Formation are intensely potassically altered over a
large region, including the areas that host the IOCG mineralization; locally, the upper
parts of the Punta del Cobre Formation contain high metal grades, but ore-grade
mineralization is nearly absent in the overlying Chañarcillo Group (Ryan et al., 1995). To
the west of Candelaria and Punta del Cobre, the Copiapó batholith intrudes the
supracrustal rocks and consists of calc-alkaline plutons that range from diorite through
monzodiorite, quartz monzonite and tonalite, to granodiorite. These plutons range in age
from 119 to 95 Ma and have O, Os, Pb, Nd, and Sr isotopic signatures indicative of
7
mixed mantle and crustal sources (Mathur et al., 2002; Marschik and Söllner, 2006; M.D.
Barton, unpublished data). Although the plutons contain voluminous sodic(-calcic)
alteration and minor IOCG vein deposits (Barton et al., 2005; Kreiner and Barton, 2009),
none of these intrusions appears to be associated with the IOCG mineralization in the
older rocks (e.g., not found either through mapping or exploratory drilling), nor is there
any recognizable zonation of alteration or mineralization away from the batholith. In
contrast, local porphyry-style mineralization is linked to particular granodioritic
intrusions (Ryan et al., 1995; Barton et al., 2005). Conversely, the batholith is clearly
responsible for a well-developed, 1-3 km wide metamorphic aureole that contains
widespread copper-poor skarn alteration in the carbonate rocks and has deformed and
overprinted the ores in the adjacent Candelaria deposit, but not in the more distal
orebodies of the Punta del Cobre district (Fig. 1).
Mineralization involved multiple magmatic, metamorphic, and metasomatic events,
with a diverse set of structural controls and incontrovertible evidence from crosscutting
relationships for discrete episodes of mineralization.
Ar-Ar geochronology yields ages on silicate alteration minerals that can be broken
into two groups: an older group of about 114 to 116 Ma and a younger group of 110 to
112 Ma with broadly similar Re-Os ages (115 Ma) on molybdenite from Candelaria
(Mathur et al., 2002). Although Marschik and Fontboté (2001) argue that copper
mineralization displays a close spatial and temporal correlation with post-magnetite,
calcic amphibole alteration, magnetite is abundant and widespread throughout the
deposit, and there appears to be no direct correlation between copper grades and the
extent of magnetite mineralization (Ryan et al., 1995). Moreover, geologic evidence,
including crosscutting relationships in dated rocks from the Punta del Cobre side of the
district, indicates that at least some and perhaps much of the mineralization is of Punta
del Cobre age (ca. 130 Ma) and predates the batholith (Pop et al., 2000; M.D. Barton,
unpublished data).
Most workers in the district have inferred a magmatic source of hydrothermal fluids
based on the isotopic similarity of the ores and igneous rocks and sulfide sulfur isotopic
compositions that are near zero per mil (e.g., Mathur et al., 2002). Even in these proposed
magmatic systems, however, the participation of non-magmatic fluids in mineralization
8
has not been ruled out (Marschik and Söllner, 2006), and recent work has demonstrated a
significant component of external, non-magmatic fluids in the ores and related alteration
(Barton et al., 2005; Chiaradia et al., 2006).
Tourmaline occurrences in the Copiapó region
Petrographic characterization of tourmaline in over 100 polished thin sections (out of
more than 1000 available sections) has been carried out as part of a multi-disciplinary
geologic and geochemical study of the region (M.D. Barton and others, in progress). The
optical properties, mineral assemblages, and timing relationships were determined using
standard transmitted and reflected light techniques. Tourmaline is by far the most
common boron mineral in the Copiapó area, although datolite and dumortierite also occur
locally (Ryan et al., 1995; Kreiner and Barton, 2009). Tourmaline occurrences are diverse
and include: occurrences with pluton- and volcanic-hosted IOCG mineralization of
multiple styles and with several alteration types, high-temperature veins associated with
biotite(-hornblende) quartz monzodiorites, locally in the contact metamorphosed rocks,
and in many areas with intensely sodicly-altered, metal-depleted rocks. With the
exception of tourmaline associated with quartz-feldspar assemblages in some of the
granitoids, nearly all tourmaline is quite fine-grained (<100 microns), rather massive,
and, therefore, subtle in appearance. This may account for the sparse attention that it has
received in earlier studies.
Petrographic studies, summarized in Table 3, show that tourmaline formed during
multiple stages of hydrothermal activity, as indicated by crosscutting, overgrowth, and
replacement relationships. Appendix 3 contains petrologic descriptions of each sample
that was analyzed chemically for major and minor elements. Tourmaline is scarce in the
Candelaria deposit, perhaps because of highly alkaline conditions which may have
produced some of the late datolite (Ryan et al., 1995). Conversely, tourmaline is
abundant in the little metamorphosed Punta del Cobre district. Tourmaline is also found
in iron-dominated IOCG occurrences, such as the Cerro Iman and Cerro Negro Norte
deposits. Tourmaline occurs as euhedral columnar, granular, massive, and acicular grains
(Fig. 2B) in veins (as the dominant or an accessory mineral), breccia cement, brecciated
9
clasts (Fig. 2A), and as part of alteration assemblages (Fig. 2H) in advanced argillic,
potassic, sericitic, sodic, and sodic-calcic types of alteration assemblages (Fig. 2).
Characteristics of Tourmalines in the Copiapó Area
Tourmaline from multiple localities within the Copiapó area were analyzed via
electron microprobe and laser ablation inductively coupled plasma mass spectrometry
(LA-ICP-MS) methods to characterize the chemical and boron isotopic compositions of
tourmaline and associated minerals (see footnotes of Tables 4 and 6 for operating
conditions and Appendix 1 for further details). These results are combined with
petrographic data to document correlations between tourmaline occurrences, textures and
optical properties, and to provide the basis for interpreting the significance of tourmaline
in the district.
Tourmaline compositions
Tourmaline from Copiapó varies widely in chemical composition, reflecting
systematic changes associated with types of hydrothermal mineral assemblages and
geologic settings. Overall, tourmalines show the greatest variation in Al, Mg, Ca, Na,
Fe+2 and Fe+3 concentrations and contain insignificant K, Mn, or Cl. Representative
analyses of tourmaline from each sample can be found in Table 4 (complete results are
provided in the Appendix). Structural formulae were calculated on the basis of 15 cations
(T + Y + Z = 15). Light-element (H, Li, B, O) contents were not determined, but boron
was assumed to be stoichiometric (Grice and Ercit, 1993), and hydrogen and oxygen
were adjusted to meet charge balance constraints. Fe+3/Fetotal calculations were derived
from working curves using the methods outlined by Fialin et al. (2004), which is outlined
in detail in Appendix 1.
Analyses of Copiapó tourmalines largely fall within the alkali compositional group
defined by Hawthorne and Henry (1999) (Fig. 3). The composition of the mineral
assemblage exerts the primary control on tourmaline compositions that plot outside of the
alkali compositional field. Alkali-deficient tourmaline from the advanced argillic type of
hydrothermal mineral assemblage contain little Ca and plot along the base of the ternary
diagram along the [Na(Mg,Fe)](□Al)-1 exchange vector (refer to Table 2 for a list of
common exchange vectors). Tourmalines from calcic assemblages show a core-to-rim
10
progression from moderately sodic to calcic end members along the NaAl[Ca(Mg,Fe)]-1
exchange vector in response to increasing Ca concentration with progressive evolution of
the hydrothermal system.
Figure 4 shows discrimination diagrams for common tourmaline end members.
Tourmaline compositions trend from alkali-free (magnesiofoitite-foitite) to dravitic
compositions (Fig. 4A) or from schorl-dravite to calcic (uvite-feruvite) end members
(Fig. 4). These latter compositions reflect the overall assemblage, commonly towards
non-acidic compositions, with higher Fe, Mg, Na, and/or Ca. For the most part, early
tourmalines trend from intermediate schorl-dravite compositions to another tourmaline
compositional end member.
Overall, the majority of tourmaline corresponds to the dravite-schorl solid-solution
series (XMg = 0.06 – 0.98) with a dominant trend towards povondraitic compositions.
Copiapó tourmalines cover the majority of known tourmaline compositions in the Al-FeMg and Ca-Fe-Mg compositional diagrams of Henry and Guidotti (1985), occupying all
fields except that associated with Li-rich pegmatites (Figs. 5 and 6), denoting a wide
array of possible exchange vectors. Within the Al-Fe-Mg diagram, the greater proportion
of tourmaline generations fall within field 6, representing Fe3+-hydrothermally altered
quartz-tourmaline, calc-silicate, and metapelitic rocks. According to Henry et al. (1999),
tourmaline samples that fall below the schorl (buergerite)-dravite join are Al-deficient
(less than 6 apfu Al) and either Fe- or Ca-Mg-rich. In the absence of a substantial calcic
component, which would result in the coupled substitution of Ca and Mg or Fe2+ for Na
and Al, it can be inferred that Fe3+ is a major substituent of Al in the Z-site to maintain
charge balance (Fig. 7A). The implications of this will be covered in further detail in the
discussion.
The elements that display the greatest variation are plotted in Figure 7 to show
potential exchange vectors that may play a role in the chemical complexity of Copiapó
tourmaline. For the most part, tourmaline compositions (with the exception of those from
potassic assemblages) do not fall along the schorl-dravite solid-solution line (Fig. 7B).
Al-deficient tourmaline tends to plot along the CaMg(NaAl)-1 or the FeAl-1 exchange
vector, whereas tourmalines with slightly more than 5.5 apfu Al appear to lie along the
□Al(NaMg)-1 exchange vector, as indicated by the negative slope in Figure 7C and the
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increasing influence of X-site vacancies in tourmalines with greater than 5.5 apfu Al (Fig.
8). Tourmalines from sodicly and some sericitically altered rocks appear to be largely
dominated by the FeAl-1 exchange vector (Fig. 7C). Magmatic tourmalines, as well as
tourmalines from sodic-calcic, potassic, and some sericitic assemblages, display a
dominant negative correlation between Al and Ca, whereas sodic and advanced argillic
tourmalines show no correlation (Fig. 7E). Overall, tourmalines trend from greater than 6
apfu Al to less than 6 apfu Al contents.
Petrography and assemblage data
Petrographic studies suggest that tourmaline was deposited in several stages of
hydrothermal alteration and is found in association with many diverse types of mineral
assemblages (see Table 3). Elongate tourmaline crystals show evidence of crack-seal
mechanisms for their formation, indicative of multistage development of tourmaline at
the vein scale. Tourmaline compositions reflect both the host rock and fluid source
characteristics and are strongly controlled by the mineral assemblage. In the following
sections, tourmaline-bearing mineral assemblages are discussed especially in terms of
their influence and correlation to tourmaline chemical variations.
Advanced argillic assemblages: Advanced argillic alteration assemblages are stable
under extremely acidic conditions (i.e., low pH or low aK+/aH+, broadly coincident with
the stability of kaolinite, pyrophyllite, or andalusite in originally K-feldspar-bearing
rocks) (Seedorff et al., 2005). Tourmaline-bearing advanced argillic assemblages in the
Copiapó area are both hydrous and anhydrous. Hydrous tourmaline-bearing samples
contain dumortierite, pyrophyllite, hematite, calcite, andalusite, and quartz. Tourmaline is
light tan to light blue-brown with Mg concentrations increasing from core to rim. The
latest generation of tourmaline growth, occurring as comb-like needles on preexisting
tourmaline, is more aluminous than the earlier phases (Fig. 9). Overall, these tourmalines
have high F contents compared to other assemblages from the Copiapó region.
It is likely that this assemblage represents a metamorphic overprint by the batholith or
preexisting advanced argillic assemblages in the volcanic rocks. The two chemically and
morphologically distinct generations of tourmaline represent discrete periods of growth
possibly reflective of formation before and following the emplacement of the intrusion.
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Early Fe-rich cores, possibly accompanied by other Al-rich phases such as albite, were
replaced by dumortierite and pyrophyllite, a low temperature, Al-rich, Na-poor
assemblages with a fine-grained, calcitic groundmass. Dumortierite and pyrophyllite are
then replaced by Mg-rich tourmaline, which is common for metamorphic environments
(Henry and Dutrow, 1996), and calcite is recrystallized to form equant interlocking
grains. Hematite probably formed early and was replaced by magnetite during the
metamorphic overprint. Late hematite after magnetite ("martite") then formed during
some later event.
Higher temperature, largely anhydrous, advanced argillic assemblages contain finegrained, acicular tourmaline in association with andalusite, quartz, hematite, and minor
sericite and lazulite (Fig. 2B). The presence of andalusite in these assemblages may
suggest a contact metamorphic overprint. Tourmalines from these assemblages have a
narrow range of XMg values (0.58 – 0.61), are highly aluminous, alkali-deficient (XNa
<0.7 apfu), and plot along the dravite-magnesiofoitite, □Al(NaMg)-1, exchange vector
(Fig. 7C).
Sericitic-chloritic assemblages: Sericitic-chloritic assemblages are stable is an acidic
environment, though at somewhat higher pH or higher aK+/aH+ conditions than those
characteristic of advanced argillic alteration (Seedorff et al., 2005). Tourmalines present
in within sericitic or chloritic assemblages range from well formed to poorly formed with
corroded grain boundaries. The compositions of tourmaline in these assemblages vary
greatly, trending from foitite to schorl-dravite and commonly plot along the exchange
vector Na(Mg, Fe)(□Al)-1. Tourmalines are progressively enriched in Fe, possibly
indicative of an increase of host rock control on tourmaline composition.
Periods of distinct growth and dissolution are particularly noticeable in tourmalines
from sample C2J-124, in which both early and late tourmaline have embayed cores and
inclusion edges. Any zones that are present are commonly discordant. C2J-124 appears to
have at least four generations of tourmaline, with an early aluminous, vacancy-rich, light
blue-gray tourmaline generation followed by brown, Mg-Fe-rich anhedral tourmaline.
Well-formed tourmalines in sericitic assemblages are found in the vicinity of the San
Gregorio pluton. Overall, albite phenocrysts in these rocks are intact and only display
sericitic alteration in the presence of tourmaline. In this case, tourmalines trends from
13
schorl to feruvite, which is possibly correlated to the breakdown of magmatic pyroxene
or amphibole. A later brown, Mg-rich schorl generation, intergrown with titanite,
contains among the highest Ti concentrations in the dataset. In other samples from this
area, the relationship to sericitic alteration is unclear (i.e., intact tourmaline vein with
scant amounts of partially sericitized plagioclase).
Sodic assemblages: Sodic assemblages form as a result of Na-enrichment of host
rocks by highly saline fluids (Seedorff et al., 2005). Albite is the most common mineral
associated with tourmaline in these assemblages and is the only other sodic phase.
Hematite and Fe-sulfides or sulfates are the next most abundant association. Sodiclyaltered rocks commonly have volcaniclastic or volcanic protoliths and are variably
overprinted by breccias associated with hydrothermal alteration. Tourmaline is common,
typically occurring as part of the breccia cement or in veinlets. These tourmaline are
largely dravitic and commonly trend from Al-saturated to slightly Al-deficient
compositions. Tourmalines that occur with specular hematite are Al-deficient and Ferich, commonly falling within the schorl-buergerite compositional field, and are
intricately zoned, which may be indicative of a fracture-fill style of formation. Early
phases are granular, Mg-rich, and contain higher F (up to 0.19 apfu) and Ti than later
generations, which become progressively more Fe-rich through time. In some cases, there
is no compositional continuity between different tourmaline generations, indicating
distinct tourmaline-forming conditions. Moreover, the grain boundaries of the earliest
generations are not embayed, showing that they were not destabilized by the later
mineralizing fluid.
Sodic-calcic assemblages: Sodic-calcic alteration is associated with the addition of
Na ± Ca by hot (>350°C), saline fluids resulting in higher temperature assemblages than
those associated with sodic alteration (Seedorff et al., 2005). Tourmalines from sodiccalcic assemblages are commonly dravitic to uvitic in composition and operate along the
exchange vector CaMg(NaAl)-1. These tourmalines also tend to have higher Ti values.
Epidote, titanite, actinolite, and calcite are common minerals that occur with tourmaline
in these assemblages. Tourmalines are also found in association with actinolite as part of
a calcic overprint on earlier, potassically altered assemblages as evidenced by abundant
biotite with chlorite in mafic sites. Similarly, calcic overprints on sodic assemblages are
14
also present, with early cores of unzoned, dravitic tourmaline slightly replaced by albite
and later rimmed by calcic, euhedral tourmaline. The overall increase in Fe, Mg, and Ca
moving from core to rim, which is evident in all samples, implies that reacting fluids
became increasingly enriched in these elements during tourmaline formation.
Tourmalines occur as veins and isolated clusters. Vein tourmaline occurs in sodiclyaltered rocks with albite or in calcicly-altered rocks with actinolite and/or epidote.
Compositionally, vein tourmaline trends from sodic to calcic compositions and generally
has sharp boundaries with included minerals. In some cases late generations of
tourmaline may have reaction rims (Fig.10) and commonly have dravitic overgrowths.
Tourmaline clusters are generally well formed, but may have irregular edges in the
presence of epidote.
Tourmalines from the aureole of the San Gregorio pluton are the most oxidized and
Fe-rich samples in the dataset. These tourmalines plot along two different exchange
vectors: CaFe(NaAl)-1 (schorl-feruvite substitution) and FeAl-1 (schorl-povondraite
substitution). This is readily evident in Figures 7A and 7E, where both Ca and Fe
concentrations show a negative correlation with Al content. Accordingly, tourmaline
compositions progress from the compositional ranges normally associated with Li-rich
granites in the earliest generations to that of Fe-rich hydrothermally altered rocks in the
latest generation, as shown in Figure 5.
Potassic assemblages: Potassic assemblages are stable in highly alkaline
environments with high aK+/aH+ ratios. Potassic alteration commonly occurs at high
temperatures and is linked to magmatic-dominated fluids (Seedorff et al., 2005). The
majority of drill core samples from Santos, believed to represent the intermediate levels
of the hydrothermal system, are characterized by potassic alteration (biotite ± K-feldspar)
with actinolite, epidote, and albite present locally (Marschik and Fontboté, 2001).
Allanite can also be locally abundant. Tourmalines from this area either occur as veins,
breccia clasts and cement, part of the alteration envelope, in altered clasts, or columnar
crystals commonly in larger biotite grains. Breccia clasts are indicative of a history of
repeated brittle deformation as well as distinct phases of tourmalinization. These Santos
samples are predominantly dravitic and either trend towards more Fe-rich or Mg-rich
compositions. For example, tourmalines from the deepest sample (DDH628-626.3) in the
15
dataset tend to plot mostly in the Li-poor granite field with trends towards Alundersaturated and intermediate schorl-dravite compositions from core to rim (Fig. 5).
However, this chemical progression is not systematic, given that elemental abundances
fluctuate at the micron scale (Fig. 11). At higher levels in the hydrothermal system,
Santos tourmalines trend from the Al-saturated and Al-undersaturated metapelitic fields
towards more Fe-rich and Al-deficient compositions (Fig. 5). Although tourmalines from
different depths appear to have different geneses, the compositions of their later
generations overlap, suggesting a second-order control on tourmaline chemistry other
than depth (e.g., interaction with wall rocks).
Potassic alteration postdates sericitic alteration in some areas, as evidenced by late
tourmaline-biotite veins in a sericitic matrix (i.e., sample C2B-576c). Whereas Santos
tourmalines are distinctly chemically zoned, these tourmalines are light blue in
transmitted light, unzoned, and largely fall within field 4 of Figure 5 associated with Alsaturated phases.
Optical characteristics: The petrographic characteristics of tourmaline vary
considerably, and pleochroic color and intensity do not always correlate with chemical
composition. In general, tourmaline is weakly to strongly pleochroic. The pleochroic
characteristics of tourmalines from each sample are summarized in Table 5. In the case of
pleochroic tourmaline, strong optical absorption and pleochroism suggest that the
tourmaline may contain significant amounts of Fe with mixed valences (2+ and 3+),
resulting in intervalence charge transfer (Mattson and Rossman, 1987). On the other
hand, tourmaline that contains monovalent iron should exhibit weak absorption. Nonpleochroic tourmaline tends to also be complexly zoned and dark in color. An interesting
characteristic of some of the vein tourmaline associated with the San Gregorio pluton is
their intense pleochroism and optical characteristics. Sample C2B-655 contains
tourmalines that are nearly optically opaque in thin section, similar to the ferridravite
(now recognized as povondraite) species identified by Walenta and Dunn (1979). These
are also some of the most Fe-rich tourmalines, suggesting that optical opacity may be
related to high Fe concentrations relative to Al.
Although Fe2+ => Ti4+ charge-transfer has been cited as the cause for blue color in
kyanite and dumortierite (Parkin et al., 1977; Platonov et al., 2000), blue tourmaline from
16
Copiapó samples have among the lowest Ti concentrations and the highest Fe values in
the dataset, suggesting that Fe is the primary chromophore. Brown colors appear to
correspond to Mg and Ti contents, although Ti content in the Copiapó tourmaline is
highly variable. Taylor and Slack (1984) interpreted the blue to black colors associated
with schorl to be dominantly influenced by Fe2+ => Fe3+ and O2- => Fe3+ charge-transfer
processes, and the brown hues of dravite by uv-centered O2- => Fe2+ and Fe2+ => Ti4+
processes.
Copiapó tourmalines are generally optically zoned, sometimes spectacularly, varying
from concentric to highly irregular. The color change can be either gradational or display
sharp optical discontinuities. Cores range from irregular (common) to euhedral with
euhedral to corroded rims. Unzoned tourmalines are brown or blue. The complexity of
zoning evident in thin section and backscattered-electron imaging (Fig. 12) is reflected in
the compositional variation of tourmalines from even one thin section.
Summary
Tourmalines formed in distinct episodes of mineralization in diverse mineral
assemblages. Copiapó tourmaline is commonly pleochroic and optically and chemically
zoned. The chemical variation evident in tourmaline from this area is a function of fluid
composition and type of hydrothermal mineral assemblage. Tourmaline compositions
operate on a variety of exchange vectors, with Fe, Mg, Al, Na, and Ca contents showing
the greatest variation. Most notably, tourmalines from all types of assemblages (except
advanced argillic) show a negative correlation between Fe and Al (Fig. 7A).
Copiapó area tourmalines largely have sodic compositions. However, advanced
argillic assemblages contain the most aluminous and alkali-deficient tourmalines in the
dataset. Calcic tourmalines (operating along the Ca(Mg,Fe)(NaAl)-1 exchange vector) are
found in sodic-calcic, potassic, and some sericitic types of hydrothermal mineral
assemblages. Magmatic tourmalines, however, also show a dominant negative correlation
between Al and Ca. Tourmalines within sericitic types of hydrothermal mineral
assemblages consist of two distinct populations: one that is aluminous and trends toward
more Fe-rich compositions and another that is more calcic as the result of the breakdown
of magmatic mafic minerals (i.e., pyroxene or amphibole). Sodic alteration assemblages
17
contain tourmalines that show the same trend as some sericitic assemblages, but display
more compositional scatter that is dominated by substitution along the FeAl-1 exchange
vector. Tourmalines present in potassic types of alteration assemblages are the only
tourmalines to plot along the FeMg-1 exchange vector and, along with sodic-calcic
tourmalines, also trend towards more Fe-rich compositions.
Boron isotopic compositions
Boron isotopic analyses were accomplished via LA-ICP-MS techniques at the
University of Arizona. Isotope ratios for selected coarse-grained samples and analytical
methods are presented in Table 6. Given the fine-grained nature of most Copiapó area
tourmaline, these results are quite selective. δ11B values range from -7.5 – +4.2 per mil,
with over half of the analyses falling below -1 per mil (Fig. 13). The most positive values
come from vein tourmaline in sample C2B-352e, which is considered the clearest and
simplest example of magmatic tourmaline in the vicinity of the San Gregorio pluton.
Thus, this would indicate a mixed boron source or equilibration of magmatic boron with
the host rock, thus driving δ11B values to more positive values.
Smith and Yardley (1996) found that isotopically lighter tourmaline was associated
with Fe enrichment and Li enrichment in the Cornwall district. However, there is no
observed correlation between elemental abundances and isotopic composition in the
Copiapó tourmaline, nor is there any correlation between δ11B values and tourmaline
morphology or sample locality. Overall, there appears to be variations in isotope
compositions where no chemical zoning is evident. The variation from magmatic to more
positive values is indicative of the influx of a source with a positive signature. Potential
sources will be covered in further detail in the discussion.
Controls on Tourmaline Compositions
Tourmaline compositions reflect the host rock and hydrothermal fluid compositions
with progressive evolution of the hydrothermal system, as well as differences in
temperature and pressure of formation. This compositional record provides insight into
mineralizing conditions, fluid flow, and possible sources of constituents in hydrothermal
systems. Although tourmaline has a wide range of stability, it is strongly controlled by
the composition of the mineralizing fluid and associated mineral assemblage.
18
Tourmaline stability
Stability of tourmaline end-members: Tourmaline is stable over a broad range of
pressure and temperature conditions (Henry and Dutrow, 1996); however, the
composition of tourmaline solid solutions should be governed by the coexisting mineral
assemblages and fluid compositions. Here we use chemographic techniques combined
with available thermodynamic data to evaluate the effect of independent compositional
variables on tourmaline compositions
Thermodynamic data for minerals and aqueous species from the SUPCRT92 database
(Johnson et al., 1992) were used to create a chemical potential diagrams for several
projections within the system Na2O – B2O3 – Al2O3 – MgO – CaO – SiO2 – HCl – H2O at
400°C and 500 bars. Tourmaline, quartz, and an aluminum mineral are considered to be
saturated throughout each activity diagram. The fugacity of oxygen is defined by
magnetite-hematite.
Comparing modeled and measured tourmaline compositions provides information on
the conditions prevailing in its host environment. Tourmaline stabilities for
magnesiofoitite – dravite and dravite – uvite end members are plotted in Figure 14. In
highly acidic environments, magnesiofoitite predominates over dravite. Dravite is stable
in environments with high Na and Mg activities, whereas uvite stability appears to be
constrained to lower Mg and higher Ca activities.
Stability of tourmaline: Tourmaline has a wide range of stability from low to high
temperatures and pressures (<150°C to >700°C and 1 bar to >10 kbars) but is strongly
influenced by the composition of the fluid phase and mineral assemblage (Henry and
Dutrow, 1996). The solubility of aluminosilicate phases and components (e.g., Al) in
borate fluids increases with increasing fluid alkalinity and may be indicative of changing
speciation mechanisms in solution as a function of pH (Morgan and London, 1989).
Thus, minerals containing relatively large amounts of alkalis that react with water to
produce alkaline solutions inhibit tourmaline growth, as tourmaline formation is favored
in strongly to weakly acidic fluids (Frondel and Collette, 1957; Morgan and London,
1989). Moreover, the minimum aqueous boron necessary to stabilize tourmaline increases
with increasing temperature and pH. Above pH 6.5, no level of boron can stabilize
19
tourmaline and another boron-bearing phase forms. This would explain the absence of
authigenic tourmaline in most evaporitic deposits (Henry and Dutrow, 1996).
The activity of Al2O3 or equivalent aqueous species also contributes to tourmaline
stability and formation, which are favored in acidic fluids with high availability of Al
species. However, since Al transport is facilitated by alkali borate species, such as
Na2B4O7, a mixture of acidic and alkaline boron compounds is essential to provide the
necessary Al for tourmaline-forming reactions (Morgan and London, 1989). Oxygen
fugacity (fO2) is another important constraint on tourmaline stability (Morgan and
London, 1989). Irregular distributions of tourmaline could reflect limited boron and water
availability, variable fO2, and restricted mobility of mafic cations (e.g., Fe and Mg)
necessary for tourmaline formation (Gawęda et al., 2002).
Stability of tourmaline relative to other boron-bearing minerals: Tourmaline is the
most common borosilicate in geologic environments. In highly alkaline and/or silica- or
aluminum-undersaturated conditions, however, tourmaline growth is inhibited and other
borosilicates form instead (Grew, 1996). High Ca concentrations, or high Ca/Al ratios,
may not be favorable for the formation of tourmaline, and boron may be distributed in
other species, such as danburite, serendibite, and axinite, to name a few (Frondel and
Collette, 1957). Like tourmaline, danburite (CaB2Si2O8) is preferentially stable in acidic
fluids (Morgan and London, 1989). In highly acidic environments, dumortierite occurs
over tourmaline due to the lack of alkalis, Fe, and Mg necessary for tourmaline formation
(Taner and Martin, 1993). However, water is a key component for dumortierite formation
(Werding and Schreyer, 1990). Tourmaline that does occur with dumortierite tends to be
alkali-deficient, with some proportion of Na, and Al-rich, commonly with tetrahedral Al
(Foit et al., 1989). Other borosilicates, such as serendibite, commonly form in calcic,
silica-undersaturated conditions, and tourmaline that forms in these settings are typically
uvitic (Grew, 1996).
Major-element variation
Copiapó tourmalines are compositionally complex and formed in multiple
generations. Most of the compositional variability observed in these tourmalines involves
Al and Fe with lesser involvement of Mg and the alkalis. This could reflect the changing
20
nature of the mineralizing fluid as it interacts with the host rock, becoming increasingly
oxidized and Fe-rich.
Zoning: Tourmaline chemical composition readily responds to changes in its chemical
environment. According to several authors (e.g., Taylor and Slack, 1984; Dutrow et al.,
1999; Henry and Dutrow, 1996), a large, external influx of boron is commonly
accompanied by the generation of considerable amounts of unzoned, weakly zoned,
oscillatory zoned, and/or complexly zoned tourmaline. The fine, oscillating chemical
zoning of a wide range of cations of varying charge and density recorded in tourmaline
suggests that cation diffusion in tourmaline is slow (Palmer et al., 1992). Zoning in
Copiapó tourmaline ranges from concentric to discordant. The complexity of zoning
present in most tourmaline is indicative of open-system behavior, with possible
fluctuations in chemistry, pressure, and temperature. This is demonstrated by periods of
distinct growth followed by dissolution and replacement by tourmaline with a different
composition, as well as fine-scale zonation, which is indicative of rapid growth in a
changing chemical environment (London and Manning, 1995). Dissolution can occur as a
result of changing conditions and can be recognized by discordant zoning patterns with
truncated compositional zones.
Alkali variation: Alkali-deficient compositions can be obtained through the exchange
vector □Al[Na(Mg,Fe)]-1. These tourmalines are associated with alkali-deficient, highly
acid, low-temperature environments (Rosenberg and Foit, 1979). Early, Al-rich cores
reflect growth in Al-rich, highly oxidized, but alkali-poor environments. The formation of
strongly Na-deficient tourmaline requires, for any given temperature, a very low
concentration of Na in the fluid, and it is unlikely that this Na-poor phase is in
equilibrium with other sodic phases such as albite. Metamorphic and synthesized
tourmalines have shown an increase in Na with increasing temperature (Henry and
Dutrow, 1996; von Goerne et al., 2001). Although such generalizations can be made, it is
essential to compare tourmaline composition to the mineral assemblage, as Na content
depends on several parameters (von Goerne et al., 2001). Overall, later generations of
tourmaline have higher alkali (Na and Ca) contents that are commonly reflective of the
alteration mineral assemblages. The alkali-defect exchange vector, □Al[Na(Mg,Fe)]-1,
accounts for the chemical difference observed in most cores.
21
Fe variation: Tourmaline compositions from various localities generally trend toward
or fall within the Fe-rich hydrothermally altered rocks domain in the Al-Fe-Mg diagram
of Henry and Guidotti (1985), suggesting an important host rock control of volcaniclastic
and andesitic rocks. Tourmalines associated with metapelites and metavolcanic terranes
tend to have intermediate schorl-dravite compositions, similar to the early generations of
Copiapó tourmaline. However, there is no consistent correlation between the Fe/(Fe+Mg)
ratio of tourmaline and a particular mineral assemblage (Power, 1968; Taylor and Slack,
1984).
A remarkable feature noted in the majority of tourmalines from the Copiapó region is
the inverse relationship between total Fe and Al. In other studies, the transition from Alrich to Fe-rich compositions has been linked to increasing distance from a magmatic
source coincident with decreasing temperature and increasing differentiation of late
magmatic fluids (Caverretta and Puxeddu, 1990) or from the breakdown of another Febearing phase. Whitney et al. (1995) also found that Fe contents tend to increase with
increasing salinity in sulfur-free systems. Decreasing Al content in tourmaline can be
linked to feruvite-uvite substitution, CaMg(NaAl)-1, and/or povondraite substitution,
FeAl-1 (Bačík et al., 2008). However, subsequent decreases below 5.0 apfu Al necessitate
the substitution of Fe3+ for Al. There is a clear FeAl-1 substitution trend in Copiapó
tourmalines that is indicative of a povondraitic component. An increase in the Fe3+/Fetotal
ratio may reflect the primary oxygen fugacity of the tourmaline-forming fluid, decreased
Al activity, and/or higher overall Fe either from the fluid or increased fluid interaction
with the host rock (i.e., Fe/(Fe+Mg) ratio of tourmaline reflects that of the bulk rock with
progressive alteration; London and Manning, 1995; Gawęda et al., 2002). Galbraith et al.
(2009) noted that the greater the fluid to rock ratio, the greater the evidence for
hybridization of the source fluid and country rock compositions. As Fe is effectively
transported as chloride complexes in hot, relatively acidic and saline solutions, this would
also suggest that later evaporitic fluids were more effective at leaching Fe from the host
rock.
22
Geologic controls
The abundance of tourmaline in the Copiapó area is indicative of acidic, boronbearing hydrothermal fluids. The diversity of tourmaline compositions is a function of
both host rock composition, reflected in later tourmaline generations, and the
composition of the original fluid, which appears to have higher Al concentrations and
lower overall alkali and FeMg contents. It also appears that these hydrothermal fluids
became increasingly oxidized, as reflected by the increase in Fe3+ in later tourmaline
generations. The lack of significant amounts of other borosilicates indicates acidic fluids
with high Al activities and sufficient ferromagnesian components to create tourmaline.
The extensive sodic(-calcic) and potassic alteration in the Copiapó area suggests that
alkalis are not a limiting factor; therefore, conditions for tourmaline formation would
necessitate a driver towards more acidic compositions. An evaporitic source would
provide the chloride ligands necessary for metal transport as well as the Na evident in
hydrothermal alteration, while driving the fluids towards oxidized, relatively S-poor
conditions (Barton and Johnson, 1996). The δ11B values in tourmaline, as with other
compositional studies of fluid compositions in the Candelaria-Punta del Cobre deposits,
suggest a mixed fluid source, suggesting both magmatic and sedimentary influences.
Further evidence of highly-saline, oxidized fluids: Several interesting minerals
indicative of highly saline solutions are scattered throughout the tourmaline-bearing
Copiapó samples. Tourmalines from samples C2J-124 and C7B-003a, associated with
sericitic and advanced argillic assemblages, respectively, contain inclusions of hypogene
anhydrite 10s of microns across. These anhydrite crystals are not present within the
matrix or in any other minerals. Sample C2B-808.2 from the San Gregorio pluton
contains chloro-potassichastingsite, a relatively uncommon Cl-rich amphibole (in this
example containing over 5 wt percent Cl) that is indicative of alkali-chloride
metasomatism (Mazdab, 2003). This mineral appears to be selectively replacing an early
Al-, Fe-rich, blue tourmaline and may be coincident in time with the formation of Mg-,
Ti-rich tourmaline within the same sample. In the Santos mine, marialitic scapolite is also
present in association with tourmaline at depth, although it appears to postdate it. This
scapolite end-member forms at temperatures around 400°C and is only stable in fluids
that contain greater than 40 mol percent NaCl (Vanko and Bishop, 1982).
23
Comparison with other tourmaline-bearing hydrothermal systems
Copiapó tourmaline compositions are compared to other occurrences from IOCG and
other economic deposits, as well as to sediment-dominated systems, to establish any
common crystal-chemical characteristics. Tourmaline compositions that plot along the
“oxydravite”(a hypothetical sodic variation of magnesiofoitite)-povondraite solidsolution line defined by Henry et al. (2008) are considered a consequence of tourmaline
formation in an oxidizing environment, possibly in the presence of high salinity aqueous
fluids with reduced H2O activities (Henry et al., 2008). Povondraite is indicative of high
oxygen fugacity during crystallization (Žáček et al., 1998), and the correlation to highly
saline fluids may reflect more effective leaching and transport of elements from host
lithologies (Henry et al., 2008).
Magmatic-hydrothermal systems (Cu-Mo, Sn-W systems): Tourmaline compositions
in porphyry and other magmatic-hydrothermal ore deposits may contain substantial Fe3+rich and uvitic components (Fig. 15A). The existence of Fe3+-rich hydrothermal
tourmalines in the majority of granitoid-related Cu–Mo–Au deposits suggests formation
under relatively oxidizing conditions, in contrast to tourmalines from Sn–W deposits
which formed under more reducing conditions and lack significant ferric iron (Slack,
1996). In most porphyry Cu-Mo systems, tourmaline compositions range from Mg-rich to
Fe-rich, and mineralization is associated with calc-alkaline to moderately felsic rocks. In
rare cases, vein tourmaline associated with Sn mineralization appears to follow the
povondraite-dravite trend as well. These tourmalines are found in mafic to ultramafic
host rocks and thus have higher Fe contents (Mao, 1995).
IOCG and similar systems: Tourmalines from the Larderello geothermal field in Italy
are similarly Fe-rich (Cavaretta and Puxxedu, 1990). As expected, IOCG-related
tourmaline show the same enrichment in Fe as Copiapó tourmaline (Fig. 15B). Out of all
the IOCG deposits in the Carajás district, the Igarapé Bahia tourmalines appear to be the
most chemically similar to the Copiapó tourmaline. IOCG mineralization is best
developed in the breccias that lie between the mafic metavolcanic and
metapyroclastic/metasedimentary units. Tourmalines from this locality are commonly Ferich dravites (Galarza et al., 2008). Boron isotopic work carried out by Xavier et al.
(2008) points towards an evaporitic origin for these tourmalines, as reflected by high δ11B
24
values. Tourmaline boron isotope results from the Yerington and Humboldt IOCG
deposits in Nevada also show evidence of external, non-magmatic fluid sources for
mineralization, with average values ranging from -0.1 to +6.1 per mil (F.K. Mazdab,
M.D. Barton, and R.L. Hervig, unpublished data) (Fig. 13)
Metamorphic hydrothermal deposits: Tourmalines from various mesothermal Auquartz deposits display intermediate schorl-dravite to dravitic compositions (Fig. 15C)
and appear to be geochemically similar to non-hydrothermal, metamorphic tourmaline.
The composition of these tourmalines reflects both the chemistry of the mineralizing fluid
and the composition of the host rock. Metamorphic hydrothermal tourmaline is most
similar to early, Al-saturated generations of Copiapó tourmaline and do not show the
same “oyxdravite”-povondraite trend.
Stratabound deposits: Stratabound tourmalines, associated with massive sulfide and
other deposits, are commonly dravitic in composition (Slack, 1982) (Fig. 15D). The
compositional variation in these tourmalines is linked to the proportions of hydrothermal
fluids and seawater, the water/rock ratio of the system, and the composition of the host
rock (Slack, 1996). In non-massive sulfide deposits, Mg-rich tourmalines are believed to
have formed through the circulation of a seawater component or a Mg-rich evaporitic
brine. Tourmalines from all of these environments commonly plot along the schorldravite solid-solution and only rarely show the Fe-enrichment evident in Copiapó
tourmaline.
Sediment-dominated systems: Similarly Fe-rich tourmalines are also found in the
Challenger Dome in the Gulf of Mexico (Henry et al., 1999) and in metamorphosed
evaporites (Žáček et al., 1998; Henry et al., 2008) (Fig. 15E). Tourmalines associated
with meta-evaporites are commonly sodic, magnesian, moderately to highly depleted in
Al, and enriched in Fe3+. These tourmalines typically fall along the “oxydravite”povondraite join. Peng and Palmer (2002) found that although tourmalines may not be
directly related to meta-evaporites, they may still exhibit an isotopic and fluid influence
from meta-evaporitic sources.
Tourmaline compositions that deviate from this trend likely reflect other
superimposed reactions and a probable influx of reactive fluids. Tourmalines associated
with the Barberton Greenstone in South Africa are very Al-enriched, even though they
25
are found in association with volcanics and evaporites, suggesting that the mineralizing
fluid was far more aluminous than other evaporite-related areas (Byerly and Palmer,
1991).
Notably, the Mg-rich tourmalines from the Fowler talc belt, New York (Ayuso and
Brown, 1984), display similar characteristics to the distinctive early Mg-rich, Al-deficient
generation in a sodic alteration assemblage observed in the Al-Fe-Mg ternary diagram
and fall in field 8 of Figure 5, which is associated with metacarbonate or metapyroxenoid
hosts. Ayuso and Brown (1984) hold that these tourmalines formed in specialized
environments associated with evaporites, consequently having a profound effect on the
bulk composition. Moreover, tourmalines from this locality also have heavy δ11B values
(+13 ‰)
Origin of boron isotope systematics
Boron is highly mobile and easily leached and redistributed, especially under alkaline
pH conditions (Dutrow et al., 1999). Tourmaline clearly shows a close relationship with
certain distinct types of geologic settings, including quartz monzodiorites, IOCG
deposits, and sodicly altered rocks but is not present or rare in other types of rocks and
mineral deposits (e.g., porphyries, diorites, and some vein type IOCG occurrences).
Although boron may be present in the latter settings, other conditions such as high
alkalinity may have inhibited tourmaline formation (Morgan and London, 1989).
In general, boron isotopic data show no correlation between mineral formation
temperature, major-element composition, mineral assemblage, or age of deposit (Palmer
and Slack, 1989; Swihart and Moore, 1989). Moreover, the mechanical and chemical
stability of tourmaline prevents significant boron isotope fractionation, preserving its
boron isotopic signature through time (Slack et al., 1989). However, boron isotope
systematics are sensitive to pH, as it determines the relative abundance of B(OH)3 and
B(OH)4 complexes in solution, and to the lithologic setting (Palmer and Slack, 1989).
The dominant control on δ11B values in tourmalines is the composition of the boron
source (Slack et al., 1989). As 10B is preferentially incorporated into the solid phase
during fluid-solid interactions, tourmaline δ11B values are systematically lower than the
liquid from which it forms and are minimum estimates of the actual fluid composition
26
(Slack et al., 1989). Fractionation experiments predict a 5 per mil to 8 per mil difference
between the mineralizing fluid and tourmaline (Palmer et al., 1992).
As previously mentioned, the results of the boron isotopic work are biased towards
coarse-grained tourmaline because of analytical constraints and thus may not reflect the
complete picture of boron isotope variation in this district. The range of δ11B values of
Copiapó tourmaline from -7.5 to +4.2 per mil overlaps a number of geological
environments including granites, volcanics, metasediments, and non-marine evaporites. It
is highly possible that the boron involved in tourmaline formation came from a mixture
of these sources and maybe others that have more positive or negative δ11B values (see
Fig. 13). Lighter δ11B values can be attained through mixing with a lighter source, such
as granitic and volcanic host rocks, or through the loss of 11B due to vapor phase
separation (Smith and Yardley, 1996), whereas heavier values commonly necessitate a
marine influence. Notably, all of the potential boron sources are present in the Copiapó
region, underscoring the fact that data from even the best isotopic tracers require careful
interpretation and commonly have non-unique interpretations.
Fluid inclusion studies on quartz and ore minerals also support a mixed source for the
origin of mineralizing fluids. The initial Sr isotope compositions of the fluid inclusions
found in Candelaria are notably more radiogenic than the magmatic host rock, thus
providing evidence for a non-magmatic source of Sr (Barton et al., 2005; Chiaradia et al.,
2006). Cl isotopic work further indicates that the ore-forming fluid is a mixture of
magmatic mantle-derived fluids (low radiogenic Sr and 37Cl-rich) with a radiogenic Srrich and 37Cl-poor crustal source such as a basinal brine (Chiaradia et al., 2006).
Chiaradia et al. (2006) suggest that the magmatic fluids mixed with basinal brines or
leached evaporites after exsolution from the magma, necessitating a mixed source model
for the development of these deposits. These results could also be applied to the
tourmaline boron isotope results, where the range from magmatic composition to more
positive values may coincide with the influx of a non-marine brine.
Conclusions
Tourmalines provide a distinctive record of compositional variation in hydrothermal
systems due to its wide range of stability and chemical variability. Tourmaline chemistry
27
can be used to provide a clearer understanding of ore-forming processes, related
depositional environments, and the location of prospective exploration targets.
Compositions of tourmalines from Copiapó reflect formation in oxidizing, acidic, highly
saline environments and compositional trends toward Fe-rich compositions that reflect
the compositions of the host lithologies. These results are consistent with relatively
oxidized fluids that varied in composition through time, suggesting that tourmaline
compositions distinguish different hydrothermal environments, even in the same area.
The trend of tourmalines from Copiapó towards povondraitic compositions and their
similarity to tourmalines from evaporitic sources attest to the highly saline and oxidizing
nature of the mineralizing fluid. As reflected in δ11B values in Copiapó tourmaline, the
boron necessary for tourmaline formation appears to have a mixed signature, with both
evaporitic and magmatic fluid sources, an interpretation that is consistent with previous
fluid inclusion studies in this area. This study is part of an ongoing study of IOCG
mineralization in the Copiapó area and additional research may further constrain the
enigmatic origin(s) of these deposits.
Acknowledgments
This study and associated field work has been financially supported by National
Science Foundation (NSF) grant EAR08-38157, an NSF Graduate Student Research
Fellowship, Science Foundation Arizona, and Freeport-McMoRan Inc. We would like to
thank Ken Domanik for technical assistance with electron microprobe analyses and Mark
Baker for his help creating an analytical method for boron isotope work on the isoprobe.
Thanks also go to Doug Kreiner for providing some of the samples for this study, to
David Cooke for tourmaline compositional data from the Río Blanco Cu-Mo deposit in
Chile, and to Eric Seedorff and Bob Downs for their reviews of this manuscript.
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36
Figure Captions
Fig. 1. Regional geologic map showing the volcanic and sedimentary sequences
intruded to the west by the Cretaceous Copiapó batholith (from Barton et al., 2005,
modified from Arévalo, 1999).
Fig. 2. Photomicrographs in plane polarized light of various tourmaline textures and
mineral assemblages from the Copiapó region. A. DDH643-430.2 (Santos). Tourmaline
clast with magnetite in a chlorite matrix surrounded by quartz. Tourmaline is
intermediate schorl-dravite in composition. B. C6B-160b (Vinita Azul). Advanced
argillic assemblage with acicular, foititic tourmaline, quartz, hematite, and andalusite.
See text for further discussion. C. DDH289-037.5 (Santos). Potassic assemblage with
dravitic tourmaline, biotite, magnetite, and quartz. D. C2B-808.2 (San Gregorio S
Granate). Fe-rich, blue tourmaline cluster with chloro-potassic-hastingsite replacing the
bottom part of the tourmaline cluster. The host is coarse-grained albite. E. C2J-124
(Cerro Buitre Radio Tower). Sericitic assemblage with tourmaline, quartz, sericite, and
zircon. Early violet gray, Al-rich tourmaline generation is rimmed by light brown
tourmaline that is Na- and Mg-rich. F. C3B-429.5 (Ojancos Viejo) Sodic assemblage
with strongly zoned tourmaline, albite, limonite after pyrite, and fine-grained,
indeterminable Al ± Fe sulfate. G. C6B-101b (Falla Ojancos Transito San Francisco).
Granular, dravitic tourmaline intergrown with albite. H. C2J-334 (Cerro Buitre Radio
Tower). Calcic assemblage with uvitic tourmaline and actinolite overprinting earlier
potassic alteration (bioitite). Abbreviations represent: Act = actinolite, Alb = albite, And
= andalusite, Bt = biotite, CPH = chloro-potassic-hastingsite, Hem = hematite, Mt =
magnetite, Qtz = Quartz, SS = sheet silicate, Tour = tourmaline.
Fig. 3. Alkali classification diagram after Hawthorne and Henry (1999). Analyses of
tourmalines from various localities within the Copiapó district are plotted based on
alteration assemblage type. The majority of tourmaline compositions fall within the alkali
compositional group. Tourmalines from advanced argillic assemblages trend towards
vacancy-rich compositions, whereas tourmalines of magmatic origin or in calcic
assemblages trend towards more Ca-rich compositions.
Fig. 4. Discrimination diagrams for naming tourmaline species, with analyses of
tourmalines from the Copiapó district plotted according to type of alteration assemblage.
A. Sodic and vacancy-rich end members. This discrimination diagram shows solid
solutions between Na- and vacancy-rich end members with varying Mg/(Mg+Fe). B.
Sodic and calcic end members. This discrimination diagram shows solid solutions
between Na- and Ca-rich end members with varying Mg/(Mg+Fe).
Fig. 5. Al-Fe-Mg compositional diagram of Henry and Guidotti (1985) with Copiapó
tourmaline analyses plotted based on alteration assemblage type. Common end members
are plotted for reference. Each field delineates various tourmaline-bearing rock types.
Copiapó tourmalines cover the range of known tourmaline compositions outside of
pegmatitic environments. The numbers correspond to distinct rock types: (1) Li-rich
granitoid pegmatites and aplites; (2) Li-poor granitoids and their associated pegmatites
and aplites; (3) Fe3+-rich quartz-tourmaline rocks (hydrothermally altered granites); (4)
37
Metapelites and metapsammites coexisting with an Al-saturating phase; (5) Metapelites
and metapsammites not coexisting with an Al-saturating phase; (6) Fe3+-rich quartztourmaline rocks, calc-silicate rocks, and metapelites; (7) Low-Ca metaultramafics and
Cr-, V-rich metasediments; and (8) Metacarbonates and meta-pyroxenites.
Fig. 6. Ca-Fe-Mg compositional diagram of Henry and Guidotti (1985) with Copiapó
tourmaline analyses. Common end members are plotted for reference. Each field
delineates distinct tourmaline-bearing rock types. The majority of tourmaline analyses
falls within field 4. The numbered fields correspond to: (1) Li-rich granitoid pegmatites
and aplites; (2) Li-poor granitoids and their associated pegmatites and aplites; (3) Ca-rich
metapelites, metapsammites, and calc-silicate rocks; (4) Ca-poor metapelites,
metapsammites, and quartz-tourmaline rocks; (5) metacarbonates; (6) metaultramafics.
Fig. 7. Potential exchange vectors. These figures denote the complexity of tourmaline
compositional trends in this area. As discussed in the text, Copiapó tourmalines are
largely Al-deficient, indicating formation in Al-undersaturated conditions. A. Al vs. Fetot.
Note the negative correlation between Fe and Al. B. Mg vs. Fe graph. The bold line on
the graph indicates the FeMg-1 exchange vector. As is apparent from this graph, the
majority of tourmaline compositions do not fall along the schorl-dravite solid-solution
line. Only tourmalines from potassic assemblages show any correlation. C. Al vs. Na
graph. Tourmalines from sodic-calcic and some sericitic assemblages plot along the
NaAl(CaMg)-1 exchange vector, whereas tourmaline with greater than 6 apfu Al plot
along the NaMg(□Al)-1 exchange vector. Tourmalines from sodicly and some sericitically
altered rocks appear to be largely dominated by the FeAl-1 exchange vector. D. Al+Ca vs
Fe graph after Henry et al. (2008). This graph reinforces the negative correlation between
Al and Fe along the exchange vector FeAl-1. E. Al vs Ca graph. There is a dominant
negative correlation between Al and Ca for magmatic tourmaline, as well as for
tourmaline from sodic-calcic, potassic, and some sericitic assemblages. Sodic and
advanced argillic tourmalines show no correlation. F. X-site-vacancy vs. Ca graph. There
is little correlation between X-site vacancies and overall Ca content.
Fig. 8. Al vs X-site vacancy graph showing that X-site vacancies only begin to take a
role in tourmaline chemical variations at Al contents greater than 5.5 apfu.
Fig. 9. Photomicrograph in plane-polarized light of various stages of tourmaline
growth in hydrous advanced argillic assemblage (sample C7B-003a from Jesus Maria).
The tourmaline core tends to be Mg-rich compared to the later comb-like overgrowth that
is more aluminous. Mineral abbreviations: Cal = calcite, Mar = hematite after magnetite
(“martite”), Tour = tourmaline.
Fig. 10. Backscattered electron image of a complexly zoned tourmaline sample from
San Gregorio (sample C2B-655). This tourmaline shows an early, embayed and slightly
fractured, Fe-rich generation overgrown by an aluminous rim that is later replaced by a
complexly zoned reaction rim with numerous inclusions. Mineral abbreviations: Cal =
calcite, Mt = magnetite, Tour = tourmaline.
38
Fig. 11. Backscattered electron image and X-ray maps for Mg, Na, Fe, Ca, and Ti of
tourmaline in Santos sample DDH628-626.3, showing micron-scale chemical variations
and coalescence phenomena (subrounded cores overgrown by sub- to euhedral rims)
(Pesquera et al., 2005), most evident in the Ca X-ray map. Numbers on the lower left
hand corner of each X-ray map represents the approximate range of values for each
element in the tourmaline cluster.
Fig. 12. Backscattered electron image and X-ray maps of a complexly zoned, blue
tourmaline (sample C2B-808.2 from San Gregorio). Numbers on the lower left hand
corner of each X-ray map represents the approximate range of values for each element in
the tourmaline cluster. In general, early, Mg-rich tourmalines are overgrown by more
aluminous, Ca-deficient, and slightly more Fe-rich compositions, which is consistent with
the later superposition of sericitic alteration on an earlier igneous (roughly potassic)
assemblage.
Fig. 13. Histograms of δ11B values of tourmaline from Copiapó and other mineralized
locations along with δ11B values of different geological environments. A. Histogram with
the δ11B values of select samples of Copiapó tourmaline. Error bar indicates an
uncertainty of ± 2 per mil. B. Histogram of unpublished boron isotope data of F. Mazdab,
M. Barton, and R. Hervig. This dataset contains boron isotope data from IOCG deposits
(Cloncurry district, Cortez Mountains, El Romeral, Humboldt, Yerington), sodicly altered
rocks (Ajo, Superior-Engels, Granite Mountain), and porphyry-style occurrences (i.e.,
Cananea, Copper Creek, Nacozari de Garcia, Zaaiplaats), as well as miscellaneous
tourmaline occurrences in kyanite ore (Cargo Muchacho-Vitrefax Hill) and sedimentary
rocks (Belt Supergroup, Boyer Ranch). The standard deviation is about ±1.1 per mil. C.
Compilation of δ11B values for different geological environments modified from Palmer
and Swihart (1996). The gray box indicates the range of values covered by Copiapó
tourmaline.
Fig. 14. Mineral phase diagrams showing the topology of magnesiofoitite-dravite and
dravite-uvite solid solution reactions at 400 ºC and 500 bars. These diagrams assume
quartz and water saturation, with tourmaline stable throughout. Al is treated as an
immobile element. Thermodynamic data was acquired using the SUPCRT92 program of
Johnson et al. (1992). A representative reaction between tourmaline end members in the
albite field is presented as an example of the effect of increasing log(K) (i.e., activity
ratios of key tourmaline end members). The blue line represents the topology of pure
end-member reactions between tourmaline end members. The green line represents an
increase in log(K) by one log unit, and the orange line represents a decrease by one log
unit. A. Magnesiofoitite to dravite reaction. This reaction is not dependent on the fugacity
of oxygen. Na content increases to the right and Mg increases to the top. The stability
fields move up and to the right with increasing dravite activity and down and to the left
with increasing magnesiofoitite coincident with increasing acidity. B. Dravite to uvite
reaction. The line on this diagram represents the topology of pure end-member reactions
between dravite and uvite. Log(Ca/H2) is held constant at 2. The stability fields move up
and to the left with increasing dravite activity and down and to the left with increasing
39
uvite activity. Mineral abbreviations: Alb = albite, Dr = dravite, MgF = magnesiofoitite,
Qtz = quartz, Uv = uvite.
Fig. 15. Al-Fe75-Mg75 diagrams after Henry et al. (2008) comparing Copiapó
tourmaline to tourmaline from other hydrothermal systems, both mineralized and
otherwise. Tourmalines from other IOCG, Cu-Mo, and sediment-dominated systems
appear to show similar chemical variations to Copiapó tourmaline. A. Magmatic
hydrothermal systems. References: Au (green): Koval et al. (1991), Golani et al. (2002);
Cu-Mo (purple): Koval et al. (1991), Lynch and Ortega (1997), Frikken (2003), Yavuz et
al. (1999); Pb-Zn-Cu (pink): Yavuz et al. (2008); Sn (blue): Mao (1995); Sn-Cu (red):
London and Manning (1995), Mlynarczyk and Williams-Jones (2006); Sn-W (light blue):
Pirajno and Smithies (1992); W (yellow): Clarke et al. (1989); Hydrothermal breccias
and veins (peach): Dini et al. (2008), Demirel et al. (2009); Yavuz et al. (2008). B.
Tourmaline from IOCG and related systems. Purple: Cavarretta and Puxeddu (1990);
Yellow: Frietsch et al (1997); Orange: Xavier et al. (2008). C. Metamorphic tourmaline
associated with Au-quartz veins. Brown: Garda et al. (2009); Blue: King and Kerrich
(1989). D. Stratabound tourmaline occurrences. Green: Jiang et al. (1995); Red: Jiang et
al. (1997b); Light blue: Mao (1995); Yellow: Plimer (1986); Orange: Plimer and Lees
(1988); Purple: Raith (1988); Pink: Slack and Coad (1989); Blue: Taylor and Slack
(1984). Abbreviations: MSD = massive sulfide deposits (includes both SEDEX and VMS
deposits), SEDEX = sedimentary exhalative, VMS = volcanogenic massive sulfide. E.
Sedimentary (evaporite-related) tourmaline occurrences. Dark red: Ayuso and Brown
(1984). This tourmaline is found in a Fowler talc belt in New York and is unusually Mn
rich. Light blue: Bačík et al. (2008). Tourmalines from this study are reworked
tourmalinites now in conglomerates with carbonates and clastic sedimentary rocks with
subordinate volcanics. Late tourmaline contains ferric iron and is Al-deficient. Purple:
Henry et al. (1999). This tourmaline was found in the cap rock of a salt dome and is
believed to have formed diagenetically within the bedded salt sequence that ultimately
formed diapirs. Red: Henry et al. (2008). These tourmalines are found in meta-evaporite,
non-marine sequences in Namibia and are moderately to highly deficient in Al and
enriched in ferric iron. Green: Jiang et al. (1997a). Tourmalines from this study are found
in meta-evaporite sequences in association with borate deposits. There is evidence for
both non-marine and marine influences on the chemistry of the Houxianyu borate
deposit, China. Blue: Peng and Palmer (2002). Tourmaline is found in meta-evaporite
sequences enclosed by volcanic tuffs. Orange: Žáček et al. (1998). Tourmaline occurs in
the meta-evaporite Locotol Breccia. Along with other silicate minerals, tourmaline
formed along the reaction rim between dikes of highly alkaline volcanic rocks and B-rich
evaporites. F. Copiapó tourmaline. Note how tourmaline from this area covers a wide
range of compositions and displays the same compositional trends as tourmalines from
highly saline environments.
Tables
Table 1. Tourmaline end members after Hawthorne and Henry (1999)
Table 2. Exchange vectors after Henry and Guidotti (1985) and Dutrow and Henry (2000)
Table 3. Tourmaline-bearing mineral assemblages
40
Table 4. Representative tourmaline analyses of Copiapó samples
Table 5. Pleochroic characteristics of and zoning in Copiapó tourmaline
Table 6. Boron isotope results of Copiapó tourmaline
41
Figure 1
Figure 2
A
B
Tour
Tour
Chl
Hem
And
Mt
Qtz
Qtz
100 μm
100 μm
C
D
Qtz
Tour
Mt
Alb
Tour
Bt
CPH
100 μm
E
100 μm
F
Tour
Lim
Tour
Alb
Tour
Qtz
100 μm
G
100 μm
AFS
H
Bt
Alb
Alb
Tour
Act
100 μm
Tour
100 μm
Figure 3
Figure 4A
Figure 4B
Figure 5
Figure 6
Figure 7A
Figure 7B
Figure 7C
Figure 7D
Figure 7E
Figure 7F
Figure 8
Figure 9
Tour
Cal
Mar
Tour
100 μm
Figure 10
Tour
Mt
Tour
Tour
100 μm
Cal
Figure 11
Mg
BSE
20 μm
1.78 – 3.60 wt%
Na
High
Fe
Low
0.94 – 1.55 wt%
Ca
7.78 – 10.84 wt%
Ti
0.41 - 0.85 wt%
0.01 - 0.21 wt%
Figure 12
Al
BSE
High
200 μm
12.79 - 16.64 wt%
Mg
Fe
Low
0.43 – 2.86 wt%
Na
11.60 – 19.05 wt%
Ca
1.02 – 1.63 wt%
0.44 – 1.80 wt%
Figure 13
B
A
marine brines
non-marine brine
seawater
C
marine evaporites
non-marine evaporites
limestones and dolomites
magmatic
fresh island arc volcanics
granite and rhyolite
fresh mantle-derived rocks
-40
-20
0
+20
δ11B‰
+40
+60
Figure 14A
Magnesiofoitite to Dravite
5
400°C, 500 bars
Qtz, H2O saturation
Chlorite
Increasing aDr
+ 2
Pyrophyllite
2+
2
Albite
+
ty
idi
c
a
ing
s
rea
Inc
1
0
1
Paragonite
2
3
4
+
5
6
+
log(Na /H )
Figure 14B
Dravite to Uvite
6
400°C, 500 bars
Qtz, H2O saturation
Chlorite
5
4
2+
+ 2
lo g [M g /(H ) )]
O
+
H2
H
+2
+4
tz
lb
+ A + + 3Q
2
Dr
g
+M
Increasing aMgF
Increasing log(K)
Na
+2
3
F
Mg
lo g [M g /(H ) )]
4
Paragonite
3
Albite
Increasing aDr
Pyrophyllite
Dr + Ca2+ + Mg2+ + 2H2O + 3Qtz
2
Uv + Alb + 4H+
ty
idi
c
a
ing
s
rea
Inc
1
Increasing aUv
Increasing Ca
Increasing log(K)
0
1
2
3
4
log(Na+/H+)
5
6
Figure 15A. Magmatic hydrothermal tourmaline
Figure 15B. IOCG and related systems
Figure 15C. Metamorphic hydrothermal tourmaline
Figure 15D. Stratabound tourmaline
Figure 15E. Sedimentary (evaporite-related) tourmaline
Figure 15F. Copiapó tourmaline
Table 1. Tourmaline end members and classifications from Hawthorne and Henry (1999).*
Alkali tourmaline
(Y3)
(Z6)
T6O18 (BO3)3 V3
Species
(X)
W
Olenite
Na Li1.5 Al1.5
Al3
Na
Dravite
Na
Mg3
Al6
Chromdravite
Na
Mg3
Cr6
Na
2+
Fe
3
Al6
Si6O18 (BO3)3 (OH)3 (OH)
Si6O18 (BO3)3 (OH)3 (OH)
Buergerite
Na
Fe
3
Al6
Si6O18 (BO3)3
Povondraite
Vanadiumdravite
Na
Fe3+3
Mg3
Elbaite
Schorl
+
3+
Al6
Al6
Si6O18 (BO3)3 (OH)3 (OH)
Si6O18 (BO3)3 O3 (OH)
Si6O18 (BO3)3 (OH)3 (OH)
O3
F
(X)
Fe3+4Mg2 Si6O18 (BO3)3 (OH)3 O
V6
Si6O18 (BO3)3 (OH)3 (OH)
Calcic tourmaline
(Z6)
T6O18 (BO3)3 V3
(Y3)
W
Liddicoatite
Ca
Li2Al
Al6
Si6O18 (BO3)3 (OH)3
F
Uvite
Feruvite
Ca
Mg3
MgAl5
Si6O18 (BO3)3 (OH)3
F
MgAl5 Si6O18 (BO3)3 (OH)3
Ca
Fe2+3
X-site vacant tourmaline
(Y3)
(Z6)
T6O18 (BO3)3 V3
(X)
F
Species
Species
Rossmanite
Na
□
□
□
LiAl2
Al6
Al6
Fe2+2Al
Foitite
Magnesiofoitite
Mg2Al
Al6
*Hypothetical end members are excluded.
+
Most common end member
W
Si6O18 (BO3)3 (OH)3 (OH)
Si6O18 (BO3)3 (OH)3 (OH)
Si6O18 (BO3)3 (OH)3 (OH)
Table 2. Common substitutions within and between sites including a compilation of exchange vectors
after Henry and Guidotti (1985) and Henry and Dutrow (1996).
Substitutions*
Exchange vectors
Y
Mg = YFe2+
Fe2+Mg-1
Y
Mn = YFe2+
Fe2+Mn-1
Z
Al = ZFe3+
Fe3+Al-1
CrAl-1
Z
Al = ZCr3+
OH- = O(1)F-
O(1)
F(OH)-1
2YFe2+ = YLi + YAl
LiAlFe2+-1
elbaite substitution
X
Na + 2YMg = X□** + YAl
□AlNa-1Mg-1
alkali-defect substitution
X
Na + YMg + O(1)OH- = X□ + 2YAl + O(1)O2-
□Al2ONa-1Mg-2(OH)-1
aluminobuergerite substitution
Y
Mg + O(3)OH- = YAl + O(3)O2-
AlOMg-1(OH)-1
Fe2+ + O(3)OH- = YFe3+ + O(3)O2-
Fe3+OFe2+-1(OH)-1
Y
buergerite substitution
Y
Mg + TSi = YAl + TAl
Al2Mg-1Si-1
Tshermaks substitution
2YAl = YMg + YTi
MgTiAl-1
Na + YAl = XCa + YMg
X
CaMgNa-1Al-1
uvite substitution
X
□ + YAl + O(1)OH- = XCa + YMg + O(1)O2Y
Z
O(1)
-
Y
Z
O(1)
CaMgO(OH)-1□-1Al-1(OH)-1
2-
CaMgO(OH)-1□-1Al-1(OH)-1
2 Mg + Al +
OH = 2 Al + Mg + O
*Superscripts denote specific crystallographic sites.
**This symbol represents an X-site vacancy
Table 3. Mineral assemblages in tourmaline-bearing samples from Copiapó, Chile
Sample no.
Cerro Bronce_Estrella
C2B-298
C2B-708
Mineral assemblage, textures, and relative timing*
Ep-Tour-Tit veins; Hbl[mafics]**, Act[Hbl] in
envelope of Ep veins; Tit[Hbl] and some Mt (50% or so
alt to Hem) are present throughout the rock; The host
rock is comprised of Plag and Pyx
Large sprays of Tour in rock with Cc-pale green SerHem-Ep and an unknown brown phase
Cerro Buitre Radio Tower
C2B-287
C2B-576c
C2J-124
C2J-334
Cerro Granate
Plag with a cataclastic texture dominates this section;
Veins of cryptocrystalline, fine grained Qtz are present
througout and cement specular Hem in some cases;
Lim[Py]; Tour is clotty, comprises a few percent of the
rock, and is most abundant where Hem is not present;
Rare Apat is also present.
Abundant green Bt and Musc; Hem(specular)-Bt veins
cut a granular Qtz vein that contains Cpy; Other veins
dominated by Bt; One such vein contains accessory
Tour; Bt is stable adjacent to crystals (no obvious
chloritization of Bt); Evidence for specular Hem after
Mushk
Mainly intergrown Plag (variably sericitized)-Qtz going
to Qtz-Tour-Hem zones; Early blue-grey Tour is
rimmed by brown Tour (majority) with later light blue
Tour; Hem and Tour do not typically occur together, but
both occur with Qtz; coarse-grained Zircon is also
present
Sparsely porphyritic "adamellite" with >3 mm Plag,
sparse Opx and Cpx now almost completely converted
to pale sheaves of Act, locally with Bt and rarely with
blue to pink Tour(± Lim); Mt and Ilm are common
(Mt>Ilm); Mt typically has Hem and both typically have
Ilm rims; late Qtz is widespread but sparse and Apat is
common
C3B-072a
Tour vein with sparse Cc and late REE mineral veinlet
grading to Tour with some Qtz locally intergrown with
specular Hem; Vein envelope is Plag with sparse Rut
and Hem; Along one edge of sample, there appears to
be a Chl-Ser-Cc-oxide veinlet; The host rock is an
equigranular fine grained Plag-dominant rock with
distributed Ser-Chl, and minor Rut
Cerro Negro Norte
C6B-076
Coarse-grained Tour + Kfs + Cc + sulfides(Py>Cpy) +
Chl ± Tit vein cuts inclusion-rich (mainly Mt) finegrained Tour vein in rock that has sericitized Plag + Act
± Ep at one end and variable Act-Ep to Mt[Hem]-rich
material in towards the other end; Act-Plag veinlets cut
matrix and are cut by other Kfs veinlets
C3B-381a
Penetratively deformed rock with Qtz-Tourm veins
grading outward into Tour-Alb ± bright yellow Fesulfate; Plag-rich zones have strong alignment of
feldspars; Within the principal veins, there are two
generations of Tour, one granular and deformed and the
other coarser, undeformed generation intergrown with
non-strained, non-oriented Qtz; Opaque minerals appear
to be mainly Lim and minor Rut
Española
Falla Ojancos_Transito San Francisco
Jesus Maria
C6B-101b
Bands of brown Tour in Plag(albite)-rich rock are cut
by coarse-grained Alb veins; Sparse Kfs is also present;
Lighter colored part of rock has Lim[Py] and minor Mt
as well as a sparse, unknown brown mineral (goethite?)
C6B-107
Host is varied very fine-grained, felsic granular rock
with a brecciated zone containing clasts with altered
Plag phenocrysts; This is cut by Qtz(±Tour
±Lim[sulfide]) vein; Qtz veins are clearly broken and
transported in the breccia; Breccia matrix consists of
very fine-grained, dark green-grey Tour intergrown with
Qtz
C7B-003a
Tour-Dum bearing rock with a groundmass of abundant
equigranular Qtz-Cc-Hem[Mt]; Certain areas of the
rock also contain Pyroph; Late Tour forms comb-like
overgrowths on embayed or euhedral edges of early
Tour; Dum is present throughout the rock but are
concentrated in areas where they appear to have
replaced earlier grains
C3B-429.5
Tour-clay-Lim[Py] vein cuts a Plag dominated rock
with an overall clastic/cataclastic texture; minor
specular Hem and Lim[Py] in the matrix
Ojancos Viejo
San Gregorio_S Granate
C2B-352e
C2B-655
C2B-671
C2B-808.2
Santos_PdC
Qtz-rich aplite, with variable textures but constant
proportions of minerals is cut by a prominent Tour that
contains an abundance of relatively unaltered Plag, Kfs,
and Qtz with minor Apat; These phases all seem to have
grown together; Outside of vein is weakly perthitic alk
Fsp, with an abundance of Plag dusted with white
micas, some Hem(Mt), and big grains of Ilm
Abundant nearly jet black, opaque Tour overgrown by
multi-colored, zoned Tour; Some Tour clearly replaces
associated Act in rock; Bt, Ep, Plag, Tit, and Qtz are
also present; Late Cc veinlet runs through the section
Brown Tour vein with network-filling envelope with
Albite>Act-yellow Tit adjacent to Ep-Act(Tit-Mt-ApatCpx) altered San Gregorio monzodiorite
Brown Bt and Act[Opx]; Significant amounts of Plag
and Qtz (some myrmekitic textures); Zircons are
present as inclusions in Bt with radiation damage; Tour
occurs in cavities where it is partially replaced by
potassic-chlorohastingsite or intergrown with Bt and
Tit; Oxides dominated by Mt with some Hem overprint
DDH289-037.5
Tour-Bt-Py-Qtz(-Mt-Mushk-Apat-Albite) vein and
breccia cement is present along contact of crystal-rich
and crystal-poor rock types; Qtz contains Hem and local
Tour and appears to fill open space; The crystal-poor
rock has Plag, Qtz (vug fill, rare veinlets), and a very
fine-grained groundmass with feldspar; The crystal-rich
rock contains Plag, Chl, and Fe oxide, but crystal
content decreases by 1/2 approaching vein contact; Thin
Qtz veins contain rare Hem ± Chl ± Bt; This rock
contains abundant, scattered Bt with rare Chl[Bt].
DDH291-188.4
Green, intensely biotitized mafic(?) porphyritic rock
with mafic(?) sites now completely converted to green
Bt as is the groundmass; Equant sites with Qtz-Ep-Bt
may have been feldspar phenocrysts; Multiple veins cut
the rock: two late vein types include Chl-Bt(-Ep-Qtz-PyCpy ± Tour) with an envelope of Bt-Tour-Qtz and a QtzTour ± Bt ± Mt vein; These both cut coarse-grained BtEp-Qtz(-Cpy) veinlets that have remarkably little
deformation even though the cross-cutting Qtz veinlet is
clearly deformed; sulfides are restricted to the veins
DDH384-004.2
DDH628-094.2
Tour vein is intergrown with well-formed Plag and
surrounded by sericitized Kfs and Chl; Blades of
specular Hem irregularly line the sides of the vein;
Yellow Ep is also present, but rare; Cc is found in
variable quantities throughout the vein; There seem to
be Cc-replaced grains within the vein with some
evidence of flow or deformation
Composite Mushk-Anhy-Qtz-Cpy-Py-Tour vein in
complex biotitized porphyritic host; The central part of
the vein contains Anhy(-Cpy-Py) grading into and outer
zone of Mushk-Qtz(-Cpy-Tour) where Tour occurs both
as isolated small crystals and sprays of very fine-grained
fibers growing off Mushk; The host is Bt-rich, but rock
contains multiple events with Ep-Mt-Cpy-Qtz-Chl in
addition to fine-grained Bt
DDH628-150.6
DDH628-626.3
DDH643-595.5
DDH684-079.8
Intensely biotitized porphyritic volcanic rock cut by
Tour-Py-Cpy-Mt[Cpy]-Allan-Chl-Bt-Kfs vein;
Abundant Mt is found away from central vein and
disappears approaching it; In the inner envelope Qtz
replaces most minerals and Allan is locally present; The
host rock contains a thin Qtz-Bt(-Cpy-Ep) veinlet that is
truncated by the large vein; Late Cc veinlet cuts the
large vein
Large Scap-Bt(-Chl-Py) vein lacking preferred
orientation of Scap, has apparent Bt-Mt(trace AllanTour) envelope grading out into less Bt- (and Mt-) rich
material; The large vein apparently cuts small veins
with Qtz-Apat-Bt-Mt and minor Tour; Tour also occurs
in bioititized grains; Py crystals are ragged and have
spotted margins in places with abundant tiny inclusions
of Cpy and silicates; Mt locally contains Cpy in vein;
Qtz and Apat occur along edges of Scap vein
Composite Qtz-Allan-Tour-Mt/Mushk-Cpy-Kfs breccia
zone with many shard-like clasts cutting through
biotitized porphyritic rock with feldspar phenocrysts
partly altered to Bt, but mainly secondary Albite ± Qtz;
Fine-grained Mt + rare Rut in original oxide sites;
These grade into Kfs-altered zone/vein toward margin
of breccia with less Mt and sparse very fine-grained
Chl; Clasts appear to be mixed and cut by Qtz-AllanTour-Mt veins; The clasts in the Qtz vein are
combinations of Allan-Qtz-Chl-Tour with various Tour
or Allan rims, sugary or recrystallized Qtz zones, and
accessory Mt, all cemented by several generations of
Qtz-Allan(Epid)-Tour-Mt-Mushk-Cpy
Very fine-grained and dark zone of Qtz-Tour with mafic
free Qtz-Plag envelope and a rim of Mt(partly Mushk)Cpy; The host is biotitized subequigranular rock with
abundant fine-grained Qtz and Plag; Certain areas very
fine-grained aggregates Bt in mafic sites; similar Bt
(rarely Chl) occurs along veins with Cpy-Mushk and
early Py; The veins have Kfs + Qtz ± Bt (or Chl) in
addition to Mushk[Py]
ME013-538
Bt-Tour-rich vein with later Ep + Py (+ Sph-Cpy) in Btrich altered porphyritic volcanic rock with scattered Py
and Sph(Cpy) + Ep + Qtz + Plag; Sph is abundant as
small grains, feldspar sites, veins, and vugs; Two
different colors of Bt correspond to differences in color
in the rocks: pale green and deep red brown
C6B-160b
Sutured Qtz-And-Hem-Rut rock with minor fibrous
blue Tour, trace Lazulite and minor brownish finegrained sheet silicate that appears to be late; Rock is cut
by veinlet of Hem-And-Tour ± Qtz with large, poikilitic
And crystals overgrowing Hem
Vinita Azul
*Mineral abbreviations: Act = actinolite, And = andalusite, Anhy = anhydrite, Apat = apatite, Bt =
biotite, Cc = calcite, Cpy = chalcopyrite, Ep = epidote, Hem = hematite, Kfs = K-feldspar, Lim =
limonite, Mt = magnetite, Mushk = mushketovite, Plag = plagioclase, Py = pyrite, Pyx = pyroxene,
Qtz = quartz, Rut = rutile, Sph = sphalerite, Tit = titanite, Tour = tourmaline
**Minerals or phases in brackets represent minerals that are being replaced.
Table 4. Representative chemical analyses of tourmalines from Copiapó, Chile1
Location
Sample no.
Spot no.
Analysis no.
SiO2
TiO2
Al2O3
B 2 O3 †
Cr2O3
Fe2O3**
FeO
MgO
MnO
CaO
Na2O
K2 O
H2O**
F
Cl
Subtotal
O = F, Cl
Total
Cerro Bronce Estrella
C2B-298
C2B-708
2
2
t5
t1
35.62
35.83
2.35
0.00
23.79
32.20
10.26
0.01
5.18
7.04
8.94
0.00
2.99
1.32
0.02
2.96
0.09
0.00
100.57
-0.04
100.54
10.49
0.00
4.47
6.06
5.55
0.01
0.83
2.24
0.02
2.93
0.03
0.01
100.68
-0.01
100.66
C2B-287
1
t20
37.13
3.83
29.29
Cerro Buitre Radio Tower
C2B-576c
C2J-124
2
1
t2
t5
36.13
36.42
0.46
0.04
31.85
34.63
10.73
0.01
0.31
0.22
11.61
0.00
1.54
2.12
0.03
2.73
0.34
0.00
100.34
-0.14
100.19
Atomic proportions based on 15 cations (T+Y+Z = 15) ‡
III
B
3.00
3.00
3.00
T
Si
6.03
5.94
6.02
B
0.00
0.00
0.00
Al
0.00
0.06
0.00
Sum
6.03
6.00
6.02
Z
C2J-334
1
t1
35.90
0.42
28.13
Cerro Granate
C3B-072a
2
t4
35.34
0.22
28.66
Cerro Negro Norte
C6B-076
4
t12
34.58
1.82
22.82
Española
C3B-381a
2
t3a
36.30
1.79
32.72
10.46
0.00
2.07
6.26
6.34
0.01
0.94
1.72
0.05
3.12
0.04
0.00
99.44
-0.02
99.42
10.77
0.00
2.01
2.24
8.18
0.05
0.28
1.80
0.01
3.44
0.03
0.06
100.06
-0.02
100.04
10.43
0.00
4.51
7.69
7.14
0.06
2.03
1.65
0.04
3.13
0.12
0.01
101.40
-0.05
101.34
10.24
0.00
7.53
8.66
4.15
0.03
0.95
2.15
0.03
2.82
0.01
0.01
100.80
-0.01
100.80
10.05
0.00
5.12
11.21
7.11
0.01
2.21
1.64
0.06
3.29
0.12
0.02
100.18
-0.05
100.12
10.66
0.02
0.71
3.48
8.19
0.04
0.75
2.29
0.09
3.00
0.12
0.02
100.34
-0.05
100.29
3.00
3.00
3.00
3.00
3.00
3.00
6.00
0.00
0.00
6.00
5.88
0.00
0.12
6.00
5.98
0.00
0.02
6.00
6.00
0.00
0.00
6.00
5.98
0.00
0.02
6.00
5.92
0.00
0.08
6.00
Cr
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
3+
Fe
Mg
Al
Sum
0.66
0.59
4.75
6.00
0.56
0.00
5.44
6.00
0.04
0.32
5.59
6.00
0.26
0.00
5.74
6.00
0.24
0.00
5.74
6.00
0.57
0.00
5.42
6.00
0.96
0.00
5.04
6.00
0.67
0.69
4.63
6.00
0.09
0.00
5.89
6.00
Al
Mg
0.00
1.67
0.79
1.37
0.00
2.49
0.50
1.57
0.72
1.97
0.09
1.77
0.69
1.05
0.00
1.14
0.31
1.99
Fe2+
Ti
Sum
1.00
0.30
2.97
0.84
0.00
3.00
0.03
0.47
2.99
0.87
0.06
2.99
0.30
0.00
2.99
1.07
0.05
2.99
1.23
0.03
2.99
1.62
0.24
3.00
0.47
0.22
2.99
Na
K
Ca
□
Sum
0.43
0.01
0.54
0.02
1.00
0.72
0.01
0.15
0.13
1.00
0.67
0.01
0.27
0.06
1.00
0.56
0.01
0.17
0.27
1.00
0.56
0.00
0.05
0.39
1.00
0.53
0.01
0.36
0.10
1.00
0.71
0.01
0.17
0.11
1.00
0.55
0.01
0.41
0.03
1.00
0.72
0.02
0.13
0.13
1.00
F
Cl
OH
O
Total
0.05
0.00
2.79
1.16
4.00
0.02
0.00
2.77
1.22
4.00
0.17
0.00
2.58
1.24
4.00
0.02
0.00
2.95
1.04
4.00
0.01
0.02
3.25
0.72
4.00
0.06
0.00
2.96
0.98
4
0.01
0.00
2.66
1.33
4.00
0.07
0.00
3.11
0.82
4.00
0.06
0.01
2.84
1.10
4.00
Fe2+/Fetotal***
0.6
0.6
0.45
0.77
0.55
0.65
0.56
0.7
0.84
Y
X
OH
1
Electron microprobe analyses were carried out on a CAMECA SX50 at an accelerating voltage of 20 kV, 30 nA beam current,
and 10 – 15 second counting time for major elements and 200 nA beam current with a 30 – 60 second counting time for minor elements.
*Santos sample numbers correspond to the drill hole number followed by the depth in meters
**H2O values were chosen to reflect an approximate Fe3+/Fetotal ratio that was derived via electron microprobe Fe working curves after
Fialin et al. (2004). See Appendix for further discussion.
***Fe ratio determined from electron microprobe working curves after Fialin et al. (2004). See Appendix for further discussion.
†
Calculated on the basis of 3 apfu B
‡
Site assignments are empirical estimates as structural refinement was not part of this study
Falla Ojanco Transito San Francisco
C6B-101b
C6B-107
1
2
t5
t9
36.14
37.59
3.00
0.38
25.92
31.94
Jesus Maria
C7B-003a
3
t2
36.45
0.15
36.33
Ojancos Viejo
C3B-429.5
1
t19
36.33
0.60
30.74
C2B-352e
3
t12
34.47
1.45
24.76
San Gregorio S Granate
C2B-655
C2B-671
2
2
t1
t2
34.51
35.32
2.30
1.47
22.50
25.05
C2B-808.2
1
t20
34.70
0.03
25.78
DDH289-037.5
2
t14
36.86
0.28
34.16
10.40
0.15
3.29
5.34
9.22
0.00
0.83
2.45
0.03
3.13
0.07
0.00
99.98
-0.03
99.95
10.79
0.01
1.29
4.97
8.31
0.00
0.92
2.33
0.01
3.25
0.05
0.00
101.98
-0.02
101.96
10.71
0.02
3.31
7.39
2.94
0.00
0.02
0.85
0.05
3.07
0.32
0.04
101.63
-0.14
101.49
10.50
0.00
2.51
6.00
7.05
0.00
0.80
2.25
0.02
3.07
0.01
0.00
100.30
0.00
100.30
9.99
0.00
7.65
9.34
5.28
0.01
1.94
1.69
0.04
2.73
0.13
0.01
99.59
-0.06
99.53
9.99
0.01
8.56
8.71
6.45
0.08
3.09
1.20
0.05
2.57
0.17
0.00
100.19
-0.07
100.12
10.23
0.00
6.41
7.09
7.71
0.06
3.22
1.17
0.05
2.78
0.10
0.01
100.67
-0.04
100.62
9.99
0.01
14.26
8.30
2.22
0.08
1.08
1.88
0.18
2.28
0.05
0.04
100.92
-0.03
100.89
10.72
0.01
1.34
3.75
7.35
0.03
0.67
2.28
0.00
3.05
0.02
0.00
100.68
-0.01
100.67
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
6.04
0.00
0.00
6.04
6.05
0.00
0.00
6.05
5.91
0.00
0.09
6.00
6.01
0.00
0.00
6.01
5.99
0.00
0.01
6.00
6.01
0.00
0.00
6.01
6.00
0.00
0.00
6.00
6.04
0.00
0.00
6.04
5.97
0.00
0.03
6.00
0.02
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.41
0.46
5.11
6.00
0.16
0.00
5.83
6.00
0.40
0.00
5.59
6.00
0.31
0.00
5.65
6.00
1.00
0.00
4.99
6.00
1.12
0.26
4.62
6.00
0.82
0.16
5.02
6.00
1.87
0.00
4.13
6.00
0.16
0.00
5.82
6.00
0.00
1.84
0.23
2.00
1.27
0.71
0.34
1.74
0.08
1.37
0.00
1.41
0.00
1.79
1.16
0.58
0.68
1.77
0.75
0.38
2.96
0.67
0.05
2.95
1.00
0.02
3.00
0.83
0.07
3.01
1.36
0.19
3.00
1.27
0.30
2.98
1.01
0.19
2.99
1.21
0.00
2.95
0.51
0.03
3.01
0.79
0.01
0.15
0.05
1.00
0.73
0.00
0.16
0.11
1.00
0.27
0.01
0.00
0.72
1.00
0.72
0.01
0.14
0.13
1.00
0.57
0.01
0.36
0.06
1.00
0.40
0.01
0.58
0.01
1.00
0.39
0.01
0.59
0.02
1.00
0.63
0.04
0.20
0.13
1.00
0.72
0.00
0.12
0.17
1.00
0.04
0.00
2.95
1.01
4.00
0.03
0.00
3.06
0.91
4.00
0.16
0.01
2.90
0.93
4.00
0.01
0.00
2.90
1.10
4.00
0.07
0.00
2.58
1.35
4.00
0.09
0.00
2.43
1.48
4.00
0.05
0.00
2.62
1.32
4.00
0.03
0.01
2.15
1.81
4.00
0.01
0.00
2.87
1.12
4.00
0.64
0.81
0.71
0.72
0.57
0.53
0.55
0.39
0.75
Santos PdC*
DDH628-094.2 DDH628-151.6
1
2
t2
t1
35.98
35.60
0.80
0.07
26.91
29.91
DDH628-626.3
2
t6
35.26
0.04
35.00
DDH643-595.5
2
t2
36.37
0.52
30.46
DDH684-079.8
3
t3
36.36
0.39
29.29
ME013-538
1
t3
36.18
0.67
31.95
Vinita Azul
C6B-160b
1
t2
35.90
0.22
36.40
10.29
0.01
4.64
8.90
4.64
0.04
0.28
2.24
0.05
3.15
0.03
0.00
99.84
-0.01
99.83
10.52
0.01
4.92
7.89
2.63
0.04
1.02
1.25
0.03
2.82
0.02
0.09
101.54
-0.03
101.52
10.49
0.00
3.60
6.91
6.28
0.00
1.08
2.10
0.01
3.01
0.05
0.00
100.88
-0.02
100.86
10.48
0.01
1.40
9.45
6.93
0.03
0.88
2.10
0.03
3.56
0.03
0.01
100.94
-0.02
100.92
10.65
0.01
0.00
10.70
5.17
0.00
1.16
1.56
0.07
3.39
0.01
0.01
101.55
-0.01
101.54
10.76
0.02
2.00
4.67
5.63
0.03
0.03
1.90
0.01
3.27
0.07
0.01
100.97
-0.03
100.94
3.00
3.00
3.00
3.00
3.00
3.00
3.00
6.01
0.00
0.00
6.01
6.01
0.00
0.00
6.01
5.82
0.00
0.17
6.00
6.03
0.00
0.00
6.03
6.03
0.00
0.00
6.03
5.96
0.03
0.01
6.00
5.80
0.00
0.20
6.00
DDH291-188.4
1
t1
36.37
0.28
30.08
DDH384-004.2
2
t3
36.69
0.38
31.50
10.46
0.07
2.57
7.85
6.50
0.01
1.05
2.05
0.06
3.21
0.04
0.00
100.61
-0.02
100.59
10.56
0.01
2.02
6.59
6.73
0.01
0.73
2.05
0.02
3.20
0.09
0.01
100.60
-0.04
100.56
10.41
0.00
5.35
8.67
6.88
0.03
1.61
1.90
0.06
3.22
0.05
0.01
101.88
-0.02
101.85
3.00
3.00
6.04
0.00
0.00
6.04
6.04
0.00
0.00
6.04
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.32
0.00
5.67
6.00
0.25
0.00
5.75
6.00
0.67
0.03
5.29
6.00
0.59
0.00
5.41
6.00
0.61
0.00
5.39
6.00
0.45
0.00
5.55
6.00
0.17
0.10
5.72
6.00
0.00
0.00
6.00
6.00
0.24
0.00
5.75
6.00
0.22
1.61
0.36
1.65
0.00
1.68
0.55
1.17
1.25
0.65
0.40
1.55
0.00
1.61
0.20
1.27
0.98
1.36
1.09
0.04
2.96
0.91
0.05
2.96
1.21
0.10
2.99
1.26
0.01
2.98
1.09
0.01
3.00
0.96
0.06
2.97
1.31
0.05
2.97
1.48
0.08
3.03
0.63
0.03
3.00
0.66
0.01
0.19
0.14
1.00
0.65
0.01
0.13
0.21
1.00
0.62
0.01
0.29
0.08
1.00
0.73
0.01
0.05
0.21
1.00
0.40
0.01
0.18
0.41
1.00
0.68
0.00
0.19
0.13
1.00
0.68
0.01
0.16
0.16
1.00
0.50
0.02
0.21
0.28
1.00
0.59
0.00
0.01
0.40
1.00
0.02
0.00
3.03
0.95
4.00
0.05
0.00
3.02
0.93
4.00
0.03
0.00
3.04
0.93
4.00
0.02
0.00
2.97
1.01
4.00
0.01
0.02
2.66
1.30
4.00
0.03
0.00
2.85
1.13
4.00
0.02
0.00
3.36
0.62
4.00
0.01
0.00
3.20
0.79
4.00
0.04
0.00
3.09
0.87
4.00
0.77
0.78
0.64
0.68
0.64
0.68
0.67
0.67
0.72
Table 5. Pleochroic characteristics of and zoning in Copiapó tourmaline
Locality
Sample
Color parallel to c
Color perpendicular to c
Zoning?
Cerro Bronce Estrella
C2B-298
C2B-708
tan; blue
tan
brown; dark blue-brown
dark sky blue
Y (on second)
N
brown (core); blue-green to bluelight tan (core); light blue (rim)
brown (rim)
tan
light blue
lavender; light tan; light greenish brown
gray; brown; green-brown
pink; light blue
dark brown; blue-brown
Cerro Buitre Radio Tower
C2B-287
C2B-576c
C2J-124
C2J-334
Cerro Granate
C3B-072a
light tan
blue-green; blue-brown
Y
Cerro Negro Norte
C6B-076
tan/pink; light blue
brown; blue-green
Y
Española
C3B-381a
light blue-green (core); light brown
(rim); tan (late)
blue-green (core); brown (rim);
blue-green (late)
Y
Falla Ojancos TransitoSan Francisco
C6B-101b
C6B-107
light brown
tan
dark brown
brown?
Y
Y
Jesus Maria
Ojancos Viejo
C7B-003a
C3B-429.5
blue-brown (core); blue-brown
light blue-brown (core); light bluish (rim); dark blue-green (core); light
brown (rim); tan (core); whitish(rim)
blue-green (rim)
light blue-green (core); light brown
(rim)
blue-green/blue-brown (core);
brown (rim)
Y
N
N
Y
Y
Y
San Gregorio_S Granate
C2B-352e
C2B-655
C2B-671
C2B-808.2
light brown
tan; light yellow-green
light brown
blue; brown
dark brown
brown; blue-green
v. dark brown
dark blue; v. dark brown
N
Y
N
Y
Santos_PdC
DDH289-037.5
DDH291-188.4
DDH384-004.2
DDH628-094.2
DDH628-150.6
DDH628-626.3
DDH643-595.5
DDH684-079.8
ME013-538
tan
tan
tan
tan
tan
tan
tan; blue-dark blue (non-pleochroic)
tan
tan
blue-green/blue-brown/brown
blue-green
blue-green/blue-brown
blue/blue-brown
dark blue; dark brown
blue/blue-green
blue green
brown?
blue-green
Y
Y
Y
Y
Y
Y
Y
Y
C6B-160b
tan
blue
Y
Vinita Azul
Table 6. Boron isotope analyses of tourmalines from the Copiapó area and Cerro Negro Norte*
Locality
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Granate
Cerro Granate
Cerro Granate
Cerro Granate
Cerro Granate
Espanola
Espanola
Espanola
Espanola
Espanola
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Sample
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-671
C2B-671
C2B-671
C2B-671
C2B-671
C2B-671
C2B-671
C2B-708
C2B-708
C2B-708
C2B-708
C2B-708
C2B-708
C3B-072a
C3B-072a
C3B-072a
C3B-072a
C3B-072a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
Spot no.
1A
1B
1C
3A
3B
1A
1B
1C
1D
2A
2B
2C
1A
1B
1C
1D
1E
1F
1A
1B
1C
1D
1E
1A
1B
1C
1D
1E
1A
1B
1C
1D
1E
1F
1G
δ11B
Morphology
vein
4.2
vein
2.0
vein
2.9
vein
2.8
vein
0.0
vein and fracture-fill -1.3
vein and fracture-fill -2.6
vein and fracture-fill -5.5
vein and fracture-fill -2.9
vein and fracture-fill -2.8
vein and fracture-fill -4.7
vein and fracture-fill -5.2
vein
-3.2
vein
-4.9
vein
-3.6
vein
-1.2
vein
-3.1
vein
-3.7
vein
-1.4
vein
-3.7
vein
-3.7
vein
-4.7
vein
-5.1
tourmalinized rock -5.9
tourmalinized rock -6.9
tourmalinized rock -7.4
tourmalinized rock -7.2
tourmalinized rock -6.7
vein
-5.9
vein
-7.1
vein
-7.5
vein
-6.6
vein
-5.5
vein
-4.8
vein
-5.0
2s
0.6
0.6
0.7
0.7
0.6
0.6
0.5
0.6
0.6
0.6
0.7
0.7
0.5
0.5
0.5
0.5
0.5
0.6
0.5
0.5
0.4
0.4
0.6
0.7
0.7
0.9
0.9
0.7
0.5
0.5
0.6
0.4
0.4
0.6
0.5
*Analyses were done on a MC-LA-ICPMS (wet plasma) at a 8 Hz laser pulse rate, 75 μm spot
size, 30 sec on-peak background measurement, followed by 80 cycles of one-second integration
time per cycle
Appendices
Appendix 1: Analytical Methods
Major- and minor-element analyses: Major-element analyses for tourmaline were
performed on 27 polished thin sections on a CAMECA SX50 at the University of
Arizona. Back-scattered electron imaging confirmed the complexity of elemental
zonation and provided the basis for the selection of microprobe data points. Two different
operating conditions were used for major and minor elements in tourmaline, respectively.
For the major elements, an accelerating voltage of 20 kV, 30 nA beam current, and 10 –
15 second counting time were used. For minor elements, a 20 kV accelerating voltage,
200 nA beam current, and a 30 – 60 second counting time were employed. Standards
used are diopside (Si, Mg, Ca), anorthite (Al), fayalite (Fe), albite (Na), K-feldspar (K),
rhodonite (Mn), rutile (Ti), MgF 2 (F), scapolite (Cl), and chromite (Cr). A PAP
correction was applied to the data (Pouchou and Pichoir, 1984). Table A1 contains all
tourmaline analyses from this study.
Even though it is possible to analytically determine most of the major elements in
tourmaline by electron microprobe, B, Li, H, and the valence states of the transition
elements cannot be directly measured. In the absence of accurate analyses of these
elements and transition element oxidation states, several assumptions were made in order
to calculate the stoichiometry of tourmaline. First, B is assumed to be stoichiometric at 3
apfu. Although natural samples exhibit variation from 2.86 to 3.26 apfu (Dyar et al.,
1998; Hughes et al., 2001), the majority of spectroscopic and structural refinement
studies suggest that B is stoichiometric (e.g., Grice and Ercit, 1993; Hawthorne, 1996;
Bloodaxe et al., 1999; Clark, 2007).
Due to the fine-grained nature of the tourmaline and its complex relationship with
other minerals, Mossbauer spectroscopy on tourmaline samples was not feasible.
Therefore, Fe3+/∑Fe ratios were estimated for Copiapó area tourmalines using methods
outlined by Fialin et al. (2004). This procedure uses the self-absorption-induced shift in
the FeLα peak caused by unfilled 3d states to determine the relative amounts of Fe3+ to
total Fe. Other than the oxidation state, the peak shift is also dependent on the total Fe
concentration, as higher Fe contents result in self-adsorption effects. These measurements
were carried out on polished thin sections at 20 kV and 299 nA. 70 peak searches with a
dwell time of 200ms were carried out per spot. To prevent any discrepancies due to
mechanical drift throughout the run, each measurement was corrected to the FeLα
position for hematite. Significantly, the FeLα peak appears to be insensitive to the
geometry of the Fe sites for pure Fe valence end members. The calibration curves
obtained hold for the majority of tourmaline samples. However, several dravitic and
uvitic tourmalines, as well as some other minerals (i.e., clinozoisite) with Fe contents less
than 10 atomic wt percent, plot above the Fe2+ calibration curve, representing peak
positions that are not consistent with their Fe concentrations. This could be due to Fe
oxidation at the analyzed spot or intervalence charge transfer, which is particularly
noticeable when Fe2+ and Fe3+ sites have similar geometries (Fialin et al., 2004).
Tourmalines for which the Fe ratio could be derived were normalized to reflect that ratio.
These ratios were related to the overall Fe content of these tourmalines to derive a
formula that was then applied to the remainder of the tourmaline to acquire an
approximate Fe3+/∑Fe ratio (Fig. A1). The fact that tourmalines from the Copiapó area
appear to fit well to this trend may reflect a geologic control on tourmaline compositions.
However, the real Fe3+ value may be higher or lower, in light of the chemical
heterogeneity present in each sample (Table A2).
To meet charge balance constraints, enough H was added to make the Fe3+/Fe tot ratio
equivalent to the estimated value for tourmalines from each sample. This H estimate,
which also affects the estimate of W-site O2-, is subject to great uncertainty because it
contains the errors associated with normalization assumptions and elemental analytical
uncertainties (Dutrow and Henry, 2000). Tourmaline with greater than 0.2 apfu Mg has
negligible concentrations of Li (Henry and Dutrow, 1996). The antipathetic nature of Li
and Mg is interpreted as the result of a chemical response to the size-adjusting
requirements of the edge-sharing Y and Z octahedra. The oxidation or reduction of Fe
changes the cation radius at the Y-or Z-sites, such that a structural fit is best achieved for
compositions between dravite–schorl and elbaite–schorl solid solution pairs and end
members. However, this fit is lacking in tourmalines with intermediate Mg-Li
compositions; thus, the pure dravite–elbaite solid solution is not possible (Hermon et al.,
1973).
Si is assumed to occupy the T site exclusively, with Al making up for any deficiencies
(MacDonald and Hawthorne, 1995). Normalizations were carried out on the basis of 15
cations, exclusive of Na, K, and Ca, which assumes no vacancies in the octahedral and
tetrahedral sites (Henry and Dutrow, 1996). Schreyer et al. (2002) reported that
tourmalines with Al greater than 7 apfu (e.g., olenite) tend to have excess B. However, all
tourmalines in this study have less than 7 apfu Al; thus, it is likely that excess B does not
need to be taken into consideration.
This work contains 965 data points with 590 tourmaline analyses associated with
multiple mineral assemblages from various geographic locations throughout the Copiapó
area. Chemical analyses of associated minerals were also obtained for a more accurate
assessment of the mineralizing environment.
Boron isotope analyses: Boron isotopes were measured in-house by MC-LA-ICPMS
using a Thermo Scientific Isoprobe fronted with a 193 nm ArF excimer laser (New Wave
Research). Although the in-house Isoprobe is nominally set up and optimized to measure
high mass species (e.g., U and Pb isotopes for geochronology), similar instrumentation
has been successfully used to measure B isotopes, in solution, at other laboratories
(Aggarwal et al., 2004). The desired use of laser ablation for sampling, however,
necessitated minor adjustments to the method of Aggarwal et al. (2004) to achieve the
maximum sensitivity for boron. In particular, Aggarwal et al. (2004) report the use of a
6.2 mL/min He collision gas in their hexapole collision cell, to facilitate the reduction of
the incoming ion kinetic energy spread prior to entering the magnetic sector. Although
emulating this set-up produced an adequate 11B signal from solution (approximately
800mV/ppm B; acceptable for basic tuning), the equivalent 11B signal from ablated
tourmaline under standard operating conditions was only ~100mV (= ~3X10-3mV/ppm
B). This signal was insufficient to achieve a desired 2σ error on individual measurements
of less than ±2 per mil. Through testing of different collision gas mixtures, we
determined that a combination of 1.5 mL/min He and 8.0 ml H 2 increased the B signal
intensity by a factor of 4, while simultaneously reducing the measured uncorrected
11 10
B/ B ratio from values of over 8 down to values between 5 and 6 (closer to the natural
2
abundance ratio of ~4). Significantly, this reduction had the effect of minimizing the
instrumental mass fractionation correction required to derive the true isotope ratios of the
unknowns. The increased B signal intensity from ablated tourmaline while utilizing the
adjusted collision cell gas mixture also had the anticipated effect of significantly reducing
the 2σ error on individual measurements, down to ~0.7 per mil. The use of H 2 in the
collision gas did prompt some concern that increased hydride formation could be
problematic; however, no evidence of significant hydride production was observed.
Notwithstanding the collision gas composition, the Isoprobe set-up generally reflected
that of Aggarwal et al. (2004). The accelerating voltage was set to 6331 kV, and the
hexapole DAC was set to 13 percent to yield the maximum B signal intensity. 10B+ and
11 +
B were centered in L3 and H5 faraday detectors, respectively, corresponding to a
theoretical mass position of 10.4 on the axial detector. The cup positions were H5 = 5342
and L3 = 2085.
Samples and standards were mounted together in a single 2.5 cm diameter epoxy
block. The laser was set to an 8 Hz laser pulse rate, delivering a ~50 mJ energy output for
~25kV of potential. A spot size of 75 μm was selected as a compromise to maximize the
signal intensity while maintaining adequate spatial resolution. An individual analysis
consisted of a 30 sec on-peak background measurement (without firing the laser),
followed by 80 cycles of one-second integration-time per cycle. Between samples, it
generally took approximately 1 min for the B signal to return to background levels.
Ablated material was introduced to the plasma via He carrier gas flowing at 0.290 L/min
through the sample cell. This flow joined with a 0.2 L/min flow of Ar ("nebulizer gas 2";
0.1 L/min for solution tuning). Nebulizer gas 1 Ar was set to a 0.9L/min flow rate for
solution tuning, and reduced to 0.54 L/min for laser abalation. The ablated material was
introduced to the plasma in "wet plasma" mode; that is, a solution of 2 percent (v/v) nitric
acid was aspirated throughout the laser work. Under the tuning conditions, the Micromist
concentric nebulizer (Glass Expansion) aspirated a flow rate of ~100 μL/min. The
comparable flow rate under the somewhat reduced Ar flow for the laser conditions was
not measured.
Five to seven sample analyses were alternated with two to three analyses on three
standards run consecutively. The two main standards used in this study are a uvite from
Brumado, Brazil, and an elbaite from an unspecified Brazilian locality. The uvite was
separated from a rock containing only fine-grained white talc and abundant 5-7 mm green
transparent uvite crystals. The elbaite was a loose, 5 cm transparent crystal consisting of a
voluminous, nearly colorless core ("achroite"), overgrown by a very thin rind of blue
tourmaline ("indicolite"); only the colorless core was used. The uvite was previously
analyzed by SIMS, against the three standard tourmalines described in Dyar et al. (2001):
dravite #108796, elbaite #98144, and schorl #112566, giving a value of δ11B = +13.4 ±
0.9 per mil (2σ; n=4; unpublished data). The "achroite" was similarly previously analyzed
by SIMS, giving a value of δ11B = +0.4 ± 0.2 per mil (2σ; n=2; unpublished data). The
"achroite" was further analyzed by MC-LA-ICPMS against the Brumado uvite, giving a
value of -0.5 ±1.0 per mil (2σ; n=20 over two sessions; unpublished data). The latter
value for the achroite, based on a larger sample set and incorporating a more conservative
error, was used in this study.
Data were processed offline. For each analysis, a preferred mean "raw 11B/10B" ratio
and standard error were calculated from the filtered data (after excluding values outside
3
of 2σ from the full 80 cycle mean). These raw values did not include a correction for
instrumental mass fraction (IMF), and hence corresponded to apparent δ11B values on the
order of ~355 to ~385 per mil. Because of a time-dependent cyclic drift in IMF, a 2nd
order polynomial was used to graphically best-fit the IMF variations in the Brumado and
achroite standards, and the derived polynomial was used to correct for IMF in the
unknown samples. Despite some scatter within individual standards, there did appear to
be a slight difference in the instrumental mass fractionation between the achroite and
uvite standards, amounting to a maximum difference of ~3.5 per mil. Although this may
be attributable to matrix effects, a definitive interpretation is difficult because there were
periods of notable measurement instability (for reasons that were not clear), as well as the
possibility of minor isotopic heterogeneity in the achroite. Nonetheless, data collected
from a ferroan uvite secondary standard from Pierrepont, New York, measured
periodically during the day's run, agreed, within error, of published results (+13 ‰;
Swihart and Moore, 1989).
Appendix 2: Literature sources of tourmaline compositional data
Ayuso and Brown (1984); Bačík et al. (2008); Byerly and Palmer (1991); Cavarretta
and Puxeddu (1989); Clarke et al. (1989); Demirel et al. (2009); Dini et al. (2008);
Frietsch et al. (1997); Frikken (2003); Garda et al. (2009); Golani et al. (2002); Henry et
al. (1999) Henry et al. (2008); Jiang et al. (1995); Jiang et al. (1997a); Jiang et al.
(1997b); King and Kerrich (1989); Koval et al. (1991); London and Manning (1995);
Lynch and Ortega (1997); Mao (1995); Mlynarczyk and Williams-Jones (2006); Peng
and Palmer (2002); Pirajno and Smithies (1992); Plimer (1986); Plimer and Lees (1988);
Raith (1988); Slack and Coad (1989); Taylor and Slack (1984); Xavier et al. (2008);
Yavuz et al. (1999); Yavuz et al. (2008); Žáček et al. (1998).
Appendix 3: Petrologic descriptions of each sample
Chile\Cerro Negro Norte
C6B-076
Hand sample: Dark gray, Mt-bearing, Act-altered rock with a Tour-Sulf(Py>Cpy)Mt-Calc vein and a lighter feldspathic zone on one end.
Thin section: This sample contains a coarse-grained, inclusion poor Tour-Kfs-EpCalc-Sulf (Py>Cpy)-Chl(gray) ± Tit vein cutting an inclusion-rich (mainly Mt) Tour vein
in a rock that has sericitized Plag-Act ± Ep at one end and variable Act-Ep-Mt-rich
material in the middle and towards the other end along with Py. A considerable amount
of Hem in the matrix is being replaced by Mt. Act-Plag(sericitized) veinlets cut the
matrix and are cut by later Kfs veinlets. Tour is zoned, blue cores with tan rims in
sections parallel to c, with variable grain sizes (0.2 – 1.8 mm) and is pleochroic (tan to
dark brown, blue/tan to dark blue). Fine-grained Tour appears to be enveloped by coarser
grained Tour, which are commonly fractured and intergrown in some cases. Tour also
occurs outside of the vein, but has corroded edges. Ep also appears to be slightly altered.
This thin section displays a complex paragenesis with Tour in several assemblages all of
which are representative of what can occur in the magnetite-apatite deposits of the iron
belt.
4
Chile\Copiapó\Candelaria\Cerro Bronce_Estrella
C2B-298
Hand sample: This is an intensely altered, Qtz-bearing (15%), roughly equigranular
but crudely layered white rock with 15 percent dark mafic minerals in clots and a
medium green vein with a pale green envelope at one end. There is no K evident from
staining and there appears to be several generations of veins.
Thin section: It is unclear what the rock was originally, but it could have possibly
been a volcaniclastic. Ep-Tour-Tit veins run through the sample with polycrystalline
aggregates of 0.25 – 0.5 mm brown Hbl crystals with some Tit now in mafic sites. There
is also a fair amount of Pyx. A part of this sample is an intergrowth of Plag and 0.1 mm
diopsidic Pyx. Both Act-rich and Ep (with a little Amph) veins crosscut this assemblage.
Pale Act replaces darker brown Hbl in jackets around Ep veins. Hbl appears to be zoned.
The clear matrix is polygranular Plag 0.25 mm in size. Some Mt is present in the rock,
but about 50 percent is now altered to Hem. Tour has highly irregular grain boundaries
and appears to be unstable although it is possible that it may also be part of the alteration
assemblage. Tour ranges from blue to dark blue and non-pleochroic to brown and
pleochroic and from 0.06 to 0.2 mm in size. Tour appears to be intergrown with zoned Ep.
C2B-708
Thin section: Spectacular large sprays of sky blue to tan Tour in rock with Calc-Ser
(with light green pleochroism)-Hem and an unknown brown phase. Tour is either
columnar with or without irregular somewhat eaten edges, a morphology that is also
evident in Ep and Hem. This may reflect a later sericitic overprint of a calcic assemblage.
Tour also contains micron-scale inclusions of zircon. Rare Allan is also present.
Chile\Copiapó\Candelaria\Cerro Granate
C3B-072a
Hand sample: Recrystallized Plag-Rut-Chl(-Ser) rock possibly replacing tuff in the
Abundancia Formation(?). This is cut by Tour ± Qtz vein with inner Plag-rich envelope
and outer Kfs-dominated envelope.
Thin section: The Tour vein transitions from predominantly Tour with minor Calc to
Tour with some Qtz locally intergrown with specular Hem. The envelope to the vein is
virtually all Plag with sparse Rut or Hem. Along one edge of sample, there appears to be
a Chl-Ser-Carb veinlet. Outside of the envelope the rock is an equigranular, fine grained
Plag-dominant rock with distributed Ser-Chl-Rut(?) which accounts for ~5 percent of
rock. There appears to be two generations of Tour, longer laths and more granular
crystals, locally intergrown with iron oxide and Plag + Ser. Ep is somewhat ratty whereas
the Tour is well formed. Tour has undulatory extinction. Pleochroism ranges from a very
light color to a blue-green with brown undertones in some places. A smaller, fine-grained
Tour + REE veinlet appears to run through the main vein (~0.04mm across). The
majority of Tour in the vein is cm-scale
5
Chile\Copiapó\Candelaria\Española
C3B-381a
Hand sample: Foliated breccia of Alb(-Tour-Qtz-Py) assemblage with Qtz-rich
matrix probably superimposed on Alb-Py-altered volcanic or volcaniclastic rocks similar
to C2B-287.
Thin section: This is a penetratively deformed rock with Qtz-Tour veins grading
outward into Tour-Alb ± Fe sulfate (bright yellow) rock. The Fe sulfate is found
predominantly in Plag-rich zone, which contains strongly aligned feldspars. Within the
principal veins, there appear to be two generations of Tour, an early generation which is
fine-grained (<0.02 mm), corroded, and granular, and a later generation that is coarser
(up to 0.3 mm) and undeformed. There is also evidence of second generation Tour
overgrowths on preexisting Tour. The later Tour are lathlike, 0.03 – 0.28 mm in length,
euhedral, and intergrown with non-strained, non-oriented Qtz. The majority of Tour
grains are optically zoned (from blue-green to brown) and Tour laths display tan to darkblue green pleochroism. Opaque minerals appear to be mainly Lim and minor Rut.
Chile\Copiapó\Cerro Buitre Radio Tower
C2B-287
Hand sample: Alb-Py rock deformed and veined replacing a Qtz-poor porphyritic or
phaneritic igneous rock. This may represent early (pre batholith?) sodic alteration,
perhaps generated in a recharge zone.
Thin section: This sample is dominated by Plag with a cataclastic texture as well as
Qtz. Plag had once been > 2/3 of rock as some of the larger crystals appear to have been
Fsp phenocrysts. Plag is moderately turbid with no obvious Ser. It is quite possible that
there is 20 percent Kfs (20% untwinned Fsp) in this sample as indicated by staining
(found only by and in veinlets). There is ~5 percent Py in the rock along with minor Tour
and Apat. Veins of cryptocrystalline, fine-grained Qtz are also present, some of which
display yellowish birefringence. Some fine-grained Qtz is found cementing specular Hem
crystals and can also be found in specular Hem veins and with Lim after Py. Tour is
commonly found in clusters in association with Plag, Py, and Qtz and comprises maybe a
few percent of the rock. Tour is columnar with tan to blue green pleochroism. Crystals
are commonly anhedral or can occur in splays near Hem xtls (rare). Tour grains range
from 0.02 to 0.1 mm in length and some grains display brown cores with blue rims.
C2B-576c
Thin section: The rock contains abundant, green Bt-rich alteration. Specular Hem
veins contain evidence for alteration of specular Hem to Mt and back to specular Hem.
Hem(specular)-Bt veins cuts a granular Qtz vein that contains Cpy. Mt is roughly equant,
but ratty. Elsewhere in the rock is coarse muscovite (few 100 µm) intergrown with Bt.
Other veins are dominated by Bt and accessory Tour with rare Apat. There is no obvious
chloritization of Bt. Tour is found solely in a Tour-Bt vein. Tour is small (commonly less
than 0.05 mm), columnar, and pleochroic (tan to light blue).
6
C2J-124
Hand sample: Irregular, miarolitic-looking, aplitic rock with relatively little Kfs
(stain). Texture destructive acid (sericitic?) alteration of rock with abundant Qtz +
Musc(Ser) ± relict(?) Plag(?) and late generations of zoned Tour filling vugs. This is
probably intensely altered La Brea.
Thin section: Zones consisting of mainly intergrown Alb-Qtz grading into Qtz-TourHem(Mt?) comprise this sample. The Plag is variably sericitized. Most Tour grains are
either brown and not very pleochroic or tan with pleochroism ranging from brown to
green with light blue late cavity filling. Early Tour cores tend to have light gray to
lavender pleochroism. Tour crystals commonly have corroded edges and range from 0.15
– 0.35 mm in length. Tour can also be massive and forms a prominent brown spot on the
thin section. Tour also appears to overgrow 0.05 mm, equant to elongate zircon. Hem and
Tour occur in common association with Qtz, but typically not with each other. Hem also
contains tiny Rut needles.
C2J-334
Hand sample: La Brea-style porphyritic aplitic diorite with sodic(-calcic) overprint
affecting the mafic sites and some of the Fsp. This is perhaps superimposed on earlier
biotitic alteration. The main groundmass is gray and contains gray to weakly maroon Plag
phenocrysts. Considerable Kfs in groundmass of rock is typical of this type of material
when fresh and may not be reflective of alteration.
Thin section: This section contains sparsely porphyritic "adamellite" with 5 percent
Plag >3 mm. Rare Opx and Cpx are almost completely converted to pale sheaves of Act,
locally with Bt and rarely with blue to blue-gray to white Tour (± Lim). Tour is
pleochroic, blue to tan, and ranges from 0.06 to 0.2 mm in length. Tour clusters tend to
have ragged edges and occur in association with pale green Act, Lim, and Mt. Tour
grains with corroded edges tend to have undulatory extinction. One Tour crystal has pink
to dark blue-green pleochroism is subhedral, and 0.22 mm in length. Mt and Ilm are
common (Mt>Ilm). The majority of Mt has Hem on {111} and both typically have Ilm
rims. Late Qtz is widespread but less than 5 percent. Apat is common, often in crystals >
0.1 mm.
Chile\Copiapó\ Falla Ojancos_Transito_San Francisco
C6B-101b
Hand sample: Banded white to brown-gray, Alb(-Py±Mt/Hem) rock with banded,
fine-grained, Tour-rich veins, which are later cut by coarser Alb veinlets. The host is
probably volcanic or volcaniclastic rocks.
Thin section: Tour occurs as granular bands of brown, moderate relief minerals in
Alb-rich rock. Tour grains range from 0.05 – 0.1 mm across. Some of Tour bands are cut
by coarse-grained Alb veins. Large Tour grains are zoned from dark brown to brown and
are embayed in some cases. Lighter portions of the rock have Lim after Py and minor Mt
as well as a sparse brown mineral. The brown mineral in question appears to have a
7
botryoidal texture and is very fine grained. The Plag is sodic Olig as determined by
Michel-Levy and some large Olig sites could be relict phenocrysts. Plag appears to be
slightly altered. Allan may also be present
C6B-107
Hand sample: Angular, matrix-supported breccia of Alb(±Py±Rut) clasts and host cut
by Qtz-Tour veinlets. The dark green-gray matrix is very fine-grained Tour intergrown
with Qtz.
Thin section: The host is a varied, very fine-grained, granular felsic rock with some
clasts containing altered Plag (Alb by Michel-Levy) phenocrysts. The host is typical of
much of what is seen at Santos as clasts and cataclastic textures and size reduction are
evident. The rock is cut and veined by Qtz(± Tour ± Lim after sulfides). Qtz veins are
clearly broken and transported in the breccia. Individual Qtz grains appear to be slightly
deformed. The breccia matrix is very fine-grained, dark green-grey, and consists
primarily of elongate, zoned grains of Tour 2-5 µm across. Tour also occurs outside of
the breccia matrix, are commonly larger (10-20 µm), and intergrown with Qtz.
Chile\Copiapó\Jesus Maria
C7B-003a
Hand sample: Tour-Dum assemblage in Qtz-Calc-rich sediments or volcaniclastic
rocks possibly contact metamorphosed by the La Brea pluton.
Thin section: Tour is light blue and visibly zoned going from light brownish blue to
blue-gray to very light from core to rim. Tour ranges in size from 25 μm to slightly
greater than 0.3 mm. Tour also contains inclusions of acicular needles of Dum (>0.1 mm
long and only microns across) and rare Anhy. Dum is very blue and is present throughout
the rock but is concentrated in certain areas where they appear to have replaced earlier
grains. Dum that replaced earlier grains tends to be very fine-grained (<0.01 mm). Early
Tour appears unstable in areas where Dum is abundant. Tour is rimmed by a very pale
late zone that appears to be in equilibrium with the other minerals. Late Tour also forms
comb-like overgrowths on embayed or euhedral edges of early Tour. The groundmass
contains abundant equigranular Qtz-Calc-Mt/Hem. Mt blades contain zones of replacive,
specular Hem. Minor Ep is also present. Certain areas of the rock also contain Prl.
Chile\Copiapó\Ojancos Viejo
C3B-429.5
Hand sample: Alb(-Py-Clay[?]) altered volcanic or volcaniclastic rock cut by Tour-Py
veinlets partly oxidized to Lim and Jar.
Thin section: This sample contains a Tour-Clay-Py (now Lim) vein cutting a Plagdominated rock with 30 – 40 percent 0.5 – 1 mm, generally rectangular, but commonly
irregular Plag in a groundmass of fine-grained Plag. Plag is twinned, shows little zoning,
is variably turbid, and exhibits fairly uniform extinction. The overall texture is clastic to
8
cataclastic with minor specular Hem and Lim after Py in the matrix. The vein contains
spectacularly zoned Tour and a colorless sheet silicate with first order gray colors. Tour
is optically zoned with blue-green cores to brown rims and ranges between 0.2 – 10 mm
in length and averages 0.2 mm across. Tour does not appear to have a preferred
orientation within the vein and numerous cross-sections are visible. The vein also
contains minor amounts of Plag. Outside of the vein, Tour is rare and occurs in
association with Lim and Plag.
Chile\Copiapó\ San Gregorio S Granate
C2B-352e
Hand sample: Coarse-grained, microgranite grading to coarser crystals with less Bt
and seriate texture (1 – 3 mm) with a few larger Plag. At one end there is a Qtz-TourKfs>Plag vein with interspersed miarolitic cavities. K-staining shows more intense color
in hydrothermal assemblages, but there is no evidence of replacement. Tour-rich
miarolitic segregation in aplitic dike cuts relatively fresh San Gregorio pluton. This is
among the clearest and simplest magmatic tourmaline in the district.
Thin section: This sample consists of a Qtz-rich aplite/microgranite with variable
textures yet constant proportions of minerals. There is a prominent Tour vein at one end
that contains an abundance of relatively unaltered Plag along with Kfs and Qtz. All of
these phases appear to have grown together. Tour is brown and massive with inclusions
of Qtz and Tit. Plag grains in Tour vein have embayed edges. Late Tour forms needlelike,
light blue overgrowths on early Tour. Outside of the vein the alkali Fsp is weakly
perthitic, with an abundance of Plag dusted with white micas. There is also some
Hem(Mt) and large grains of Ilm that look pretty fresh in places.
C2B-655
Thin section: Nearly jet black, opaque Tour is overgrown by multi-colored (dark blue,
dark green, and various shades of brown) zoned Tour. There are several textures and in
some areas Act is clearly being replaced. Ep-Mt-Tit-Plag are associated with Tour as well.
There is abundant, coarse-grained Bt, Ep, and Tour. Possible Fe-sulfate (bright yellow
mineral) may be present. Kfs and Qtz are also present. Tour is complexly zoned and has
complex associations with other tourmalines as well as other minerals. Color ranges from
brown to very dark blue and late generations of Tour are highly irregular. Late Calc
veinlet runs through the section. Mt is the dominant oxide. There are at least three
generations of Tour and brown Tour similar to that found in C2B-352e is also present.
C2B-671
Hand sample: This sample contains a complex Tour-bearing vein in brecciated,
intensely sodic-calcic altered (Act-Ep-Chl-Alb), coarse-grained diorite either of San
Gregorio age or older (La Brea). Sr work indicates small component of external Sr in the
Act, however the main vein tourmaline has ratios identical to magmatic values.
Thin section: Brown Tour vein with network filling envelope is found with Alb (wide
twins) adjacent to Ep-Act(Tit[yellow]-Mt-Apat-Cpx) altered San Gregorio monzodiorite.
9
Alb is much more common than either Act or Tit. Remarkably all Tour shows identical
extinction and there is no obvious color zoning. Pleochroism ranges from light brown to
dark brown and is similar in appearance to Tour from sample C2B-352e. The Tit color is
also remarkable.
C2B-808.2
Hand sample: Relatively fresh, coarse-grained San Gregorio Qtz monzodiorite with
early Pyx overgrown by late Amph and Bt. There are rare, late (proto-miarolitic?) Tourbearing zones/cavities.
Thin section: This sample contains relict Opx bordered by Mt and overgrown by Bt
which is overgrown by Amph. There are significant amounts of Alb (>15%) and Qtz
(10%). Zircons are also present as inclusions in Bt, as evidenced by radiation damage
halos. This rock also displays myrmekitic textures. Cpx is still present in places. Oxides
are dominated by Mt with a Hem overprint on about 50 percent of existing crystals. 20
percent of the mafics are an equal distribution between Pyx and Bt, with good magmatic
foliation. Tour exists in cavities and in alteration assemblages along with Bt, pale green
Act, and beige Chl. Tour varies in color from tan to dark blue and appears to occur in two
separate generations. The tan Tour tends to have corroded edges and is commonly
intergrown with Bt, Chl, and Tit. The blue to dark blue, zoned Tour, on the other hand,
tends to be prismatic except where overgrown by chloro-potassichastingsite. Individual
Tour grains range from 0.01 – 1.4 mm in size. Other minerals with which Tour is found
in close association are Plag, Opx and Qtz.
Chile\Copiapó\Santos PdC
DDH289-037.5a
Hand sample: The contact between crystal-rich and crystal-poor biotitized porphyritic
andesites is a Tour-Qtz-Py-rich zone that is perhaps at the original contact. The crystalrich (35%, 0.5 – 1 mm Fsp) side appears to have a chilled margin against the contact.
Thin Qtz veins are present in the crystal-rich side up into the chill zone. At one side of
the contact Mt is variable whereas on the other Mt is associated with pinkish Fsp and rare
Sulf veinlets.
Thin section: This sample contains a crystal-rich Plag porphyry (50%, 0.2-1 mm Plag;
<5% mafic sites) with little or no original Qtz crystals. Qtz is now altered to turbid Alb
with common Chl. Sparse Mt(Mushk?) veinlets are present along with common greenbrown Bt in association with green-grey Chl in matrix and in Qtz veinlets. The timing of
Bt and Chl is not clear, but Bt might post-date Chl in places. The breccia zone contains
complex heterolithic fragments including very fine-grained trachytic clasts and others
clasts containing isolated Fsp crystals. The matrix is very fine-grained and dark, though
not uniform. Tour is locally present in veins with Qtz-Py-Bt ± Mt as radial splays. Tour is
zoned, commonly with lighter cores in cuts looking down the c-axis or darker cores as
evident in the radial splays. Individual crystals are 0.1 – 1.2 mm in length and 0.04 mm
across on average. Tour is also pleochroic ranging from light tan to dark blue-green. Qtz
veinlets, some of which contain Tit, cut host and breccia, but appear to be offset by Py-
10
Bt-Tour or Py-Mt-Ser-Bt veinlets along the main zone. Tour is present in the matrix as
well. Py is both euhedral and has an unusual "shattered" habit where it might be locally
replaced by Mt. Rare Lim, Ilm, and Ep are also present.
DDH291-188.4
Hand sample: Fine-grained, weakly porphyritic, dark green rock cut by several vein
types including: a thick gray-green Chl(-Bt)-Py(-Cpy-Ep) vein (with Bt-Tour-Qtz-rich
margin); various dark green, thin Bt veinlets (±Qtz±Tour); and a larger Ep-Qtz-Bt+Cpy
vein. In hand specimen, the Qtz-Bt-Tour appears to cut the Ep-Cpy-Qtz-Bt vein. Kfs is
locally present at one corner of the billet. There is also a possible Bt-rich envelope on a
composite Act-Py-Cpy-Mt vein in fine-grained, medium to dark gray, felsic
volcaniclastic or volcanic rock.
Thin section: This sample is composed of green, intensely biotitized, mafic(?)
porphyritic rock with 20 – 30 percent, 0.1 – 0.4 mm mafic(?) sites now completely
converted to green Bt as is the groundmass. 1-3 percent equant sites with Qtz-Ep-Bt may
have been Fsp phenocrysts (0.2 mm). Multiple veins cut the rock. Two late vein types
include Chl-Bt(-Ep-Qtz-Py-Cpy ± Tour)enveloped by Bt-Tour-Qtz and Qtz-Tour ± Bt ±
Mt. These both cut coarse-grained Bt-Ep-Qtz(-Cpy) veinlets that have remarkably little
deformation even though the cross-cutting Qtz veinlet is clearly deformed. Tour is only
0.04 mm on average, blue to tan, and is very small in comparison to larger Bt and Ep
grains. Tour is commonly found in the Bt groundmass. Sulfides are restricted to the veins.
Py is zoned. Mt is equant.
DDH384-004.2
Thin section: Tour vein (about 1 mm across) surrounded by sericitized Plag and Chl
although it is also intergrown with well-formed Plag. Blades of specular Hem irregularly
line the sides of the vein. Calc in very fine-grained masses to coarser grains is present in
variable quantities throughout the vein. There seem to be Calc-replaced grains within the
vein and in some areas there appears to be evidence of flow or deformation. Tour is
variably fractured, ranges in size from 0.04 mm to >1mm, and are pleochroic from tan to
blue-blue brown. Tour is also found as fine needles and coexists with specular Hem, Kfs
and Calc. Yellow, zoned Ep is also present, but rare.
DDH628-094.2
Hand sample: Anhy-Py-Mushk-Cpy vein fill with Mushk-Cpy-Qtz outer vein in finegrained gray host.
Thin section: This sample contains a composite Mushk-Anhy-Qtz-Cpy-Py-Tour vein
in a complexly biotitized porphyritic host, possibly brecciated. The central part of the
vein contains Anhy(-Cpy-Py) grading into an outer zone of Mushk-Qtz(-Cpy-Tour)
where Tour occurs as isolated grains or in small clusters. Tour is columnar, zoned and
appears to be growing off of the Mushk grains in some cases. Tour displays tan to brown
pleochroism or is non-pleochroic with a light blue core and dark blue rims. The Qtz is
strain-free for the most part and contains relatively large fluid inclusions of various types.
The Bt-rich host appears to have Scap sprays in one area. This rock contains multiple
11
events with Ep-Mt-Cpy-Qtz-Chl in addition to fine-grained Bt and may represent an
original or hydrothermal breccia of a weakly porphyritic rock.
DDH628-150.6/DDH628-151.6
Hand sample: Py-Cpy-Tour vein with white envelope cuts representative massively
biotitized porphyritic host rock typical of a broad interval. K-stain shows that Kfs is
abundant throughout the matrix, mainly in the groundmass but appears to be absent in the
white vein envelope.
Thin section: Intensely biotitized, porphyritic volcanic rock with 30 percent, 0.2 – 0.5
mm biotitized phenocrysts has abundant clouds of Mt away from central vein. Mt
disappears approaching vein. Kfs might become more intense and in the inner (white)
envelope Qtz replaces most minerals, although some green-brown Bt remains. There is
one spot of blue-green Bt. Allan is locally present in envelope. The main vein is Tour-PyCpy(-Mt[Cpy]-Allan-Chl-Bt) and also contains scattered amounts of Apat. Allan shows
nice twins. The host contains thin Qtz-Bt (-Cpy-Ep) veinlets that are truncated by the
large vein. A late Calc veinlet cuts the large vein. The vein has abundant Tour ranging
from less than 0.02 - 0.2 mm and is also found within Py and chloritized grains outside of
the vein. Tour is pleochroic from tan to blue-blue brown and is variably fractured
perpendicular to the c-axis
DDH628-626.3
Hand sample: This sample contains a Mushk-Py-Act-Scap veinlet with Bt-rich
envelope in dark host.
Thin section: This sample contains a large Scap-pale blue-green Bt(-Chl) vein that is
offset in the middle of the section by about 1.3 cm. The Scap within the vein lacks a
preferred orientation. Py with minor Mt and trace Cpy occurs in the vein as well. Py
crystals are ragged and have spotted margins in places with abundant tiny inclusions of
Cpy and silicates. Mt within the vein locally contains Cpy as well. The vein has an
apparent brown/olive green Bt-Mt(trace Allan-blue Tour) envelope grading out into less
Bt-(and Mt?)rich material. The main vein cuts veinlets with Qtz-Apat-Bt-Mt. Qtz-ApatKfs is found along edges of the Scap vein as well. A Qtz-Tour vein cuts through the
envelope, but is truncated by the Scap-Bt vein. Tour has no preferred orientation, is
pleochroic (tan to blue), and can either be columnar (0.02 – 0.08 mm in length) or occur
in radial splays (0.02 mm across). Tour is found within biotitized clasts (rare) as well as
scattered in trace amounts throughout the groundmass.
DDH643-595.5
Hand sample: Angular, breccia zone with tan clasts with Mt rims. The matrix is Qtz
with gray, variably feldspathic clasts and host. Sparse, later Mt[Py] veinlets with possible
Kfs are also present.
Thin section: This sample consists of a composite Qtz-Allan-Tour-Mt/Mushk-CpyKfs breccia zone with many shard-like clasts cutting through biotitized porphyritic rock.
The dark host contains 10-15 percent, 0.3 – 0.8 mm Fsp phenocrysts partly altered to
12
green Bt, but mainly to secondary Fsp (possibly Alb) ± Qtz with 10 percent fine-grained
Mt + rare Rut in original oxide sites(?). This grades into a Kfs-altered zone/vein towards
the margin of the breccia with less Mt, sparse very fine-grained Chl, and no Bt. Other
clasts on this side of the section show similar features and appear to be mixed and cut by
Qtz-Allan-Tour-Mt/Mushk-Cpy-Kfs veins/matrix. A prominent trapezoidal clast is
surrounded by several generations of Qtz. At one end, it has massive Chl-Allan-Mt ±
Tour which grades into Mt-rich porphyry with Bt-Mt-Kfs±Qtz. This clast is cut on one
side by a composite Qtz/Qtz-Tour vein and the breccia side by Qtz-Tour-Allan which had
an earlier Allan-Tour vein that is later cut by a Qtz vein at the short end. The clasts in the
Qtz vein are combinations of Allan-Qtz-Chl-Tour with various Tour or Allan rims,
sugary or recrystallized Qtz zones, and accessory Mt. All of these features are cemented
by several generations of Qtz-Allan(Ep)-Tour-Mt-Mushk-Cpy. Tour is columnar,
commonly zoned with lighter cores and darker rims, and occurs in association with Allan,
Bt, Mt, Mushk, Qtz, Py, Chl. The length of Tour grains ranges from to 0.01 – 0.3 mm.
Tour inside clasts, some of which are deformed, appear to have the same optical character
as the Tour rimming the clast. There is evident replacement of Plag(?) by Allan, Chl, Qtz,
Mt, and Mushk.
DDH684-079.8
Hand sample: Fine-grained biotitzed, phenocryst-absent, volcanic rock (medium to
dark green in color) with clast(?) of darker green material, cut by Fe oxide veins and by a
dark dike(?) of Qtz-Tour-Py breccia fill, ragged edges, and white, Alb-rich envelope.
Thin section: The host is biotitized subequigranular rock with abundant 0.2 mm Qtz
and Plag, probably volcaniclastic protolith. Mafic sites now contain very fine-grained
aggregates of bright green Bt. Similar Bt (rarely Chl) occurs along veins with Cpy-Mushk
and early Py. Py in matrix can be complexely zoned. The veins have Kfs-Qtz ± Bt (or
Chl) in addition to Mushk[Py] and Sulf. Very fine-grained, dark zone of Qtz-Tour with
mafic-free Qtz-Plag envelope, a rim of Mt(partly Mushk)-Cpy and inclusions of Qtz-Plag
and Qtz-Tour (with sharp contacts) and interior Cpy[Py]-Py-Hem-Mt (equilibrium
textures). Pale to blue Tour are very fine-grained to greater than 0.1 mm. Pleochroism
ranges from pale yellow to light green or blue. Only a few tourmaline intergrown with
Qtz are >0.2 mm. Tour does not occur outside of the vein.
ME013-538
Hand sample: Composite Bt-Sulf(-Tour-Ep) vein with clasts in complexly altered
albitofiro. Envelope on vein appears to be Bt-rich (tan with green patches) and grades out
into less altered texture-preserving material.
Thin section: This sample is comprised of red Bt-Tour-rich vein with later Ep +
Py(+Sphalerite-Cpy) in a Bt-rich, altered, porphyritic volcanic rock. The host also
contains scattered Py+Sph(Cpy)+Ep+Qtz. Sph is quite abundant as small grains and can
be found in Fsp sites as well as veins and vugs. Two different colors of Bt correspond to
differences in color in the rocks: pale green and deep red brown. Tour is small (<0.2mm),
blue, columnar, and occurs with Ep, Bt, Lim, Py, Qtz, Plag.
13
Chile\Copiapó\Vinita Azul
C6B-160b
Hand sample: Bedded grayish quartzite (possibly originally volcaniclastic now
completely altered) with sand grains up to 0.4 mm cut with And(-Hem-Laz-TourPyroph[?]) assemblage with a possible metamorphic overprint on earlier alteration
assemblage.
Thin section: 66 percent sutured Qtz, 25 percent And, 5 percent Hem, and <2 percent
Rut comprise this sample with minor fibrous, blue Tour, trace Lazul, and minor (<5
percent) brownish fine-grained, second order colored sheet silicate (Pyroph?) that appears
to be late. The rock is cut by a veinlet of Hem-And-Tour ± Qtz with large And crystals
(less than or equal to 1 mm) overgrowing Hem and may possibly be metamorphic in
origin. And is subhedral and poikilitic. Rut occurs in equant grains whereas Hem is
elongate. Tour tends to have a columnar crystal habit and Tour aggregates are no larger
than 0.08 mm. Pleochroism ranges from light tan to blue.
Mineral abbreviations
Act: actinolite, Alb: albite, Allan: allanite, Amph: amphibole, And: andalusite, Anhy:
anhydrite, Apat: apatite, Bt: biotite, Calc: calcite, Carb: carbonate, Chl: chlorite, Cpx:
clinopyroxene, Cpy: chalcopyrite, Dum: dumortierite, Ep: epidote, Fsp: feldspar, Hem:
hematite, Hbl: hornblende, Jar: jarosite, Jsp: jasperoid, Kfs: K-feldspar, Lazul: lazulite,
Lim: limonite, Mt: magnetite, Musc: muscovite, Mushk: musketovite, Olig: oligoclase,
Opx: orthopyroxene, Plag: plagioclase, Prl: pyrophyllite, Py: pyrite, Pyx: pyroxene; Qtz:
quartz, Rut: rutile, Scap: scapolite, Ser: sericite, Sph: sphalerite, Sulf: sulfides, Tit:
titanite, Tour: tourmaline
Appendix 4: Chemical characteristics of each sample
Chile\Cerro Negro Norte
C6B-076
Tourmaline within the vein is primarily euhedral with concentric zoning. Some
tourmaline grains contain anhedral cores with albite overgrowths, followed by concentric,
euhedral tourmaline that becomes progressively more aluminous and magnesian and then
drops back towards the initial composition. Fine-grained tourmalines appear to have low
Al, but comparable Mg# values to the coarse-grained tourmaline. Outside of the vein,
tourmaline is corroded and has embayed edges with cores that have higher Al and
Mg/(Fe+Mg) values than the optically darker, later rims. There is a positive correlation
between Na and Al, with optically lighter cores and rims displaying the highest
concentrations of both elements, and a negative correlation between Ti and Al as well as
Fe and Al. Tourmaline compositions changed from primarily dravitic to uvitic
compositions with some variation in Fe contents.
Chile\Copiapó\Candelaria\Cerro Bronce_Estrella
C2B-298
14
The earliest generation of blue tourmaline plots on the schorl-dravite solid solution
series whereas later, darker tourmaline overgrowths are more calcic and geochemically
similar to the brown tourmaline found in another part of the section. Brown tourmalines
from this area have intermediate Mg/(Fe+Mg) values and belong to the uvite-feruvite
solid solution series. Unlike the earliest generation, later tourmalines are also Al-deficient
(less than 5 apfu Al) and have higher Ti contents (up to 0.3 apfu).
C2B-708
Tourmalines in this sample have almost no Ti. Early generations of tourmaline are
dravitic whereas later generations are schorls, Al-deficient, and have slightly higher Ca
contents (up to 0.3 apfu). Fe-rich generations are optically darker than the dravitic
generation.
Chile\Copiapó\Candelaria\Cerro Granate
C3B-072a
Tourmaline from this locality plots within the schorl-buergerite compositional field
and ranges from Al-rich to Al-deficient denoting an overall change from aluminous to
more Fe-rich compositions. As with many of the tourmalines from this area, the chemical
variation is not uniform. Overall, zoning is highly complex and it appears that the Fe-rich
generation acts as fracture-fill in more aluminous phases during a different tourmalineforming event. The Mg/(Fe+Mg) values range from about 0.2 to 0.4. Ca concentration
increases from about 0 to almost 0.2 apfu in later generations, but Na is the dominant
alkali.
Chile\Copiapó\Candelaria\Española
C3B-381a
Late tourmaline laths and overgrowths tend to be deficient in Mg and Al in
comparison to the earlier, granular generation. However, late tourmaline has higher Fe
and Na concentrations than the early generation. These generations form two distinct
groupings. Within the granular generation there seems to be very little variation in the Al
content, but there is an overall increase in Mg and decrease in Fe from core to rim
(schorl-dravite substitution along the YMg  YFe2+ exchange vector). This generation
also has slightly higher Ca values (possible uvitic component). However, in some areas
with dark euhedral to subhedral cores with well-preserved zonation it appears that Fe
increases as Mg decreases from the core to the rim. Zones in late tourmaline display the
opposite trend with decreasing Fe and slight increases in Mg and Al from core to rim.
Tourmaline chemistry changes from dravite in the granular generation to schorl in the
later generation.
Chile\Copiapó\Cerro Buitre Radio Tower
C2B-287
The tourmaline in this sample represent two chemically distinct generations between
which there is no compositional continuum. The tourmaline is not concentrically zoned
and the earlier cores have highly irregular boundaries within the later, rimming
15
generation. The first generation is Mg- and Ti-rich (averaging around 0.45 apfu, but can
be as much as 0.8 apfu) whereas the second generation is Fe-rich and Ti-poor. F also
tends to be higher in the first generation (up to 0.19 apfu). The Al values of both phases
are comparable. Overall, these tourmalines are dravites with the later generation trending
towards more intermediate schorl-dravite compositions.
C2B-576c
Surprisingly, tourmalines from this sample are not zoned although there is evidence
for slight chemical variation. Tourmalines from this sample are largely Fe-rich dravites
and have greater than 6 apfu Al.
C2J-124
Older generations of tourmaline tend to have lower concentrations of Fe and Mg,
which corresponds to a higher Al content, than the younger tourmaline host, thus forming
a chemically distinct group. The first generation is also Na-poor and has embayed or
corroded edges. It is evident that the early generation was destabilized and incorporated
into a Na-, Fe-, and Mg-rich generation. There is also evidence for a distinct generation
that is Fe-rich and Mg-poor and is part of the later rimming phase. Zoning is patchy or
interfingering with optically lighter zones corresponding to higher Na contents than
darker zones. This style of zonation may indicate a different substrate for tourmaline
growth and/or the tourmalinization of an earlier mineral. Lighter cores surrounded by
darker rims tend to have higher Fe and lower Mg concentrations than its rims. Because
zonation is so complex, there is no uniform progression in elemental abundance. Later
generations of tourmaline have higher Ti and F contents. The tourmalines are schorldravite in composition.
C2J-334
The core of a single tourmaline lath has slightly higher Al and Mg/(Fe+Mg) values
than the latest rims on opposite ends. The latest rims appear to plot in a single group with
lower Al, but comparable Mg/(Fe+Mg) values, than the darker cores. The latest rims also
appear to have slightly higher to comparable Ca contents with little room for vacancies,
whereas the earlier group has a slightly higher foitite component. The same trend is not
observed in all tourmaline grains and there is no apparent correlation between Na and Al.
Overall, these tourmalines are uvitic in composition.
Chile\Copiapó\ Falla Ojancos_Transito_San Francisco
C6B-101b
These tourmaline have high Ti overall (up to 0.4 apfu) with respect to C6B-107. The
most abundant generation is Mg-rich and may contain Fe-rich cores and rims. These
tourmalines plot within the dravite compositional field.
C6B-107
In this sample, cores are more aluminous and magnesian in comparison to rims or
certain sectors/apices which have low Al and slightly lower Mg/(Fe+Mg) values. Lighter
zones in back scattered electron images have the highest Ca, Fe, and Ti contents and the
16
lowest Na and Al values. There is no direct correlation between Na and Al although there
are two different groupings corresponding to lighter and darker zones. Tourmaline
compositions are dravitic.
Chile\Copiapó\Jesus Maria
C7B-003a
Tourmaline cores are Fe-rich and, where present, are rimmed by euhedral to anhedral
Mg-rich tourmaline. These later phases may later be rimmed by an acicular to comb-like
Al-rich tourmaline phase. F contents range from slightly greater than 0.2 apfu in the
earliest generation to 0 apfu in the latest generation. In areas where dumortierite is most
abundant only the early, Fe-rich tourmaline generation remains and is highly irregular.
Tourmaline compositions plots along the foitite-magnesiofoitite solid solution.
Chile\Copiapó\Ojancos Viejo
C3B-429.5
Zoning is highly irregular and patchy. There appear to be three main groupings. The
first appears to correlate with the zone that is closest to the center of the tourmaline in
sections parallel to the c-axis. This group has the greatest Al concentrations and low Fe,
Ca, and Na. The second grouping corresponds to the final, dark (in back scattered
electron imaging) zone exhibited by the majority of the tourmaline grains with high Mg,
higher Ca, moderate Al, lower Na, and low Fe contents (possibly indicative of YMg 
Y
Fe2+ and XNa + YAl  XCa + YMg substitution). The third group corresponds to early
and late lighter zones that can be found irregularly rimming group 1, being rimmed by
group 2 and, in turn, also rimming group 2. This group has the highest Na concentrations,
high Fe, moderate Mg and Al, and low Ca contents. In tourmaline with concentric zones,
there is no real trend. Overall, intact cores tend to have the highest Fe concentrations and
the latest rims have lower Fe concentrations than the earlier rims (schorl-dravite
substitution). Later rims, those with low Fe contents, have higher and highly variable Ca
and Ti concentrations whereas tourmaline cores occupy a narrow range of Ca and Ti
values. The composition of tourmaline is initially dravitic trending towards uvite and
schorl.
Chile\Copiapó\ San Gregorio S Granate
C2B-352e
Some tourmaline generations from this locality overlap the brown, Ti-rich generation
found in sample C2B-808.2 as well as the blue tourmaline cluster found in the same
sample. There is a late, light green, Al-rich tourmaline generation (similar to those seen
in C2J-124) that forms acicular needles around preexisting tourmalines and can also be
found in cavities. Tourmaline compositions from this locality range from schorlbuergerite to feruvite. There is no clear relationship between Fe, Mg, and Al or any
systematic change in composition.
C2B-655
17
This sample contains Fe-rich, Al-deficient tourmaline cores, overgrown by
comparably Al-rich, subhedral rims that are slightly replaced by Fe-rich, Al-deficient
tourmaline. Both the early and the latest generations appear to have the same composition.
The Al-rich rims have intermediate schorl-dravite compositions whereas the Fe-rich
generations have intermediate feruvite-uvite compositions. The latter generations tends to
have higher Ti contents (up to 0.3 apfu).Where the third generation of tourmaline is not
present, the Al-rich generation is altered and appears to have multiple reaction rims and
textures. A late dravitic generation is also present and tends to be subhedral and sky blue.
C2B-671
There are multiple generations of tourmaline, but for the most part they fall into two
populations: a lower Al and higher Ti (slightly higher than 0.3 apfu), intermediate
feruvite-uvite population that is locally rimmed and infilled by a more aluminous phase
that has a higher sodic component.
C2B-808.2
This sample contains two distinct episodes of tourmaline growth. The first is blue, Ferich, complexly optically and compositionally zoned, and slightly replaced by chloropotassic-hastingsite. The second generation is brown, Mg- and Ti-rich and intergrown
with titanite. There is no clear relationship between Fe, Mg, and Al. The overall
tourmaline composition of this sample fluctuated from schorl to feruvite back to schorl.
Chile\Copiapó\Santos PdC
DDH289-037.5
Later generations of tourmaline have higher Fe contents and lower concentrations of
Na, Mg, and Al although there is no progressive trend. Tourmaline crystals with corroded
or inclusion-rich cores have lower Mg/(Fe+Mg) values than well-formed tourmaline with
preserved zonation. Overall, cores appear to have among the highest Mg and Fe
concentrations combined with the lowest Al values in comparison to the other zones.
Optically lighter cores tend to have high Al and Na contents. Within the same tourmaline
lath, Na content changes by almost 0.3 apfu from one end to another. Cross-sections of
tourmaline perpendicular to c show a marked increase in Al and a slight decrease in Na
followed by an Al content that is midway between the core and first zone, but with lower
Na content. Tourmaline compositions are primarily schorl-dravite. There appears to be no
set pattern to Fe-Mg chemical variation.
DDH291-188.4
Tourmaline has intermediate schorl-dravite compositions with slightly more
magnesian later generations. Ti is low and Ca is variable (up to 0.3 apfu) and tourmaline
is well formed. Al contents range between 5.5 and 6 apfu.
DDH384-004.2
Early generations tend to have a higher uvitic component than later generations which
have higher Na contents and are slightly more magnesian. Later generations often rim
18
earlier generations or are found in fractures. Overall, these tourmalines can be classified
as dravites.
DDH628-094.2
Blue tourmalines tend to have a slightly higher X-site vacancy, Ti, and Fe values than
tan tourmalines. Tourmalines from this sample display concentric to patchy zoning and
are euhedral. Ca content is low. The tourmalines from this sample can be classified as
Mg-rich schorls.
DDH628-151.6
There are at least three tourmaline generations from this sample. All tourmalines tend
to have high Na/(Na+Ca) values (generally greater than 0.75) and have intermediate
schorl-dravite compositions. Tourmaline cores tend to have slightly higher Fe values than
rimming phases although rims outside of the vein tend to have high Fe contents as well.
Ti contents are low overall.
DDH628-626.3
Tourmaline cores are highly deficient in Ca. The rims contain negligible Ca, but
higher overall values than the core. Ti appears to be inversely correlated to Fe on the
majority of the rims, but not in cores. The cores contain Fe, Mg, Al, and Na and have
higher Mg/(Fe+Mg) values than the rims which tend to have higher Al concentrations
and lower Mg/(Fe+Mg) values overall. In the rims, where Fe and Al are high, Mg and Na
are low. The zones alternate between high Mg and Na to high Al and Fe. The final
preserved rim shows high Fe and Al contents. This trend is consistent with alkali-defect
[NaMg(□Al) -1 ] and Mg(Fe) -1 substitutions. The former substitution is supported by a
positive linear correlation between Al and X-site vacancies, suggesting a magnesiofoitite
component. There is also a negative linear correlation between Na and Al. In fine-grained
vein tourmaline, there appears to be no progressive change in composition as the zoning
is highly irregular. Overall, tourmaline compositions plot in the schorl-dravite
compositional fields.
DDH643-595.5
There are three potential tourmaline generations in this sample. Tourmaline cores are
commonly Fe-rich dravites and tend to have higher Na and Mg contents than later rims.
The second generation has lower Na and higher Ca and Fe than the first generation, forms
euhedral rims, and has intermediate schorl-dravite compositions. The latest generation is
a Mg-rich schorl with higher Na/(Na+Ca) values than the first generation and comparable
to slightly greater Fe contents. This later generation also has variable vacancy ratios up to
0.55. Overall, these tourmalines are only slightly Al-deficient (Al contents less than 6
apfu).
DDH684-079.8
Tourmalines from this sample are very fine-grained and have intermediate schorldravite compositions with low Ca and Ti.
ME013-538
19
Tourmalines from this sample are well-formed and contain low Ti and Ca. Zoning is
patchy to concentric. Overall, these tourmalines are schorls with the core of one
tourmaline containing a significant foititic component.
Chile\Copiapó\Vinita Azul
C6B-160b
Tourmalines from this area have low F and 0.3 – 0.5 apfu X-site vacancies.
Tourmaline composition falls along the dravite-magnesiofoitite solid solution and is Alrich with greater than 6 apfu Al. There is no evident zoning.
Mineral abbreviations
Act: actinolite, Alb: albite, Allan: allanite, Amph: amphibole, And: andalusite, Anhy:
anhydrite, Apat: apatite, Bt: biotite, Calc: calcite, Carb: carbonate, Chl: chlorite, Cpx:
clinopyroxene, Cpy: chalcopyrite, Dum: dumortierite, Ep: epidote, Fsp: feldspar, Hem:
hematite, Hbl: hornblende, Jar: jarosite, Jsp: jasperoid, Kfs: K-feldspar, Lazul: lazulite,
Lim: limonite, Mt: magnetite, Musc: muscovite, Mushk: musketovite, Olig: oligoclase,
Opx: orthopyroxene, Plag: plagioclase, Prl: pyrophyllite, Py: pyrite, Pyx: pyroxene; Qtz:
quartz, Rut: rutile, Scap: scapolite, Ser: sericite, Sph: sphalerite, Sulf: sulfides, Tit:
titanite, Tour: tourmaline
Appendix 5: Other interesting graphs
This section contains interesting graphs (Figs A2-A4) reinforcing the trend towards a
similar Fe-rich composition and negative correlation between Al and total Fe as well as
variations in other elements such as Ti and F. High Ti and the presence of hydrothermal
titanite could be related to the breakdown of hornblende during hydrothermal alteration
(Lynch and Ortega, 1997). Slack and Coad (1989) noted that systematic Ti variations
may be also be controlled indirectly by the chemical potential of Al during alteration and
mineralization (i.e., □Ti(NaAl) -1 ). F concentrations are highly variable in Copiapó
tourmaline, but early generations generally have the highest F contents.
References cited in Appendix
Aggarwal, J.K., Mezger, K., Pernicka, E., and Meixner, A., 2004. The effect of
instrumental mass bias on d11B measurements: A comparison between thermal
ionisation mass spectrometry and multiple collector ICP-MS. International
Journal of Mass Spectrometry, 232, 259–263.
Bloodaxe, E. S., Hughes, J. M., Dyar, M. D., Grew, E. S., and Guidotti, C. (1999).
Linking structure and chemistry in the schorl-dravite series. American
Mineralogist, 84, 922-928.
Clark, C. M. (2007). Tourmaline; Structural formula calculations. The Canadian
Mineralogist, 45, 229-237.
Dutrow, B. L., and Henry, D. J. (2000). Complexly zoned fibrous tourmaline, Cruzeiro
Mine, Minas Gerais, Brazil: A record of evolving magmatic and hydrothermal
fluids. The Canadian Mineralogist, 38, 131-143.
20
Dyar, M. D., Taylor, M. E., Lutz, T. M., Francis, C. A., Guidotti, C. V., and Wise, M.
(1998). Inclusive chemical characterization of tourmaline: Mossbauer study of Fe
valence and site occupancy. American Mineralogist, 83, 848-864.
Dyar, M. D., Wiedenbeck, M., Robertson, D., Cross, L. R., Delaney, J. S., Ferguson, K.,
Francis, C. A., Grew, E. S., Guidotti, C. V., Hervig, R. L., Hughes, J. M., Husler,
J., Leeman, W., McGuire, A. V., Rhede, D., Rothe, H., Paul, R. L., Richards, I.,
andYates, M. (2001). Reference minerals for the microanalysis of light elements.
Geostandards and Geoanalytical Research, 25(2-3), 441-463.
Fialin, M., Bezos, A., Wagner, C., Magnien, V., and Humler, E. (2004). Quantitative
electron microprobe analysis of Fe3+/∑Fe: Basic concepts and experimental
protocol for glasses. American Mineralogist, 89(4), 654-662.
Grice, J. D., and Ercit, T. S. (1993). Ordering of Fe and Mg in the tourmaline crystal
structure; the correct formula. Neues Jahrbuch fuer Mineralogie Abhandlungen,
165(3), 245-266.
Hawthorne, F. C. (1996). Structural mechanisms for light-element variations in
tourmaline. The Canadian Mineralogist, 34, 123-132.
Henry, D. J., and Dutrow, B. L. (1996). Metamorphic tourmaline and its petrologic
applications. Reviews in Mineralogy, 33, 503-557.
Hermon, E., Simkin, D. J., Donnay, G., and Muir, W. B. (1973). The distribution of Fe
(super 2+) and Fe (super 3+) in iron-bearing tourmalines; A Mossbauer study.
Tschermak's Mineralogische und Petrographische Meitteilungen, 19(2), 124-132.
Hughes, K. A., Hughes, J. M., and Dyar, M. B. (2001). Chemical and structural evidence
for [4]B <=> [4]Si substitution in natural tourmalines. European Journal of
Mineralogy, 13, 743-747.
Lynch, G., and Ortega, J. (1997). Hydrothermal alteration and tourmaline-albite
equilibria at the Coxheath porphyry Cu-Mo-Au deposit, Nova Scotia. The
Canadian Mineralogist, 35, 79-94.
MacDonald, D. J., and Hawthorne, F. C. (1995). The crystal chemistry of Si <=> Al
substitution in tourmaline. The Canadian Mineralogist, 33, 849-858.
Pouchou, J. L., and Pichoir, F. (1984). A new model for quantitative x-ray microanalysis.
Part I: Applications to the analysis of homogeneous samples. Recherche
Aérospatiale(5), 13-38.
Schreyer, W., Hughes, J. M., Bernhardt, H.-J., Kalt, A., Prowatke, S., and Ertl, A. (2002).
Reexamination of olenite from the type locality: detection of boron in tetrahedral
coordination. European Journal of Mineralogy, 14, 935-942.
Swihart, G. H., and Moore, P. B. (1989). A reconnaissance of the boron isotopic
composition of tourmaline. Geochimica et Cosmochimica Acta, 53, 911-916.
Figure Captions
Fig. A1. Calibration curve for Fe and Copiapó tourmaline graph with formula
Fig. A2. Fe/(Fe+Mg) vs. Al graph. The trend to an intermediate schorl-dravite
composition is most evident in this graph.
21
Fig. A3. Na vs. F graph showing distinct to gradual changes in F content. Early
generations tend to have the highest F contents and either have high Mg, high Al, and/ or
are vacancy-rich.
Fig. A4. Al vs. Ti graph showing an apparent negative correlation between Al and Ti
when Al is less than 6 apfu. There also does not appear to be a correlation between
alteration assemblage and overall Ti concentrations.
Tables
Table A1: Fe3+/Fe total ratios derived from working curves based on work by Fialin et al.
(2004)
Table A2: All tourmaline analyses from this study
Table A3: All framework silicate analyses from this study
Table A4: All sheet silicate analyses from this study
Table A5: All pyroxene analyses from this study
Table A6: All epidote analyses from this study
Table A7: All amphibole analyses from this study
Table A8: All oxide analyses from this study
22
Figure A1
3+
3+ Chilean tourmalines
Relationship
between Fe
and ?Fe
Relationship
between
Fein
and total Fe
1.00
0.90
y = 0.0458x - 0.0528
R 2 = 0.7197
y = 0.0477x - 0.0583
R 2 = 0.7891
0.80
y = 0.0371x + 0.0323
R 2 = 0.6571
0.70
all valid data
C2B
C6B
(Linear (all valid data
(Linear (C2B
(Linear (C6B
F e3+/? Fe
0.60
0.50
C2J
0.40
0.30
0.20
0.10
0.00
0
5
10
15
Fe wt%
20
25
30
Figure A2
Figure A3
Figure A4
AlFe-1
NaAl(CaMg)-1
CaTi(Al)-2
NaAl(□Ti)-1
Table A1. Fe2+/Fetotal ratios derived from working curves using the methods outlined by Fialin et al. (2004)
Sample no.
Fe2+/Fetotal
Cerro Bronce_Estrella
C2B-298
0.6
C2B-708
0.6
Cerro Buitre Radio Tower
C2B-287
0.45
C2B-576c
0.77
C2J-124
0.55
C2J-334
0.65
Cerro Granate
C3B-072a
0.56
C3B-130
0.8
Cerro Negro Norte
C6B-076
0.7
Espanola
C3B-381a
0.84
Falla Ojancos_Transito San Francisco
C6B-101b
0.64
C6B-107
0.81
Jesus Maria
C7B-003a
0.71
Ojancos Viejo
C3B-429.5
0.72
San Gregorio_S Granate
C2B-352e
0.57
C2B-655
0.53
C2B-671
0.55
C2B-808.2
0.39
Santos_PdC
DDH289-037.5
0.75
DDH291-188.4
0.77
DDH384-004.2
0.78
DDH628-094.2
0.64
DDH628-150.6
0.68
DDH628-626.3
0.64
DDH643-595.5
0.68
DDH684-079.8
0.67
ME013-538
0.67
Vinita Azul
C6B-160b
0.72
Table A2. Chemical analyses of tourmalines from Copiapó, Chile
Locality
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Sample
C2B-298
C2B-298
C2B-298
C2B-298
C2B-298
C2B-298
C2B-298
C2B-298
C2B-298
C2B-298
C2B-708
C2B-708
C2B-708
C2B-708
C2B-708
C2B-708
C2B-708
C2B-708
C2B-708
C2B-708
C2B-708
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
Spot no. Analysis no.
1
t1
1
t3
1
t4
1
t5
1
t1
1
t2
1
t3
1
t4
1
t5
1
t6
1
t1
1
t2
1
t3
1
t4
1
t5
1
t6
1
t7
1
t8
2
t1
2
t2
2
t3
1
t1
1
t3
1
t5
1
t6
1
t7
1
t9
1
t10
1
t12
1
t13
1
t14
SiO2
35.51
35.11
35.06
35.41
35.26
36.24
36.75
35.51
35.62
35.71
36.93
36.16
36.43
35.81
36.69
35.92
35.86
35.75
35.83
35.26
35.60
36.91
37.47
35.99
36.24
37.78
36.97
37.01
36.81
36.79
36.69
TiO2
1.52
1.75
2.40
1.22
0.28
0.43
0.38
0.85
2.35
0.55
0.00
0.08
0.02
0.00
0.02
0.02
0.02
0.15
0.00
0.02
0.23
0.12
3.90
0.36
0.52
3.83
0.11
0.12
0.08
0.05
0.27
Al2O3
23.96
21.52
21.63
23.32
22.86
25.26
29.12
23.85
23.79
26.17
31.23
28.23
32.22
27.78
31.44
28.95
27.38
27.91
32.20
29.76
30.16
28.64
29.17
26.60
26.34
29.15
30.53
29.51
29.94
29.23
28.36
B2O3
10.20
10.07
10.01
10.14
10.14
10.37
10.54
10.18
10.26
10.28
10.59
10.37
10.52
10.32
10.56
10.42
10.35
10.24
10.49
10.22
10.44
10.46
10.77
10.33
10.38
10.79
10.58
10.56
10.56
10.54
10.53
Cr2O3
0.01
0.01
0.01
0.01
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.01
0.02
0.00
0.01
0.00
0.01
0.01
Fe2O3
5.33
7.12
6.38
5.95
6.94
4.55
3.01
5.40
5.18
5.83
4.21
5.62
5.09
6.42
4.30
5.87
6.28
5.73
4.47
7.82
5.41
6.62
0.30
8.42
8.75
0.33
5.85
6.41
5.46
6.55
7.43
FeO
7.33
9.79
8.74
8.06
9.52
6.23
4.16
7.46
7.04
8.02
5.77
7.62
6.96
8.74
5.81
7.94
8.59
7.87
6.06
10.72
7.33
4.98
0.23
6.20
6.45
0.24
4.32
4.80
4.12
4.82
5.55
MgO
8.67
7.76
7.96
8.34
7.99
9.77
9.30
8.87
8.94
7.18
6.47
6.30
4.49
5.62
6.25
5.90
6.20
5.84
5.55
1.99
5.75
6.93
11.70
6.66
6.57
11.62
6.85
6.85
7.60
7.13
6.84
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
2
2
2
2
2
2
2
2
2
2
2
t15
t16
t17
t18
t19
t20
t21
t23
t24
t25
t26
t27
t28
t29
t30
t31
t32
t33
t34
t35
t36
t37
t38
t1
t2
t3
t4
t5
t6
t8
t9
t10
t11
t12
36.44
36.53
37.41
37.35
36.98
37.13
36.77
37.19
36.79
37.31
36.19
37.28
37.16
36.53
36.01
36.99
35.80
36.56
36.59
37.41
37.53
37.37
36.72
37.03
36.59
36.86
37.11
36.83
36.65
36.79
36.22
37.06
36.66
36.59
0.16
0.05
3.88
3.93
0.05
3.83
0.08
3.57
0.06
3.82
0.14
0.05
3.80
0.14
0.71
0.02
0.26
0.06
0.11
3.85
3.58
3.25
0.23
2.79
0.06
0.04
0.05
3.94
4.72
0.10
6.22
0.11
0.08
0.07
27.45
30.39
29.16
29.28
30.68
29.29
30.53
28.91
30.21
29.39
27.39
29.83
29.06
29.43
26.03
31.43
25.63
28.57
29.29
28.67
29.20
29.68
29.21
29.18
29.24
30.93
32.04
28.19
27.08
29.97
22.54
31.11
29.37
29.38
10.45
10.51
10.79
10.77
10.61
10.73
10.55
10.70
10.54
10.77
10.43
10.60
10.69
10.52
10.34
10.63
10.28
10.48
10.53
10.75
10.79
10.78
10.56
10.71
10.53
10.63
10.66
10.64
10.59
10.56
10.41
10.62
10.53
10.53
0.01
0.00
0.02
0.02
0.00
0.01
0.00
0.03
0.00
0.01
0.00
0.00
0.02
0.00
0.00
0.01
0.00
0.00
0.00
0.01
0.02
0.03
0.01
0.01
0.00
0.00
0.00
0.02
0.01
0.00
0.02
0.02
0.00
0.00
8.03
6.43
0.32
0.35
5.68
0.31
5.43
0.44
6.30
0.28
8.10
6.30
0.28
6.49
8.66
4.94
8.92
7.04
6.77
0.49
0.39
0.40
6.76
2.61
7.29
5.38
4.63
1.95
2.46
6.56
4.19
5.25
6.86
6.94
5.95
4.74
0.24
0.26
4.24
0.22
4.04
0.33
4.72
0.21
5.97
4.68
0.21
4.86
6.41
3.66
6.71
5.30
5.01
0.37
0.28
0.30
4.99
1.94
5.43
4.05
3.42
1.44
1.87
4.84
3.09
3.90
5.16
5.16
6.84
6.36
11.83
11.62
7.10
11.61
7.17
11.68
6.58
11.66
6.91
6.95
11.58
7.03
6.76
7.32
6.77
7.00
6.96
11.92
11.77
11.58
7.07
10.11
6.49
7.33
7.20
10.50
10.30
6.66
10.71
7.11
6.71
6.75
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-576c
C2B-576c
C2B-576c
C2B-576c
C2B-576c
2
2
2
2
2
2
2
2
2
2
2
2
3
3
3
3
3
3
3
3
3
3
3
3
3
3
3
3
3
1
1
1
1
2
t13
t14
t15
t16
t17
t18
t19
t20
t21
t22
t23
t24
t1
t2
t3
t5
t6
t7
t8
t9
t10
t11
t13
t14
t15
t16
t18
t19
t20
t1
t2
t3
t4
t1
37.05
36.94
37.25
36.55
36.50
36.57
37.64
36.90
37.63
37.00
37.56
36.70
36.96
36.63
37.09
37.59
37.37
37.47
37.47
37.32
37.46
37.09
35.71
37.39
37.36
37.39
36.76
37.29
36.53
35.59
36.83
37.08
36.74
35.72
0.10
4.72
3.84
5.53
0.25
5.47
3.21
0.10
3.23
0.08
3.20
0.06
0.05
0.06
0.09
0.05
4.53
3.39
3.48
0.04
3.39
0.10
1.14
3.65
0.05
3.77
0.11
3.75
0.18
0.40
0.36
0.27
0.22
0.36
31.01
27.30
29.52
24.33
27.78
24.39
29.67
30.01
29.72
29.04
29.98
28.23
31.09
29.23
29.27
31.46
27.77
29.40
29.67
31.65
29.80
30.69
25.26
29.49
31.38
29.27
30.12
27.93
28.73
32.55
34.19
34.04
31.08
33.57
10.64
10.65
10.77
10.49
10.42
10.49
10.78
10.58
10.83
10.58
10.83
10.52
10.63
10.49
10.59
10.72
10.71
10.80
10.82
10.66
10.80
10.63
10.31
10.80
10.66
10.79
10.52
10.68
10.50
10.44
10.75
10.67
10.58
10.49
0.00
0.01
0.02
0.04
0.00
0.02
0.02
0.00
0.01
0.00
0.02
0.00
0.00
0.00
0.00
0.00
0.02
0.01
0.02
0.00
0.01
0.00
0.01
0.02
0.00
0.01
0.01
0.02
0.00
0.00
0.00
0.00
0.00
0.00
5.26
1.19
0.27
2.94
7.63
3.32
0.38
6.44
0.49
6.77
0.38
6.98
5.29
6.67
1.97
5.02
0.67
0.63
0.37
5.04
0.38
5.84
9.02
0.32
5.14
0.30
6.15
1.18
6.94
2.08
1.98
1.81
2.64
2.02
3.88
0.88
0.20
2.17
5.70
2.46
0.28
4.78
0.37
5.12
0.27
5.24
3.99
4.92
8.14
3.77
0.50
0.47
0.28
3.71
0.28
4.31
6.74
0.24
3.89
0.22
4.59
0.89
5.17
6.43
6.12
5.58
7.98
6.09
7.33
11.51
11.60
11.01
6.66
10.71
11.54
6.78
11.67
7.15
11.64
7.44
7.20
6.89
7.64
7.30
11.78
11.66
11.69
6.98
11.58
6.96
6.78
11.74
7.06
11.84
6.62
11.54
7.03
6.00
5.85
5.83
6.08
5.64
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
C2B-576c
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
2
2
1
1
1
1
1
1
1
1
1
1
2
2
2
2
2
2
2
2
2
2
2
2
2
3
3
3
3
3
3
3
3
3
t2
2m
t1
t2
t3
t4
t5
t6
t7
t8
t10
t11
m1
2a
2b
2c
2d
2e
2f
2g
2h
2i
2j
2k
2l
tour2c
tour2b
tour2a
tour2r
tour2q
tour2bq
tour2b1
tour2b2
tour2b3
36.13
35.65
36.45
36.62
35.87
37.26
36.42
35.99
35.69
36.78
37.59
36.14
37.18
36.07
37.49
36.08
35.94
37.20
37.30
37.02
35.46
35.95
37.38
37.19
36.03
36.20
37.33
36.53
36.46
36.02
36.09
35.53
36.11
35.75
0.46
1.85
1.24
0.79
1.19
0.04
0.04
1.25
1.45
0.05
0.02
1.22
0.03
1.12
0.06
1.68
1.58
0.03
0.02
0.02
1.82
1.64
0.03
0.16
1.74
0.76
0.21
0.14
0.46
0.77
0.30
0.91
0.72
0.74
31.85
26.22
27.64
29.17
28.29
34.97
34.63
27.45
26.53
31.52
34.78
27.95
32.79
29.32
32.89
27.47
26.82
32.65
33.18
31.56
25.85
27.12
33.40
32.62
26.69
28.89
32.02
30.18
29.69
27.84
29.87
28.17
28.46
28.43
10.46
10.44
10.52
10.54
10.47
10.83
10.77
10.46
10.40
10.70
10.89
10.48
10.73
10.46
10.75
10.50
10.44
10.73
10.79
10.67
10.42
10.46
10.84
10.91
10.46
10.53
10.73
10.59
10.59
10.50
10.46
10.47
10.48
10.44
0.00
0.01
0.02
0.00
0.01
0.01
0.00
0.01
0.01
0.00
0.01
0.01
0.01
0.01
0.00
0.02
0.01
0.01
0.00
0.00
0.01
0.02
0.00
0.00
0.01
0.01
0.00
0.00
0.01
0.01
0.00
0.01
0.01
0.01
2.07
4.55
4.49
3.42
4.16
1.65
2.01
4.65
5.07
2.97
1.54
4.35
2.19
3.83
1.95
4.08
4.30
1.74
2.01
2.36
4.95
3.93
1.63
2.70
4.41
3.96
2.51
3.67
3.28
4.89
3.63
4.68
4.23
4.29
6.26
5.13
4.97
3.83
4.65
1.84
2.24
5.21
5.59
3.38
1.71
4.80
2.41
4.30
2.21
4.51
4.74
1.93
2.23
2.63
5.57
4.50
1.80
3.05
4.91
4.40
2.79
4.05
3.62
5.41
4.04
5.17
4.69
4.82
6.34
9.34
8.65
8.94
8.65
8.01
8.18
8.51
8.62
8.77
8.44
8.57
8.61
8.09
8.66
9.17
9.20
9.26
8.87
9.22
9.20
9.41
9.30
8.82
9.11
8.79
8.74
8.59
9.29
8.46
8.38
8.51
8.60
8.56
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Granate
Cerro Granate
Cerro Granate
Cerro Granate
Cerro Granate
Cerro Granate
Cerro Granate
Cerro Granate
Cerro Granate
Cerro Granate
Cerro Granate
Cerro Granate
Cerro Granate
Cerro Granate
Cerro Granate
Cerro Negro Norte
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C3B-072a
C3B-072a
C3B-072a
C3B-072a
C3B-072a
C3B-072a
C3B-072a
C3B-072a
C3B-072a
C3B-072a
C3B-072a
C3B-072a
C3B-072a
C3B-072a
C3B-072a
C6B-076
3
3
3
3
3
3
3
3
3
3
1
1
1
2
2
2
2
2
1
1
1
1
1
2
2
2
2
2
2
3
3
3
3
1
tour1a
tour1b
tour1c
tour1ba
tour1bb
tour1bc
tour1bd
tour1bf
tour1a
tour1b
t1
t2
t3
t1
t2
t3
t4
t5
t1
t2
t3
t4
t5
t1
t2
t3
t4
t5
t6
t1
t2
t3
t4
t1
35.94
36.51
35.40
35.97
35.72
37.16
36.34
35.94
36.06
35.95
35.90
36.31
35.79
36.16
35.90
35.70
35.07
37.05
36.04
35.73
35.79
35.39
35.79
36.68
35.56
35.40
35.34
35.19
35.55
36.02
34.76
35.53
35.79
35.48
1.12
0.03
0.14
1.04
0.65
0.00
0.17
0.55
1.54
1.46
0.42
0.29
0.36
0.39
0.68
0.36
0.22
0.40
0.16
0.29
0.20
0.16
0.14
0.05
0.55
0.11
0.22
0.48
0.10
0.10
0.21
0.15
0.03
1.29
26.92
33.41
29.91
28.29
27.51
33.92
28.68
28.33
27.26
26.91
28.13
29.11
28.24
27.53
26.06
28.92
28.72
26.89
29.73
31.05
29.55
28.35
30.69
32.07
27.73
30.09
28.66
27.09
29.22
28.09
20.67
30.57
30.32
24.76
10.41
10.73
10.26
10.53
10.44
10.77
10.55
10.48
10.49
10.42
10.43
10.46
10.44
10.38
10.28
10.38
10.12
10.40
10.41
10.41
10.34
10.24
10.40
10.54
10.27
10.33
10.24
10.18
10.31
10.37
10.00
10.33
10.33
10.36
0.01
0.00
0.01
0.01
0.00
0.01
0.01
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.02
0.00
0.00
0.00
4.70
2.58
3.21
4.39
4.97
1.86
4.29
4.47
4.16
4.19
4.51
4.17
4.53
4.48
4.95
4.21
3.85
4.34
6.62
6.47
7.06
8.69
6.91
6.31
8.15
7.67
7.53
8.53
7.81
3.44
11.80
1.91
2.03
4.17
5.31
2.87
3.61
4.93
5.61
2.10
4.88
4.99
4.65
4.66
7.69
7.00
7.72
7.58
8.30
7.05
6.45
7.31
7.78
7.47
8.10
10.01
8.09
7.38
9.43
9.10
8.66
10.10
9.13
10.99
12.27
12.70
14.08
8.90
8.66
8.20
8.12
8.72
8.45
8.40
8.84
8.64
9.21
9.16
7.14
6.93
7.22
7.26
7.26
6.94
6.58
7.50
4.81
4.14
4.27
3.03
3.83
3.68
4.01
3.24
4.15
3.66
3.61
5.70
5.27
3.64
2.89
8.79
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
2
2
2
2
2
2
2
t3
t4
t5
t6
t7
t8
t9
t10
t11
t13
t14
t16
t17
t18
t19
t20
t21
t22
t23
t24
t25
t26
t27
t28
t29
t30
t31
t1
t2
t3
t4
t5
t6
t7
35.92
36.35
36.11
35.45
35.90
36.13
36.05
36.03
36.43
35.98
35.70
36.45
34.90
36.05
36.61
36.83
36.11
36.25
35.98
35.90
36.12
35.74
35.55
36.22
35.47
35.71
35.46
36.36
35.49
35.96
36.66
36.13
35.74
35.47
0.90
0.51
0.76
0.71
0.80
0.71
0.60
0.79
0.56
0.49
0.92
0.21
0.42
0.43
0.44
0.13
0.35
0.70
0.78
0.52
0.56
0.84
1.67
0.47
0.80
0.99
1.33
0.19
0.60
0.57
0.11
0.49
0.62
1.16
26.21
29.52
25.57
25.47
27.09
28.08
28.54
27.45
27.46
29.76
26.84
30.27
28.12
28.40
30.41
31.43
28.74
28.74
27.83
27.06
29.13
25.86
25.90
29.02
24.95
25.14
25.82
29.62
25.96
27.69
30.87
27.92
25.90
25.07
10.38
10.58
10.44
10.27
10.42
10.50
10.54
10.48
10.57
10.49
10.42
10.60
10.21
10.47
10.59
10.65
10.41
10.47
10.44
10.32
10.48
10.31
10.35
10.48
10.23
10.29
10.26
10.57
10.29
10.42
10.61
10.47
10.37
10.35
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.01
3.69
2.99
3.79
3.60
3.62
3.47
3.44
3.55
3.30
2.83
3.49
2.85
3.28
3.34
2.67
2.15
3.48
3.11
3.38
3.11
2.99
3.60
3.49
3.04
3.68
3.90
3.59
2.82
3.90
3.30
2.65
3.09
4.01
3.74
7.82
6.39
8.10
7.57
7.96
7.41
7.30
7.66
7.13
6.16
7.66
6.20
6.92
7.02
5.68
4.64
7.40
6.57
7.28
6.55
6.48
7.82
7.54
6.51
7.84
8.41
7.65
6.12
8.48
7.16
5.80
6.76
8.70
7.97
8.54
8.15
9.07
9.04
8.08
8.06
8.09
8.25
9.05
7.88
8.57
7.93
7.66
8.10
7.92
8.32
7.20
7.93
8.06
8.72
7.95
8.58
8.70
7.96
8.97
8.48
8.35
8.42
8.15
8.31
7.77
8.65
8.34
9.32
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Española
Española
Española
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C3B-381a
C3B-381a
C3B-381a
2
2
2
2
2
2
2
2
2
3
3
3
3
3
3
3
3
3
4
4
4
4
4
4
4
4
4
4
4
4
4
1
1
1
t8
t9
t9-1
t10
t11
t12
t13
t14
t15
t2
t3
b1
t4
t5
t6
t7
a6
b1
t1
t2
t3
t4
t5
t6
t8
t9
t10
t11
t12
t13
t14
t1
t2a
t2b
36.61
36.12
36.88
36.11
35.43
35.61
35.59
36.61
35.71
35.26
35.35
36.05
36.02
35.85
35.65
35.23
36.25
36.05
35.01
36.71
35.43
36.52
35.96
35.54
36.24
36.00
35.81
35.96
34.58
35.76
36.66
36.04
35.94
36.50
0.13
0.56
0.09
0.43
1.46
1.40
1.42
0.13
0.62
1.48
1.27
0.55
0.85
0.73
1.04
1.31
0.58
0.55
1.15
0.61
1.24
0.39
0.24
1.15
0.25
0.59
0.57
0.73
1.82
0.83
0.43
0.12
1.87
1.66
30.46
27.87
31.27
28.64
24.57
25.17
25.13
31.10
28.13
23.68
24.87
28.94
28.74
27.01
26.45
24.53
29.27
28.94
24.36
29.72
24.85
30.38
29.72
25.09
30.29
28.12
27.67
29.02
22.82
27.75
29.60
28.31
32.52
33.67
10.58
10.47
10.67
10.48
10.33
10.37
10.38
10.64
10.46
10.27
10.34
10.45
10.51
10.46
10.34
10.26
10.56
10.45
10.25
10.70
10.33
10.55
10.46
10.34
10.53
10.43
10.37
10.48
10.05
10.37
10.59
10.39
10.59
10.74
0.01
0.00
0.00
0.01
0.00
0.01
0.01
0.00
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.01
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.02
2.98
3.15
2.19
2.74
4.12
3.85
4.02
2.70
3.72
4.33
4.06
3.32
2.75
3.20
3.43
3.98
3.13
3.28
3.93
2.40
3.84
2.70
3.22
3.61
2.87
3.26
3.65
3.10
5.12
3.42
2.97
3.25
0.75
0.49
6.40
6.82
4.62
5.98
8.85
8.36
8.59
5.87
7.81
9.19
8.60
7.11
5.86
6.92
7.27
8.49
6.57
7.15
8.46
5.05
8.21
5.69
6.81
7.89
6.14
7.04
7.92
6.69
11.21
7.31
6.44
8.47
3.55
2.43
7.45
8.61
8.56
8.81
8.79
8.87
8.71
7.68
7.77
8.91
8.95
7.48
8.80
9.26
8.69
8.86
8.08
7.48
9.24
9.42
9.18
7.75
7.33
9.33
7.68
8.07
7.57
7.91
7.11
7.82
7.99
7.13
8.05
8.50
Española
Española
Española
Española
Española
Española
Española
Española
Española
Española
Española
Española
Española
Española
Española
Española
Española
Española
Española
Española
Española
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C6B-101b
C6B-101b
C6B-101b
C6B-101b
C6B-101b
C6B-101b
C6B-101b
C6B-101b
C6B-101b
C6B-101b
C6B-107
C6B-107
C6B-107
1
1
1
1
2
2
2
2
2
2
2
2
2
3
3
3
3
3
3
3
3
1
1
1
1
1
2
2
2
2
2
1
1
1
t2c
t3a
t3b
t3c
t1a
t1c
t2a
t3a
t3b
t4a
t4b
t4c
t5
t1b
t1c
t2
t2a
t3a
t3c
t3d
t5
t1
t2
t3
t4
t5
t1
t2
t3
t4
t5
t1
t2
t3
36.43
37.12
37.31
37.28
36.64
35.83
35.84
36.30
36.66
37.11
36.69
36.61
36.61
36.89
35.80
36.42
36.25
35.97
36.27
37.36
35.80
36.31
36.46
36.43
35.97
36.14
36.78
36.59
36.69
36.92
36.86
37.84
37.47
37.44
1.91
0.44
0.29
0.51
0.06
0.12
0.09
1.79
2.11
0.73
2.01
2.05
1.21
1.11
0.96
0.11
0.13
1.04
0.18
1.36
0.15
2.99
3.01
2.88
3.02
3.00
2.59
2.90
2.47
2.25
2.53
0.54
1.03
1.39
32.56
33.90
34.22
33.95
30.32
26.91
28.43
32.72
33.03
33.13
32.96
32.69
29.44
34.54
35.01
31.17
31.46
36.29
29.47
33.16
27.87
24.90
25.88
25.29
25.08
25.92
26.46
26.16
27.46
27.59
27.03
31.72
29.65
28.84
10.65
10.72
10.82
10.75
10.48
10.30
10.41
10.66
10.74
10.72
10.75
10.75
10.48
10.80
10.73
10.49
10.47
10.81
10.46
10.69
10.32
10.30
10.42
10.31
10.24
10.40
10.49
10.46
10.52
10.53
10.52
10.81
10.73
10.71
0.01
0.01
0.01
0.01
0.00
0.00
0.00
0.02
0.01
0.01
0.02
0.03
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.01
0.01
0.02
0.05
0.01
0.03
0.15
0.02
0.01
0.01
0.00
0.01
0.01
0.01
0.02
0.45
0.59
0.56
0.49
1.50
4.11
3.72
0.71
0.17
0.40
0.37
0.25
1.74
0.40
1.04
1.88
1.74
0.21
1.95
0.72
3.30
4.08
3.30
3.81
3.73
3.29
3.13
3.20
3.15
3.08
3.09
1.28
1.39
1.54
2.15
2.82
2.82
2.43
7.55
9.96
8.17
3.48
0.83
1.93
1.82
1.19
8.74
1.96
5.10
9.35
8.65
1.02
9.58
3.41
9.91
6.74
5.30
6.28
6.20
5.34
5.11
5.12
5.09
5.01
5.01
5.10
5.55
6.03
9.04
8.18
8.42
8.42
7.07
6.57
7.19
8.19
9.70
9.26
9.24
9.64
6.41
8.57
6.49
5.40
5.61
8.50
6.43
7.55
6.35
8.21
9.23
8.36
8.43
9.22
9.38
9.40
8.86
8.90
9.16
8.22
9.03
9.06
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
C6B-107
C6B-107
C6B-107
C6B-107
C6B-107
C6B-107
C6B-107
C6B-107
C6B-107
C6B-107
C6B-107
C6B-107
C6B-107
C6B-107
C6B-107
C6B-107
C6B-107
C6B-107
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C7B-003a
1
1
1
1
1
1
1
1
2
2
2
2
2
2
2
2
2
2
1
1
1
1
2
2
2
2
2
2
2
3
3
3
3
4
t5
t7
t8
t10
t11
t12
t14
t15
t1
t2
t3
t4
t5
t6
t7
t8
t9
t10
t1
t2
t3
t4
t1
t2
t3
t4
t5
t6
t8
t1
t2
t3
t4
t1
37.91
37.19
37.48
38.16
37.98
38.09
38.38
38.43
38.22
37.71
37.72
38.14
37.69
38.26
37.96
38.70
37.59
38.06
36.30
36.63
36.43
36.49
36.46
38.91
38.13
38.56
38.88
36.16
38.43
36.77
36.45
38.69
39.24
36.02
0.31
1.03
0.45
0.19
0.18
0.38
0.35
0.16
0.14
0.39
0.16
0.17
0.41
0.23
0.52
0.36
0.38
0.18
0.14
0.13
0.13
0.13
0.07
0.03
0.01
0.01
0.03
0.12
0.00
0.12
0.15
0.02
0.01
0.07
31.54
28.78
31.75
31.00
31.95
30.81
31.66
31.60
30.85
30.25
30.15
31.69
29.41
30.93
30.95
31.91
31.94
32.09
36.49
37.04
36.73
37.00
37.02
36.37
34.52
36.15
36.02
36.28
35.83
36.56
36.33
35.69
37.89
36.88
10.87
10.69
10.80
10.85
10.90
10.80
10.86
10.87
10.86
10.75
10.79
10.85
10.75
10.86
10.80
10.92
10.79
10.85
10.76
10.84
10.76
10.77
10.76
11.06
10.91
11.01
11.09
10.73
10.98
10.78
10.71
11.06
11.17
10.72
0.00
0.00
0.01
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.01
0.01
0.01
0.00
0.02
0.01
0.02
0.02
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.02
0.00
0.01
0.01
1.31
1.72
1.22
1.33
1.28
1.46
1.16
1.23
1.47
1.69
1.60
1.34
1.72
1.39
1.28
1.05
1.29
1.24
1.28
1.29
1.28
3.06
3.08
0.70
1.84
1.66
0.87
3.41
0.88
3.31
3.31
0.81
0.20
3.32
5.19
6.67
4.82
5.35
5.03
5.65
4.51
4.82
5.72
6.66
6.47
5.39
6.97
5.34
5.16
4.08
4.97
4.84
9.10
9.02
8.88
7.00
6.97
1.55
4.06
3.72
1.96
7.73
1.96
7.49
7.39
1.84
0.45
7.37
8.73
8.94
8.59
8.86
8.75
8.43
8.75
8.71
8.78
8.16
8.73
8.19
8.60
8.80
8.69
8.92
8.31
8.38
3.25
3.14
3.14
3.08
3.06
7.91
7.06
6.36
8.11
3.06
7.92
2.91
2.94
8.41
8.03
2.88
Jesus Maria
Jesus Maria
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
C7B-003a
C7B-003a
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
4
4
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
2
2
2
2
t2
t3
t1
t2
t3
t4
t5
t6
t7
t8
t9
t10
t11
t12
t13
t14
t15
t16
t17
t18
t19
t20
t21
t22
t23
t24
t25
t26
t27
t28
t1
t2
t3
t4
36.16
36.13
36.75
36.13
36.60
36.54
36.56
36.75
35.90
36.58
36.16
36.67
36.07
36.71
36.90
36.22
36.75
35.30
36.50
36.52
36.33
36.80
36.80
35.98
36.48
36.07
36.45
35.68
36.75
36.28
36.95
35.98
37.10
36.22
0.07
0.08
1.13
1.72
1.18
0.32
0.08
1.13
0.55
0.43
0.40
1.17
0.05
1.20
0.22
0.72
1.05
0.58
1.27
0.53
0.60
1.13
1.15
0.47
1.20
0.07
0.05
0.38
1.15
0.37
1.12
0.32
0.17
0.50
36.95
36.80
29.53
27.57
29.51
31.04
29.36
29.76
27.02
29.76
27.61
29.61
27.83
29.68
31.61
27.83
30.38
23.88
29.23
31.31
30.74
29.97
29.55
27.70
30.02
27.66
29.00
25.68
30.04
26.93
29.87
27.45
31.99
29.25
10.72
10.73
10.58
10.43
10.57
10.60
10.49
10.61
10.36
10.57
10.42
10.56
10.41
10.60
10.63
10.42
10.66
10.22
10.57
10.60
10.50
10.63
10.60
10.42
10.64
10.38
10.51
10.36
10.69
10.46
10.63
10.40
10.68
10.48
0.02
0.01
0.03
0.00
0.03
0.00
0.00
0.01
0.00
0.00
0.00
0.03
0.00
0.03
0.01
0.01
0.03
0.00
0.03
0.00
0.00
0.03
0.03
0.01
0.03
0.00
0.00
0.01
0.03
0.01
0.03
0.00
0.01
0.01
3.29
3.49
2.38
3.07
2.34
2.45
2.91
2.38
3.57
2.87
3.45
2.34
3.67
2.35
2.33
3.28
2.31
5.65
2.45
2.31
2.51
2.23
2.35
3.60
2.35
4.15
3.25
4.41
2.42
3.74
2.31
3.61
2.10
2.97
7.33
7.73
5.56
7.10
5.52
5.80
6.74
5.52
8.34
6.73
8.03
5.45
8.54
5.51
5.44
7.76
5.36
11.57
5.80
5.46
6.00
5.27
5.53
8.47
5.55
9.60
7.68
10.39
5.74
8.80
5.34
8.47
4.96
6.92
2.79
2.63
8.19
7.78
8.29
7.54
7.63
8.21
7.59
7.53
7.59
8.14
7.25
8.22
7.36
7.46
8.21
6.86
8.29
7.44
7.05
8.32
8.26
7.23
8.27
6.43
7.36
7.26
8.26
7.76
8.26
7.40
7.63
7.44
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-655
2
2
2
2
2
2
2
2
2
2
2
2
2
2
2
2
3
3
3
3
3
3
3
3
3
4
4
4
4
4
4
4
4
1
t5
t6
t7
t9
t11
t12
t1
t2
t3
t4
t5
t6
t7
t8
t9
t10
t1
t3
t4
t7
t8
t9
t10
t11
t12
t1
t2
t3
t4
t5
t6
t10
t11
t1
36.84
36.69
37.18
36.82
36.67
36.07
34.92
35.91
35.61
36.07
34.98
35.14
34.98
36.48
34.92
35.00
35.67
36.53
36.59
35.58
36.24
35.53
36.26
35.50
34.47
34.94
35.98
36.13
34.88
35.18
35.13
35.31
35.19
35.09
1.15
0.20
0.18
0.27
1.10
0.03
1.95
1.14
0.06
0.02
2.13
2.20
1.83
0.41
2.23
2.08
0.52
0.17
0.29
1.25
0.83
1.59
0.10
0.33
1.45
2.34
0.02
0.02
2.24
2.04
2.13
2.02
0.02
1.58
29.83
29.80
31.71
29.80
30.14
30.82
24.50
26.19
28.81
29.19
24.10
23.90
24.62
28.71
23.36
23.72
27.01
30.32
29.53
25.83
28.23
24.49
30.42
27.68
24.76
23.45
32.41
32.08
23.12
23.48
22.63
23.48
29.80
23.51
10.59
10.58
10.73
10.52
10.64
10.56
10.17
10.31
10.28
10.38
10.17
10.17
10.14
10.47
10.13
10.13
10.24
10.45
10.46
10.25
10.43
10.23
10.44
10.29
9.99
10.15
10.39
10.40
10.10
10.16
10.09
10.17
10.10
10.17
0.04
0.00
0.00
0.00
0.04
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
2.24
2.77
2.05
2.68
2.32
2.58
7.54
6.57
7.50
7.08
7.45
7.49
7.58
6.10
7.94
7.75
7.38
6.15
5.88
7.48
6.23
7.80
6.45
7.63
7.65
7.82
2.18
1.99
2.12
2.04
2.00
2.10
2.22
8.75
5.28
6.50
4.77
6.26
5.49
6.09
9.20
7.94
9.05
8.73
9.25
9.21
9.08
7.41
9.60
9.32
9.10
7.40
7.07
9.14
7.51
9.41
7.97
9.23
9.34
9.38
14.89
14.46
14.65
14.34
14.45
14.37
15.48
8.95
8.14
7.76
8.17
7.51
8.17
7.78
6.00
6.48
3.92
4.33
6.21
6.21
5.81
6.01
6.10
6.11
4.88
4.66
5.56
5.47
5.95
5.95
4.28
4.65
5.28
6.23
0.91
1.44
6.27
6.40
6.63
6.36
1.48
6.48
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
C2B-655
C2B-655
C2B-655
C2B-655
C2B-655
C2B-655
C2B-655
C2B-655
C2B-655
C2B-655
C2B-655
C2B-655
C2B-655
C2B-655
C2B-655
C2B-655
C2B-655
C2B-655
C2B-671
C2B-671
C2B-671
C2B-671
C2B-671
C2B-671
C2B-671
C2B-671
C2B-671
C2B-671
C2B-671
C2B-671
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
1
1
1
1
1
1
1
2
2
2
2
2
2
2
2
2
2
3
1
1
1
1
1
2
2
2
3
3
3
3
1
1
1
1
t2
t3
t4
t5
t6
t7
t8
t1
t2
t3
t4
t5
t6
t7
t8
t9
t10
t1
t1
t2
t3
t4
t5
t1
t2
t3
t1
t2
t3
t4
t1
t2
t3
t4
36.13
34.76
35.96
35.02
36.58
35.06
34.70
34.51
35.11
35.34
36.01
36.63
36.54
35.28
35.47
35.60
35.96
34.49
35.15
35.86
35.81
34.87
35.83
35.00
35.32
35.66
34.76
35.21
35.56
34.79
34.85
35.05
35.71
35.71
0.05
1.75
0.50
1.78
0.07
1.28
2.07
2.30
0.87
0.32
0.03
0.05
0.03
0.30
0.28
0.48
0.03
2.10
2.60
0.53
0.67
2.39
0.53
2.17
1.47
2.00
0.63
0.62
0.43
2.32
0.15
0.07
0.01
0.05
28.30
23.49
26.04
24.26
30.42
24.13
22.31
22.50
22.41
24.43
28.93
29.08
30.02
23.49
25.77
25.70
27.96
22.01
22.62
25.09
25.15
23.17
25.34
24.00
25.05
25.24
22.48
24.58
25.30
23.41
27.54
29.11
30.92
30.71
10.36
10.10
10.29
10.17
10.53
10.12
10.06
9.99
10.11
10.17
10.33
10.51
10.48
10.15
10.23
10.26
10.33
9.96
10.14
10.23
10.21
10.13
10.24
10.20
10.23
10.31
10.05
10.15
10.19
10.09
10.15
10.21
10.36
10.35
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.03
0.00
0.00
0.01
0.00
0.01
0.01
0.01
0.00
0.00
0.00
0.00
6.43
8.37
6.20
8.13
5.42
8.07
9.02
8.56
9.46
8.30
5.44
5.52
4.74
9.67
8.01
6.56
8.39
9.11
6.94
6.69
7.19
6.90
6.77
6.63
6.41
6.22
9.50
7.65
6.89
6.61
13.06
12.28
10.90
10.75
6.64
8.59
6.38
8.28
5.53
8.22
9.32
8.71
9.61
8.48
5.62
5.67
4.82
9.86
8.19
6.72
8.58
9.30
7.77
7.46
7.92
7.66
7.57
7.37
7.09
6.91
10.54
8.51
7.61
7.38
7.59
7.19
6.34
6.32
6.35
6.65
7.93
6.52
6.52
6.60
6.48
6.45
6.68
6.75
6.88
7.28
7.31
5.97
6.28
7.84
4.53
6.22
8.06
7.49
6.75
7.93
7.26
7.99
7.71
7.76
6.04
6.72
7.15
7.88
2.63
2.28
2.44
2.66
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
1
2
2
2
2
2
2
2
2
t5
t6
t7
t8
t9
t10
t11
t12
t13
t14
t15
t16
t17
t18
t19
t20
t22
t23
t24
t25
t26
t27
t28
t29
t30
t31
t1
t2
t3
t4
t5
t6
t7
t8
35.95
35.56
34.88
34.27
35.07
35.04
35.47
35.26
34.75
35.13
35.59
35.20
35.14
35.81
35.02
34.70
34.43
34.98
34.72
34.45
34.21
35.45
34.91
35.20
35.21
34.82
35.34
35.13
34.82
35.33
35.18
34.88
34.95
35.12
0.04
0.03
0.10
0.02
0.06
0.15
0.15
0.02
0.05
0.13
0.10
0.15
0.47
0.09
1.15
0.03
0.22
0.03
0.16
2.29
0.03
0.11
0.42
0.24
0.20
0.07
1.98
3.75
4.13
2.49
3.09
4.17
3.77
3.85
31.44
30.63
28.53
24.16
29.09
27.08
29.16
29.62
28.36
25.06
28.23
25.81
25.54
28.86
25.91
25.78
23.72
27.95
23.50
23.75
26.57
27.14
24.91
24.99
26.60
29.19
25.55
24.58
22.10
24.06
23.28
22.43
22.15
23.12
10.39
10.32
10.18
9.92
10.23
10.18
10.33
10.27
10.11
10.15
10.33
10.19
10.20
10.37
10.12
9.99
9.97
10.20
10.02
9.97
10.06
10.23
10.12
10.16
10.18
10.17
10.23
10.23
10.13
10.20
10.11
10.11
10.10
10.15
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.01
0.01
0.00
0.00
0.00
0.00
0.01
11.19
11.59
12.76
16.48
12.89
13.35
10.78
11.78
14.40
12.96
10.85
12.21
12.54
10.08
13.01
14.26
16.06
13.81
15.85
14.33
14.99
11.31
13.03
13.00
13.09
13.89
10.94
10.57
11.99
10.97
11.48
11.61
12.34
11.23
6.52
6.80
7.57
9.68
7.59
7.87
6.31
6.90
8.44
7.51
6.31
7.25
7.41
5.85
7.75
8.30
9.26
8.03
9.29
8.45
8.74
6.52
7.69
7.65
7.59
8.02
6.31
6.28
7.09
6.44
6.70
6.74
7.23
6.48
1.82
1.96
2.19
1.51
1.81
2.68
3.80
2.51
0.71
4.49
4.48
4.62
4.44
4.74
3.01
2.22
2.42
1.94
2.63
2.58
1.72
4.45
4.28
4.38
3.25
0.75
5.15
5.34
5.49
5.81
5.30
5.52
5.17
5.53
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
2
2
2
2
2
1
1
1
1
1
1
1
1
1
1
1
1
2
2
2
2
2
2
2
2
2
2
2
2
2
2
2
2
2
t9
t10
t11
t12
t13
t1
t2
t3
t4
t5
t6
t7
t8
t10
t11
t13
t14
t1
t2
t3
t4
t5
t3
t4
t5
t6
t8
t9
t9-1
t11
t12
t13
t14
t15
35.18
35.00
36.32
35.27
35.96
36.80
37.35
37.44
36.11
35.86
36.63
37.35
36.82
36.16
36.80
36.28
36.71
35.94
36.63
37.27
36.20
36.80
35.83
35.90
35.60
36.09
36.09
35.49
36.01
37.12
37.42
35.90
36.86
36.39
3.86
2.45
0.72
3.48
0.99
0.20
0.07
0.12
1.30
0.65
0.17
0.15
0.17
0.12
0.13
0.50
0.30
0.75
0.37
0.05
0.28
0.23
0.75
0.40
1.42
0.48
0.35
0.37
0.55
0.03
0.07
0.07
0.28
0.87
22.49
25.74
29.07
24.63
28.30
30.72
31.80
31.18
27.21
30.46
32.01
32.97
33.92
30.93
30.63
30.91
30.80
29.66
31.82
33.52
31.21
33.78
29.72
30.23
26.15
30.12
29.70
32.80
29.25
32.61
30.55
27.08
34.16
30.02
10.14
10.18
10.47
10.17
10.39
10.58
10.65
10.68
10.43
10.46
10.61
10.76
10.77
10.50
10.56
10.59
10.64
10.45
10.63
10.69
10.55
10.73
10.50
10.43
10.33
10.42
10.41
10.49
10.42
10.61
10.69
10.40
10.72
10.52
0.01
0.00
0.01
0.00
0.00
0.01
0.00
0.00
0.01
0.03
0.03
0.00
0.00
0.00
0.00
0.04
0.04
0.03
0.03
0.00
0.01
0.01
0.03
0.04
0.01
0.03
0.03
0.03
0.01
0.01
0.00
0.01
0.01
0.01
11.29
11.30
9.13
10.51
10.02
2.18
1.94
1.78
3.06
2.26
1.96
1.36
1.27
2.21
2.30
2.53
2.53
2.30
2.01
2.45
2.33
1.43
2.61
2.56
3.19
2.18
2.78
1.99
2.85
2.92
2.11
3.47
1.34
2.29
6.53
6.73
5.27
6.08
5.88
5.90
5.34
4.87
8.61
6.24
5.44
3.75
3.56
6.18
6.35
7.14
7.00
6.25
5.55
6.86
6.31
3.97
7.13
7.09
9.06
5.91
7.57
5.46
7.85
8.12
5.98
9.40
3.75
6.30
5.82
4.29
5.26
5.12
4.72
7.61
7.28
8.24
7.43
7.23
7.26
8.24
8.03
7.31
7.31
6.77
7.03
7.58
7.31
5.21
7.03
7.58
7.33
6.70
7.63
7.43
6.58
6.62
6.70
4.58
8.09
7.53
7.35
7.41
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH289-037.5
DDH291-188.4
DDH291-188.4
DDH291-188.4
DDH291-188.4
DDH291-188.4
DDH291-188.4
DDH291-188.4
DDH291-188.4
DDH291-188.4
DDH291-188.4
DDH384-004.2
DDH384-004.2
DDH384-004.2
DDH384-004.2
DDH384-004.2
DDH384-004.2
DDH384-004.2
DDH628-094.2
DDH628-094.2
DDH628-094.2
DDH628-094.2
DDH628-094.2
DDH628-094.2
DDH628-094.2
DDH628-151.6
DDH628-151.6
DDH628-151.6
3
3
3
3
3
3
3
1
1
1
1
1
1
2
2
2
2
1
1
1
1
2
2
2
1
1
1
2
2
2
2
1
1
1
t2
t3
t4
t5
t6
t8
t9
t1
t2
t3
t4
t5
t6
t2
t3
t5
t7
t1
t2
t3
t4
t1
t2
t3
t1
t2
t3
t1
t2
t3
t4
t1
t2
t3
36.45
36.95
36.93
36.75
36.01
36.39
36.71
36.37
36.07
37.01
36.45
37.14
36.43
36.63
36.58
37.42
36.41
36.33
37.14
36.13
37.12
36.05
36.63
36.69
37.03
35.98
36.56
37.08
36.45
36.26
36.60
36.24
36.37
36.20
0.40
0.08
0.07
0.27
0.97
0.48
0.30
0.28
0.70
0.08
0.57
0.08
0.53
0.60
0.65
0.12
0.57
1.00
0.27
0.95
0.18
1.22
0.37
0.38
0.20
0.80
0.20
0.05
0.22
0.13
0.37
0.08
0.10
0.07
29.53
32.08
32.54
29.42
28.87
31.03
30.40
30.08
27.53
29.59
27.81
30.50
29.10
27.53
28.89
30.53
28.61
29.74
32.27
28.59
32.31
27.79
31.54
31.50
31.01
26.91
30.04
32.29
30.65
29.83
29.89
31.38
31.54
30.44
10.51
10.65
10.67
10.54
10.51
10.58
10.47
10.46
10.32
10.55
10.46
10.67
10.50
10.50
10.46
10.62
10.52
10.44
10.63
10.39
10.69
10.37
10.50
10.56
10.55
10.41
10.54
10.59
10.45
10.43
10.49
10.42
10.47
10.39
0.01
0.00
0.00
0.00
0.03
0.06
0.03
0.07
0.09
0.00
0.09
0.01
0.19
0.03
0.07
0.00
0.12
0.03
0.01
0.00
0.00
0.07
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
2.93
2.42
2.13
2.53
2.50
2.21
3.02
2.57
3.06
2.99
1.50
1.49
1.31
3.28
2.66
2.36
3.07
2.35
1.91
2.60
1.95
2.72
2.14
2.02
4.03
5.35
4.50
4.23
4.65
5.13
4.58
3.57
3.21
3.99
7.92
6.73
5.98
7.09
7.00
6.11
8.39
7.85
9.28
9.03
11.72
9.94
9.62
10.04
8.29
7.45
9.52
7.70
6.13
8.37
6.36
8.90
6.84
6.59
6.46
8.67
7.39
6.93
7.45
8.38
7.42
6.90
6.24
7.78
6.85
6.42
6.75
7.54
7.88
7.31
5.42
6.50
6.62
6.25
6.48
6.37
6.93
6.81
6.85
6.83
6.63
6.55
6.55
6.83
6.81
6.83
6.17
6.73
5.97
6.88
6.20
4.86
5.16
5.07
5.87
5.47
6.12
5.39
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
DDH628-151.6
DDH628-151.6
DDH628-151.6
DDH628-151.6
DDH628-151.6
DDH628-151.6
DDH628-151.6
DDH628-151.6
DDH628-151.6
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH-643-595.5
DDH-643-595.5
1
1
2
2
2
3
3
3
3
1
1
1
1
1
1
1
1
1
1
1
1
1
2
2
2
2
2
2
2
2
2
2
1
1
t5
t6
t1
t2
t3
t1
t2
t3
t4
t1
t2
t6
t8
t9
t10
t11
t14
t15
t16
t17
t18
t24
t5
t6
t7
t8
t9
t10
t11
t13
t14
t16
t1
t2
36.45
36.60
35.60
37.08
36.20
36.13
36.58
36.30
36.39
36.39
35.96
37.23
37.23
36.15
37.01
36.15
37.27
37.12
36.30
36.77
36.48
37.03
37.00
35.26
36.23
36.88
35.25
36.93
36.93
35.95
36.55
37.16
36.45
36.78
0.07
0.15
0.07
0.23
0.65
0.13
0.15
0.15
0.20
0.18
0.36
0.02
0.10
0.15
0.80
0.07
0.35
0.22
0.15
0.17
0.22
0.28
0.61
0.04
0.29
0.34
0.04
0.22
0.33
0.15
0.84
0.29
0.18
0.58
31.46
32.10
29.91
32.31
29.55
30.29
30.86
30.59
30.55
32.60
33.22
31.40
31.92
32.69
30.44
32.92
32.08
32.22
32.68
32.53
33.77
32.11
31.29
35.00
33.26
32.06
34.95
32.75
32.17
32.98
30.75
32.37
31.48
32.35
10.46
10.56
10.29
10.68
10.40
10.31
10.52
10.43
10.49
10.65
10.60
10.66
10.69
10.64
10.62
10.60
10.73
10.71
10.66
10.65
10.71
10.72
10.66
10.52
10.62
10.65
10.54
10.70
10.68
10.59
10.59
10.70
10.52
10.63
0.00
0.00
0.01
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
3.45
3.04
4.64
3.50
4.16
3.75
3.83
3.82
3.35
4.83
5.58
4.78
4.28
5.03
4.55
4.98
3.73
3.91
5.03
4.58
4.94
4.03
4.13
4.92
4.96
3.98
5.15
3.94
3.77
4.72
4.50
3.80
3.73
3.63
6.71
5.83
8.90
6.78
8.09
7.24
7.55
7.48
6.47
7.77
8.93
7.65
6.95
8.12
7.38
8.09
6.06
6.36
8.16
7.42
8.02
6.46
6.71
7.89
8.06
6.47
8.30
6.31
6.13
7.63
7.32
6.17
7.25
7.03
5.65
6.28
4.64
5.70
5.60
5.47
5.70
5.62
6.73
4.57
2.94
5.19
5.53
4.29
5.71
3.93
6.25
5.97
4.32
4.65
3.70
5.96
5.96
2.63
3.69
5.70
2.47
5.56
6.04
4.34
5.61
5.85
5.47
5.22
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Vinita Azul
Vinita Azul
Vinita Azul
Vinita Azul
Vinita Azul
Vinita Azul
DDH-643-595.5
DDH-643-595.5
DDH-643-595.5
DDH-643-595.5
DDH-643-595.5
DDH-643-595.5
DDH-643-595.5
DDH-643-595.5
DDH-643-595.5
DDH-643-595.5
DDH-643-595.5
DDH684-079.8
DDH684-079.8
DDH684-079.8
DDH684-079.8
DDH684-079.8
DDH684-079.8
DDH684-079.8
DDH684-079.8
DDH684-079.8
DDH684-079.8
ME013-538
ME013-538
ME013-538
ME013-538
ME013-538
ME013-538
ME013-538
C6B-160b
C6B-160b
C6B-160b
C6B-160b
C6B-160b
C6B-160b
1
1
1
1
2
2
2
2
2
3
3
1
1
1
2
2
2
2
3
3
3
1
1
1
2
2
2
2
1
1
1
1
1
2
t3
t4
t5
t6
t1
t2
t3
t4
t5
t1
t2
t1
t2
t3
t1
t3
t4
t5
t1
t2
t3
t1
t3
t4
t1
t2
t3
t4
t2
t3
t5
t6
t7
t1
36.82
36.75
36.52
37.16
36.78
36.37
37.01
36.84
36.39
36.67
36.65
37.34
36.51
36.57
36.00
36.86
35.45
36.40
36.57
36.34
36.36
36.90
36.18
36.24
36.69
35.60
36.18
36.09
35.90
37.13
37.14
37.76
36.83
37.43
0.02
0.08
0.27
0.07
0.08
0.52
0.08
0.07
0.18
1.62
0.72
0.43
1.03
0.20
0.69
0.22
0.57
0.69
0.27
0.98
0.39
0.58
0.67
0.53
0.20
0.20
0.08
0.42
0.22
0.12
0.08
0.04
0.12
0.07
30.53
32.65
31.25
32.91
32.18
30.46
32.56
32.61
29.95
30.16
29.85
31.07
29.05
30.65
33.67
30.78
30.37
30.38
28.73
30.16
29.29
31.31
31.95
32.03
33.52
35.54
33.56
33.44
36.40
36.20
35.11
36.44
35.17
36.35
10.56
10.53
10.53
10.66
10.58
10.49
10.61
10.60
10.47
10.61
10.52
10.67
10.57
10.54
10.55
10.54
10.58
10.57
10.56
10.58
10.48
10.64
10.65
10.91
10.68
10.62
10.61
10.61
10.76
10.84
10.84
10.98
10.79
10.87
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.02
0.00
0.06
0.03
0.00
0.01
0.01
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.02
0.01
0.01
0.01
0.01
0.02
4.03
4.03
3.30
3.95
3.06
3.60
2.72
3.70
3.98
4.20
3.63
3.52
1.44
1.37
1.31
3.51
4.10
3.49
3.27
1.33
1.40
3.87
0.00
1.34
3.75
3.96
3.74
3.93
2.00
1.96
2.28
1.89
2.28
2.01
7.78
7.84
6.33
7.65
5.86
6.91
5.26
7.17
7.80
8.18
7.09
6.60
9.97
9.67
8.72
6.47
7.67
6.50
10.74
9.43
9.45
7.14
10.70
9.73
7.00
7.50
6.89
7.38
4.67
4.55
5.48
4.43
5.30
4.68
5.87
4.01
6.42
4.44
6.28
6.28
6.52
4.96
6.04
5.46
6.53
6.48
6.86
6.04
4.32
6.47
6.75
6.99
6.04
6.58
6.93
5.84
5.17
5.27
4.79
3.20
4.79
4.44
5.63
5.61
5.77
5.93
5.69
5.38
Vinita Azul
Vinita Azul
Vinita Azul
Vinita Azul
Vinita Azul
Vinita Azul
C6B-160b
C6B-160b
C6B-160b
C6B-160b
C6B-160b
C6B-160b
2
2
2
2
2
2
t2
t3
t4
t5
t6
t7
37.73
36.64
37.50
37.39
37.75
37.73
0.04
0.04
0.05
0.08
0.09
0.08
37.13
36.39
36.15
36.42
36.94
37.01
10.94
10.85
10.86
10.88
10.96
10.95
0.02
0.01
0.01
0.01
0.01
0.01
1.93
2.08
1.95
2.08
1.94
1.94
4.48
4.85
4.56
4.85
4.49
4.65
5.11
5.66
5.53
5.28
5.33
5.19
MnO
0.03
0.03
0.00
0.05
0.03
0.00
0.00
0.01
0.00
0.00
0.01
0.03
0.00
0.01
0.00
0.01
0.03
0.01
0.01
0.04
0.00
0.00
0.00
0.02
0.02
0.00
0.00
0.00
0.02
0.03
0.03
CaO
2.85
2.81
2.74
2.94
2.88
2.80
1.64
2.73
2.99
1.89
0.49
1.44
0.21
1.12
0.62
1.23
1.61
1.40
0.83
0.34
1.26
0.30
1.53
0.43
0.49
1.54
0.13
0.17
0.16
0.31
0.49
Na2O
1.46
1.33
1.79
1.27
1.39
1.43
1.97
1.48
1.32
1.89
2.44
2.17
2.29
2.31
2.33
2.28
1.97
2.20
2.24
2.45
2.22
2.69
2.17
2.63
2.62
2.23
2.56
2.59
2.56
2.54
2.55
K2O
0.07
0.04
0.04
0.04
0.01
0.01
0.01
0.02
0.02
0.04
0.00
0.02
0.01
0.02
0.02
0.02
0.02
0.02
0.02
0.04
0.05
0.03
0.03
0.02
0.03
0.03
0.01
0.02
0.01
0.01
0.03
H2O
3.00
3.13
2.74
3.04
3.28
3.16
3.17
3.11
2.96
3.06
3.07
2.96
2.92
3.03
3.00
3.05
3.07
2.85
2.93
2.72
2.96
2.94
2.76
3.01
2.98
2.71
3.00
3.02
3.15
3.08
3.05
F
0.07
0.05
0.07
0.15
0.10
0.34
0.11
0.20
0.09
0.14
0.01
0.07
0.04
0.10
0.07
0.01
0.13
0.08
0.03
0.03
0.05
0.04
0.27
0.06
0.07
0.24
0.04
0.01
0.02
0.05
0.00
Cl
0.05
0.01
0.27
0.01
0.01
0.01
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.01
0.01
0.01
0.00
0.00
0.01
0.01
0.01
Subtotal O=F+Cl Total
100.07
-0.04
100.03
100.54
-0.02
100.51
99.86
-0.09
99.77
99.94
-0.07
99.88
100.69
-0.04
100.65
100.60
-0.15
100.45
100.16
-0.05
100.12
99.70
-0.09
99.62
100.57
-0.04
100.54
100.76
-0.06
100.70
101.22
0.00
101.21
101.07
-0.03
101.04
101.19
-0.02
101.18
101.27
-0.04
101.23
101.12
-0.03
101.09
101.63
-0.01
101.63
101.50
-0.05
101.45
100.04
-0.03
100.00
100.68
-0.01
100.66
101.39
-0.01
101.37
101.46
-0.02
101.44
100.73
-0.02
100.72
100.76
-0.11
100.64
100.85
-0.03
100.82
101.63
-0.03
101.60
100.94
-0.10
100.84
101.02
-0.02
101.00
101.42
-0.01
101.42
100.63
-0.01
100.62
101.19
-0.02
101.17
101.94
0.00
101.94
Stuctural formula on the basis of 15 cations
B
Si
B
Al
3.00
6.05
0.00
0.00
3.00
6.06
0.00
0.00
3.00
6.09
0.00
0.00
3.00
6.07
0.00
0.00
3.00
6.04
0.00
0.00
3.00
6.07
0.00
0.00
3.00
6.06
0.00
0.00
3.00
6.07
0.00
0.00
3.00
6.03
0.00
0.00
3.00
6.03
0.00
0.00
3.00
6.06
0.00
0.00
3.00
6.06
0.00
0.00
3.00
6.02
0.00
0.00
3.00
6.03
0.00
0.00
3.00
6.04
0.00
0.00
3.00
5.99
0.00
0.01
3.00
6.02
0.00
0.00
3.00
6.07
0.00
0.00
3.00
5.94
0.00
0.06
3.00
6.00
0.00
0.00
3.00
5.93
0.00
0.07
3.00
6.13
0.00
0.00
3.00
6.04
0.00
0.00
3.00
6.06
0.00
0.00
3.00
6.07
0.00
0.00
3.00
6.09
0.00
0.00
3.00
6.07
0.00
0.00
3.00
6.09
0.00
0.00
3.00
6.06
0.00
0.00
3.00
6.07
0.00
0.00
3.00
6.06
0.00
0.00
Sum
6.05
6.06
6.09
6.07
6.04
6.07
6.06
6.07
6.03
6.03
6.06
6.06
6.02
6.03
6.04
6.00
6.02
6.07
6.00
6.00
6.00
6.13
6.04
6.06
6.07
6.09
6.07
6.09
6.06
6.07
6.06
0.00
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.01
0.00
0.02
0.00
0.00
0.01
0.00
0.01
0.00
0.01
0.02
0.00
0.02
0.01
0.00
0.00
0.01
0.01
0.02
0.00
0.00
0.00
0.00
0.02
0.00
0.01
0.53
0.12
1.57
1.52
0.23
1.54
0.27
1.53
0.11
1.54
0.54
0.23
1.50
0.24
0.81
0.14
0.52
0.36
0.28
1.67
1.43
1.30
0.32
1.04
0.11
0.15
0.18
1.24
1.31
0.16
1.74
0.14
0.12
0.09
2.52
2.66
2.21
2.20
2.44
2.12
2.48
2.14
2.54
2.14
2.61
2.52
2.11
2.70
2.45
2.55
2.61
2.57
2.66
2.07
2.14
2.27
2.60
2.35
2.79
2.63
2.44
2.37
2.26
2.64
2.13
2.52
2.64
2.72
0.02
0.01
0.03
0.03
0.01
0.03
0.01
0.03
0.01
0.03
0.02
0.02
0.02
0.01
0.05
0.00
0.03
0.02
0.02
0.03
0.03
0.02
0.02
0.04
0.02
0.02
0.01
0.04
0.04
0.00
0.04
0.01
0.01
0.02
3.07
2.91
2.73
2.71
3.09
2.73
3.04
2.84
3.03
2.76
3.10
3.05
2.73
3.05
2.97
3.09
3.08
3.11
3.08
2.83
2.83
2.88
3.09
2.94
3.05
3.13
3.06
2.71
2.65
3.02
2.59
3.06
3.09
3.10
0.04
0.10
0.37
0.33
0.03
0.34
0.03
0.17
0.02
0.30
0.03
0.00
0.31
0.05
0.01
0.02
0.04
0.00
0.00
0.23
0.31
0.26
0.02
0.12
0.00
0.00
0.00
0.18
0.12
0.02
0.06
0.00
0.00
0.00
0.00
0.01
0.01
0.01
0.01
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.02
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.00
0.00
0.01
0.00
0.00
0.01
0.00
0.01
0.00
0.00
0.00
101.60
100.89
101.02
100.79
101.19
100.34
100.47
100.08
100.96
100.66
101.51
101.55
99.93
101.12
101.32
100.84
100.84
101.14
101.36
100.62
100.79
100.63
101.66
101.20
101.64
101.19
100.84
100.65
100.75
101.36
100.93
100.97
101.27
101.42
-0.02
-0.04
-0.16
-0.14
-0.01
-0.14
-0.01
-0.07
-0.01
-0.13
-0.01
0.00
-0.13
-0.02
0.00
-0.01
-0.02
0.00
0.00
-0.10
-0.13
-0.11
-0.01
-0.05
0.00
0.00
0.00
-0.08
-0.05
-0.01
-0.03
0.00
0.00
0.00
101.58
100.85
100.86
100.65
101.18
100.19
100.46
100.01
100.95
100.53
101.49
101.54
99.80
101.09
101.31
100.83
100.82
101.13
101.36
100.53
100.66
100.52
101.65
101.15
101.64
101.19
100.84
100.58
100.70
101.35
100.91
100.97
101.27
101.42
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
6.06
6.04
6.03
6.03
6.06
6.02
6.06
6.04
6.07
6.02
6.03
6.11
6.04
6.04
6.05
6.05
6.05
6.06
6.04
6.05
6.05
6.03
6.04
6.01
6.04
6.03
6.05
6.02
6.02
6.06
6.04
6.06
6.05
6.04
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
6.06
6.04
6.03
6.03
6.06
6.02
6.06
6.04
6.07
6.02
6.03
6.11
6.04
6.04
6.05
6.05
6.05
6.06
6.04
6.05
6.05
6.03
6.04
6.01
6.04
6.03
6.05
6.02
6.02
6.06
6.04
6.06
6.05
6.04
0.03
0.00
0.00
0.00
0.01
0.03
0.01
0.01
0.00
0.01
0.00
0.00
0.00
0.02
0.00
0.00
0.00
0.00
0.01
0.02
0.00
0.00
0.01
0.00
0.00
0.01
0.02
0.01
0.01
0.00
0.02
0.00
0.02
0.01
0.15
1.65
1.48
1.81
0.37
1.49
1.40
0.22
1.35
0.25
1.53
0.30
0.15
0.13
0.14
0.16
1.71
1.38
1.38
0.20
1.37
0.20
0.71
1.49
0.22
1.58
0.23
1.73
0.47
0.83
0.70
0.53
0.40
0.66
2.60
2.09
2.15
1.93
2.62
2.11
2.19
2.54
2.21
2.66
2.17
2.62
2.57
2.70
2.59
2.61
2.02
2.30
2.21
2.35
2.28
2.37
2.49
2.17
2.49
2.16
2.72
2.06
2.63
1.85
1.77
1.59
2.39
1.65
0.01
0.04
0.02
0.03
0.01
0.04
0.02
0.01
0.02
0.02
0.03
0.02
0.02
0.01
0.00
0.01
0.03
0.03
0.03
0.00
0.03
0.02
0.04
0.04
0.01
0.03
0.01
0.03
0.02
0.05
0.05
0.04
0.04
0.05
3.07
2.67
2.81
2.64
2.99
2.64
2.81
3.06
2.90
3.12
2.84
3.18
3.08
3.06
3.65
3.05
2.71
2.88
2.88
3.02
2.81
3.09
3.00
2.83
3.02
2.79
2.90
2.80
3.01
3.11
3.15
3.11
3.28
3.14
0.05
0.29
0.22
0.11
0.02
0.16
0.29
0.00
0.26
0.01
0.30
0.06
0.03
0.00
0.00
0.00
0.23
0.25
0.25
0.04
0.33
0.03
0.04
0.28
0.01
0.30
0.04
0.18
0.08
0.11
0.07
0.07
0.05
0.06
0.01
0.00
0.00
0.01
0.01
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.02
0.01
0.00
0.01
0.00
0.01
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.01
101.22
100.56
100.59
100.54
101.04
100.71
100.67
101.45
101.14
101.86
101.19
101.42
101.12
100.90
101.28
101.79
100.58
101.02
101.00
101.08
100.99
101.37
101.38
100.91
101.33
100.88
100.93
100.53
101.37
99.43
101.83
100.61
101.50
99.47
-0.02
-0.12
-0.09
-0.05
-0.01
-0.07
-0.12
0.00
-0.11
-0.01
-0.13
-0.02
-0.01
0.00
0.00
0.00
-0.10
-0.10
-0.11
-0.02
-0.14
-0.01
-0.02
-0.12
0.00
-0.13
-0.02
-0.08
-0.03
-0.05
-0.03
-0.03
-0.02
-0.03
101.20
100.44
100.50
100.49
101.03
100.64
100.55
101.45
101.03
101.85
101.06
101.40
101.11
100.90
101.28
101.79
100.48
100.91
100.90
101.07
100.84
101.36
101.36
100.79
101.33
100.75
100.92
100.45
101.34
99.38
101.80
100.59
101.48
99.44
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
6.05
6.03
6.01
6.05
6.09
6.06
6.07
6.06
6.04
6.08
6.03
6.06
6.04
6.07
6.09
6.09
6.07
6.03
6.02
6.08
6.02
6.06
6.02
6.02
6.09
6.02
6.07
6.07
6.05
5.92
5.96
6.04
6.04
5.92
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.08
0.04
0.00
0.00
0.08
6.05
6.03
6.01
6.05
6.09
6.06
6.07
6.06
6.04
6.08
6.03
6.06
6.04
6.07
6.09
6.09
6.07
6.03
6.02
6.08
6.02
6.06
6.02
6.02
6.09
6.02
6.07
6.07
6.05
6.00
6.00
6.04
6.04
6.00
0.01
0.02
0.01
0.01
0.02
0.05
0.05
0.05
0.00
0.08
0.00
0.02
0.05
0.01
0.04
0.02
0.01
0.03
0.02
0.03
0.02
0.00
0.06
0.48
0.00
0.01
0.03
0.05
0.04
0.03
0.04
0.02
0.03
0.04
0.94
0.26
0.21
0.19
0.21
0.06
0.28
0.26
0.36
0.03
0.00
0.20
0.09
0.09
0.54
0.28
0.20
0.06
0.06
0.13
0.63
0.27
0.03
0.53
0.20
0.20
0.63
0.55
1.27
0.28
0.73
0.24
0.18
0.33
1.72
2.85
2.68
2.89
2.65
1.45
1.80
2.72
2.77
2.84
1.68
2.72
2.16
2.64
2.25
2.75
2.94
2.39
2.37
2.51
2.77
2.74
2.25
2.39
2.74
2.81
2.20
2.57
2.12
2.85
2.49
2.87
2.71
2.55
0.05
0.06
0.06
0.05
0.05
0.02
0.01
0.07
0.07
0.01
0.00
0.05
0.01
0.05
0.00
0.05
0.05
0.01
0.00
0.00
0.07
0.05
0.00
0.03
0.05
0.05
0.10
0.03
0.03
0.07
0.07
0.05
0.05
0.06
3.12
3.31
3.20
3.01
3.27
3.40
3.44
3.22
3.24
3.39
3.47
3.20
3.37
3.10
3.15
3.21
3.17
3.42
3.40
3.43
3.28
3.27
3.51
3.44
3.26
3.24
3.17
3.28
3.21
3.27
3.17
3.35
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0.01
0.04
0.01
0.03
0.00
0.00
0.01
0.01
0.00
0.01
0.03
0.00
0.02
0.00
0.10
0.00
0.01
0.00
0.03
0.01
0.03
0.01
0.00
0.00
0.01
0.01
0.03
0.01
0.03
0.02
0.03
0.02
0.05
0.00
0.35
0.24
1.19
0.27
0.52
1.08
0.52
0.24
0.94
0.85
1.26
1.13
1.40
0.46
0.28
0.58
0.67
1.06
0.34
1.33
0.88
0.98
1.16
1.15
0.98
0.06
0.78
1.11
0.03
0.02
0.01
0.00
0.02
0.01
2.59
1.35
1.97
1.47
2.13
2.10
2.04
1.86
2.00
1.90
1.85
1.91
1.88
2.08
2.05
2.15
2.20
1.97
2.38
1.84
2.10
2.13
1.56
1.58
1.56
1.17
1.51
1.47
1.90
1.88
2.15
2.03
2.19
1.66
0.00
0.02
0.04
0.02
0.01
0.01
0.01
0.01
0.02
0.05
0.04
0.04
0.03
0.03
0.03
0.03
0.03
0.03
0.04
0.04
0.03
0.04
0.07
0.02
0.06
0.02
0.02
0.04
0.01
0.00
0.02
0.00
0.00
0.01
3.16
3.15
3.03
3.19
3.12
3.01
3.13
3.17
3.16
3.01
3.05
3.04
3.46
3.57
2.98
3.15
3.46
3.19
3.64
3.42
3.56
3.00
3.39
3.12
3.01
3.22
3.13
2.97
3.27
3.14
3.19
3.15
3.18
3.15
0.06
0.03
0.00
0.05
0.04
0.05
0.00
0.01
0.06
0.07
0.07
0.05
0.04
0.00
0.43
0.04
0.12
0.05
0.04
0.02
0.03
0.01
0.01
0.03
0.00
0.07
0.00
0.04
0.07
0.07
0.12
0.11
0.06
0.05
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.03
0.02
0.02
0.01
0.01
0.00
0.00
0.07
0.02
0.01
0.01
0.01
0.03
0.01
0.03
0.03
0.05
0.02
0.04
0.01
0.00
0.01
0.01
0.00
0.02
101.78
100.72
100.87
101.88
100.64
100.88
100.46
101.25
100.99
102.80
101.30
102.30
102.30
101.17
101.15
100.78
102.10
101.36
102.67
102.09
100.94
102.48
101.55
102.00
102.30
101.24
101.34
102.01
100.97
101.58
102.30
102.86
101.75
101.76
-0.03
-0.01
0.00
-0.02
-0.02
-0.02
0.00
0.00
-0.03
-0.04
-0.03
-0.03
-0.02
0.00
-0.18
-0.02
-0.06
-0.03
-0.02
-0.01
-0.02
-0.01
-0.01
-0.02
-0.01
-0.04
0.00
-0.03
-0.03
-0.03
-0.05
-0.05
-0.03
-0.03
101.76
100.71
100.86
101.86
100.63
100.86
100.46
101.25
100.96
102.77
101.26
102.27
102.28
101.17
100.98
100.76
102.04
101.33
102.65
102.08
100.92
102.47
101.54
101.98
102.29
101.20
101.34
101.99
100.94
101.55
102.25
102.81
101.73
101.73
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
6.06
6.07
6.03
6.06
6.04
6.03
6.06
6.04
6.04
6.01
6.05
6.08
6.00
6.03
5.93
6.08
5.82
5.99
6.02
5.97
6.03
6.03
5.96
5.95
5.97
5.82
5.93
5.91
5.80
5.95
5.95
5.98
5.93
5.99
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.03
0.09
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.07
0.00
0.18
0.01
0.00
0.03
0.00
0.00
0.01
0.00
0.03
0.18
0.07
0.09
0.20
0.05
0.04
0.02
0.07
0.01
6.06
6.07
6.03
6.06
6.04
6.03
6.06
6.04
6.04
6.01
6.05
6.08
6.00
6.03
6.00
6.08
6.00
6.00
6.02
6.00
6.03
6.03
6.00
6.04
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
0.01
0.01
0.01
0.01
0.00
0.00
0.02
0.02
0.01
0.00
0.00
0.00
1.54
2.11
1.82
1.70
1.57
1.60
0.00
0.00
0.00
0.01
0.01
0.02
3.10
3.21
3.14
3.17
3.16
3.12
0.07
0.08
0.01
0.03
0.05
0.09
0.00
0.00
0.00
0.00
0.00
0.01
102.17
102.01
101.63
101.96
102.35
102.46
-0.03
-0.03
0.00
-0.01
-0.02
-0.04
102.14
101.97
101.63
101.95
102.33
102.42
3.00
3.00
3.00
3.00
3.00
3.00
6.00
5.87
6.00
5.97
5.99
5.99
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.13
0.00
0.03
0.01
0.01
6.00
6.00
6.00
6.00
6.00
6.00
Cr
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
V
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.05
0.01
0.02
0.05
0.01
0.04
0.01
0.00
0.01
3+
Fe
0.68
0.92
0.83
0.77
0.89
0.57
0.37
0.69
0.66
0.74
0.52
0.71
0.63
0.81
0.53
0.74
0.79
0.73
0.56
1.00
0.68
0.83
0.04
1.07
1.10
0.04
0.72
0.79
0.68
0.81
0.92
Mg
0.50
0.70
0.74
0.52
0.49
0.44
0.00
0.50
0.59
0.05
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.36
0.00
0.00
0.37
0.00
0.00
0.00
0.00
0.00
Al
4.81
4.38
4.43
4.71
4.62
4.99
5.63
4.80
4.75
5.21
5.48
5.29
5.37
5.19
5.47
5.26
5.21
5.27
5.44
5.00
5.32
5.17
5.55
4.93
4.88
5.53
5.27
5.17
5.31
5.18
5.07
Sum
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
Al
0.00
0.00
0.00
0.00
0.00
0.00
0.03
0.00
0.00
0.00
0.56
0.28
0.91
0.33
0.63
0.42
0.21
0.32
0.79
0.96
0.52
0.44
0.00
0.35
0.32
0.00
0.64
0.55
0.49
0.50
0.45
Mg
1.70
1.30
1.33
1.61
1.55
2.00
2.29
1.76
1.67
1.76
1.58
1.57
1.11
1.41
1.53
1.47
1.55
1.48
1.37
0.50
1.43
1.72
2.45
1.67
1.64
2.42
1.68
1.68
1.87
1.75
1.68
2+
Fe
1.05
1.41
1.27
1.16
1.36
0.87
0.57
1.07
1.00
1.13
0.79
1.07
0.96
1.23
0.80
1.11
1.21
1.12
0.84
1.52
1.02
0.69
0.03
0.87
0.90
0.03
0.59
0.66
0.57
0.67
0.77
Li
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Sc
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
Cu
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Zn
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Ti
0.19
0.23
0.31
0.16
0.04
0.05
0.05
0.11
0.30
0.07
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.02
0.00
0.00
0.03
0.02
0.47
0.04
0.07
0.46
0.01
0.02
0.01
0.01
0.03
Sum
2.94
2.94
2.91
2.92
2.95
2.93
2.94
2.93
2.97
2.97
2.94
2.94
2.98
2.97
2.96
3.00
2.97
2.93
3.00
2.99
3.00
2.87
2.96
2.95
2.93
2.92
2.93
2.92
2.94
2.93
2.94
Na
0.48
0.45
0.60
0.42
0.46
0.46
0.63
0.49
0.43
0.62
0.78
0.71
0.73
0.75
0.74
0.74
0.64
0.72
0.72
0.81
0.72
0.87
0.68
0.86
0.85
0.69
0.81
0.83
0.82
0.81
0.82
K
0.02
0.01
0.01
0.01
0.00
0.00
0.00
0.01
0.01
0.01
0.00
0.01
0.00
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.01
Ca
0.52
0.52
0.51
0.54
0.53
0.50
0.29
0.50
0.54
0.34
0.09
0.26
0.04
0.20
0.11
0.22
0.29
0.25
0.15
0.06
0.22
0.05
0.26
0.08
0.09
0.27
0.02
0.03
0.03
0.06
0.09
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.05
0.05
0.00
0.05
0.01
0.06
0.00
0.05
0.01
0.00
0.05
0.00
0.01
0.00
0.02
0.00
0.00
0.04
0.05
0.06
0.00
0.04
0.00
0.00
0.00
0.08
0.08
0.00
0.11
0.00
0.00
0.00
1.01
0.80
0.04
0.04
0.70
0.04
0.67
0.05
0.78
0.03
1.02
0.78
0.03
0.81
1.10
0.61
1.13
0.88
0.84
0.06
0.05
0.05
0.84
0.32
0.91
0.66
0.57
0.24
0.30
0.81
0.53
0.65
0.85
0.86
0.00
0.00
0.37
0.34
0.00
0.32
0.00
0.35
0.00
0.32
0.00
0.00
0.34
0.00
0.00
0.00
0.00
0.00
0.00
0.44
0.35
0.25
0.00
0.06
0.00
0.00
0.00
0.26
0.37
0.00
0.92
0.00
0.00
0.00
4.99
5.19
5.54
5.57
5.30
5.59
5.32
5.53
5.22
5.59
4.98
5.22
5.57
5.19
4.89
5.39
4.85
5.12
5.16
5.46
5.54
5.64
5.16
5.58
5.09
5.33
5.43
5.43
5.24
5.18
4.43
5.35
5.15
5.14
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
0.39
0.73
0.00
0.00
0.62
0.00
0.61
0.00
0.66
0.00
0.40
0.54
0.00
0.54
0.26
0.67
0.26
0.47
0.54
0.00
0.00
0.00
0.51
0.00
0.60
0.63
0.73
0.00
0.00
0.63
0.00
0.65
0.57
0.58
1.70
1.57
2.47
2.46
1.73
2.49
1.76
2.48
1.62
2.49
1.72
1.70
2.46
1.73
1.69
1.78
1.71
1.73
1.71
2.43
2.48
2.54
1.73
2.39
1.60
1.79
1.75
2.30
2.14
1.63
1.74
1.73
1.65
1.66
0.83
0.66
0.03
0.03
0.58
0.03
0.56
0.04
0.65
0.03
0.83
0.64
0.03
0.67
0.90
0.50
0.95
0.73
0.69
0.05
0.04
0.04
0.69
0.26
0.75
0.55
0.47
0.20
0.26
0.67
0.43
0.53
0.71
0.71
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.02
0.01
0.47
0.48
0.01
0.47
0.01
0.44
0.01
0.46
0.02
0.01
0.47
0.02
0.09
0.00
0.03
0.01
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0.59
0.43
0.52
0.48
0.48
0.48
0.42
0.59
0.69
0.59
0.52
0.62
0.56
0.61
0.45
0.48
0.62
0.56
0.60
0.49
0.51
0.61
0.61
0.49
0.64
0.48
0.46
0.58
0.56
0.46
0.46
0.45
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
5.57
5.62
5.41
5.57
5.48
5.52
5.52
5.52
5.58
5.40
5.30
5.41
5.47
5.37
5.43
5.38
5.54
5.52
5.38
5.43
5.39
5.50
5.49
5.39
5.38
5.51
5.36
5.51
5.53
5.41
5.43
5.53
5.53
5.55
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
0.60
0.61
0.55
0.63
0.34
0.50
0.49
0.49
0.38
0.80
1.01
0.62
0.65
0.82
0.44
0.92
0.59
0.64
0.82
0.83
0.99
0.64
0.53
1.25
0.96
0.66
1.24
0.76
0.64
0.87
0.51
0.67
0.60
0.68
1.40
1.54
1.17
1.38
1.40
1.37
1.40
1.40
1.66
1.11
0.72
1.26
1.34
1.05
1.39
0.96
1.51
1.44
1.05
1.13
0.89
1.44
1.45
0.65
0.90
1.39
0.61
1.35
1.47
1.06
1.37
1.42
1.35
1.27
0.93
0.80
1.26
0.92
1.13
1.02
1.04
1.04
0.90
1.06
1.22
1.04
0.95
1.11
1.01
1.11
0.82
0.86
1.11
1.01
1.09
0.88
0.91
1.09
1.10
0.88
1.14
0.86
0.84
1.05
1.00
0.84
1.00
0.96
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.01
0.01
0.01
0.01
0.01
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.01
0.00
0.01
0.01
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.02
0.01
0.03
0.08
0.02
0.02
0.02
0.02
0.02
0.04
0.00
0.01
0.02
0.10
0.01
0.04
0.03
0.02
0.02
0.03
0.03
0.07
0.01
0.04
0.04
0.01
0.03
0.04
0.02
0.10
0.04
0.02
0.07
2.94
2.97
2.98
2.96
2.95
2.91
2.95
2.95
2.97
3.01
3.00
2.93
2.95
3.00
2.95
3.00
2.97
2.98
3.00
3.00
3.00
3.00
2.97
3.00
3.00
2.98
3.00
3.00
2.99
3.00
3.01
2.97
2.97
2.99
0.61
0.66
0.73
0.67
0.64
0.74
0.70
0.71
0.71
0.52
0.40
0.66
0.63
0.46
0.61
0.46
0.67
0.64
0.49
0.54
0.50
0.67
0.61
0.40
0.52
0.60
0.38
0.58
0.64
0.47
0.57
0.65
0.58
0.59
0.00
0.00
0.01
0.01
0.01
0.01
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.01
0.01
0.01
0.00
0.01
0.01
0.00
0.01
0.01
0.01
0.01
0.01
0.01
0.10
0.09
0.05
0.08
0.18
0.10
0.07
0.09
0.10
0.18
0.17
0.10
0.11
0.21
0.21
0.18
0.17
0.18
0.19
0.16
0.15
0.17
0.20
0.18
0.17
0.18
0.17
0.18
0.18
0.19
0.22
0.17
0.13
0.15
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.01
0.00
0.01
0.01
0.50
0.50
0.41
0.48
0.38
0.45
0.34
0.46
0.50
0.52
0.45
0.43
0.18
0.17
0.16
0.44
0.51
0.43
0.41
0.16
0.17
0.48
0.00
0.17
0.46
0.49
0.46
0.48
0.24
0.24
0.28
0.23
0.28
0.24
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.19
0.00
0.00
0.00
0.00
0.00
0.02
0.03
0.10
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
5.50
5.50
5.59
5.52
5.62
5.55
5.66
5.54
5.50
5.48
5.55
5.57
5.63
5.83
5.83
5.56
5.49
5.56
5.57
5.80
5.72
5.52
6.00
5.83
5.54
5.51
5.54
5.52
5.75
5.76
5.72
5.77
5.72
5.75
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
0.42
0.85
0.49
0.81
0.61
0.40
0.62
0.76
0.36
0.34
0.26
0.39
0.00
0.13
0.64
0.42
0.22
0.31
0.00
0.00
0.00
0.50
0.20
0.36
0.86
1.17
0.87
0.85
0.98
1.03
0.87
1.00
0.90
1.08
1.44
0.99
1.58
1.08
1.54
1.55
1.59
1.21
1.49
1.33
1.61
1.57
1.49
1.48
1.06
1.59
1.65
1.71
1.46
1.58
1.61
1.42
1.27
1.29
1.16
0.78
1.17
1.08
1.36
1.34
1.38
1.40
1.37
1.28
1.07
1.08
0.87
1.04
0.81
0.96
0.72
0.98
1.08
1.12
0.98
0.90
1.37
1.33
1.20
0.89
1.05
0.89
1.48
1.30
1.31
0.98
1.48
1.33
0.95
1.03
0.94
1.01
0.63
0.61
0.73
0.59
0.71
0.63
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.03
0.01
0.01
0.06
0.01
0.01
0.02
0.20
0.09
0.05
0.13
0.02
0.09
0.03
0.07
0.09
0.03
0.12
0.05
0.07
0.08
0.07
0.02
0.02
0.01
0.05
0.03
0.01
0.01
0.00
0.01
0.01
2.94
2.93
2.97
2.94
2.96
2.97
2.94
2.96
2.96
2.99
2.94
2.92
2.99
2.97
2.99
2.92
3.00
3.00
2.97
3.00
2.97
2.97
3.03
3.05
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
2.99
3.00
0.83
0.43
0.63
0.46
0.68
0.68
0.65
0.59
0.64
0.60
0.59
0.60
0.60
0.66
0.65
0.69
0.70
0.63
0.76
0.59
0.68
0.67
0.50
0.50
0.49
0.37
0.48
0.47
0.59
0.58
0.67
0.62
0.68
0.51
0.00
0.01
0.01
0.01
0.00
0.00
0.00
0.00
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.02
0.01
0.01
0.01
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.06
0.04
0.21
0.05
0.09
0.19
0.09
0.04
0.17
0.15
0.22
0.20
0.25
0.08
0.05
0.10
0.12
0.19
0.06
0.23
0.16
0.17
0.21
0.20
0.17
0.01
0.14
0.19
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.01
0.23
0.25
0.23
0.25
0.23
0.23
0.00
0.00
0.00
0.00
0.00
0.00
5.76
5.74
5.76
5.74
5.76
5.76
6.00
6.00
6.00
6.00
6.00
6.00
1.19
0.99
1.06
1.08
1.13
1.15
1.21
1.35
1.32
1.26
1.26
1.23
0.60
0.65
0.61
0.65
0.60
0.62
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.01
0.01
3.00
3.00
3.00
3.00
3.00
3.00
0.47
0.65
0.56
0.53
0.48
0.49
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
□
0.00
0.03
0.00
0.03
0.01
0.03
0.08
0.00
0.02
0.03
0.14
0.03
0.23
0.04
0.14
0.04
0.06
0.02
0.13
0.12
0.05
0.07
0.05
0.06
0.06
0.03
0.16
0.14
0.15
0.13
0.09
Sum
1.02
1.00
1.12
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
F
0.04
0.03
0.04
0.08
0.05
0.18
0.06
0.11
0.05
0.07
0.01
0.04
0.02
0.05
0.04
0.01
0.07
0.04
0.02
0.02
0.03
0.02
0.14
0.03
0.03
0.12
0.02
0.01
0.01
0.02
0.00
Cl
0.01
0.00
0.08
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
OH
2.83
2.96
2.59
2.87
3.10
2.98
2.99
2.94
2.79
2.89
2.90
2.79
2.75
2.86
2.83
2.88
2.90
2.69
2.77
2.56
2.79
2.77
2.60
2.84
2.82
2.55
2.83
2.85
2.97
2.91
2.87
O
1.12
1.01
1.30
1.05
0.85
0.83
0.95
0.95
1.16
1.03
1.10
1.17
1.23
1.09
1.13
1.11
1.03
1.27
1.22
1.42
1.18
1.21
1.26
1.13
1.15
1.32
1.15
1.14
1.01
1.07
1.12
Total
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.09
0.12
0.03
0.04
0.18
0.06
0.16
0.05
0.16
0.06
0.06
0.16
0.07
0.09
0.05
0.17
0.04
0.11
0.10
0.06
0.08
0.06
0.11
0.07
0.08
0.14
0.20
0.02
0.04
0.13
0.00
0.17
0.13
0.11
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.01
1.00
1.00
1.00
0.02
0.05
0.19
0.17
0.02
0.17
0.01
0.09
0.01
0.15
0.02
0.00
0.16
0.02
0.01
0.01
0.02
0.00
0.00
0.12
0.16
0.13
0.01
0.06
0.00
0.00
0.00
0.09
0.06
0.01
0.03
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
2.90
2.75
2.58
2.56
2.92
2.58
2.87
2.68
2.86
2.61
2.93
2.88
2.58
2.88
2.80
2.92
2.91
2.94
2.91
2.67
2.67
2.72
2.91
2.78
2.87
2.95
2.89
2.56
2.50
2.85
2.45
2.89
2.92
2.93
1.08
1.20
1.23
1.27
1.07
1.24
1.12
1.23
1.13
1.24
1.06
1.12
1.26
1.09
1.19
1.07
1.07
1.06
1.09
1.21
1.17
1.15
1.08
1.16
1.12
1.04
1.11
1.34
1.43
1.14
1.52
1.11
1.08
1.07
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.15
0.04
0.07
0.05
0.08
0.05
0.07
0.15
0.07
0.10
0.06
0.10
0.15
0.11
0.15
0.15
0.06
0.04
0.07
0.22
0.05
0.21
0.05
0.06
0.17
0.05
0.09
0.04
0.07
0.25
0.31
0.40
0.16
0.34
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
0.02
0.15
0.11
0.06
0.01
0.08
0.15
0.00
0.13
0.01
0.15
0.03
0.01
0.00
0.00
0.00
0.12
0.12
0.13
0.02
0.17
0.01
0.02
0.14
0.01
0.15
0.02
0.09
0.04
0.06
0.04
0.03
0.02
0.03
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
2.90
2.52
2.66
2.49
2.82
2.50
2.66
2.89
2.74
2.95
2.68
3.00
2.91
2.89
3.45
2.88
2.56
2.72
2.72
2.85
2.65
2.91
2.83
2.67
2.85
2.64
2.74
2.65
2.84
2.93
2.97
2.93
3.09
2.96
1.07
1.33
1.23
1.45
1.16
1.42
1.19
1.11
1.12
1.05
1.17
0.97
1.08
1.11
0.55
1.12
1.32
1.16
1.15
1.13
1.18
1.07
1.14
1.18
1.15
1.21
1.24
1.26
1.12
1.01
0.99
1.03
0.88
1.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.27
0.02
0.09
0.03
0.10
0.54
0.39
0.06
0.02
0.10
0.48
0.08
0.30
0.12
0.20
0.06
0.00
0.24
0.25
0.19
0.00
0.06
0.29
0.16
0.07
0.05
0.18
0.08
0.10
0.02
0.05
0.02
0.08
0.10
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.02
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
0.02
0.15
0.16
0.27
0.12
0.03
0.01
0.14
0.13
0.02
0.02
0.13
0.01
0.12
0.01
0.16
0.20
0.00
0.00
0.01
0.11
0.16
0.02
0.03
0.15
0.15
0.06
0.02
0.08
0.14
0.01
0.08
0.13
0.08
0.00
0.00
0.00
0.00
0.00
0.04
0.02
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.02
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
2.95
3.12
3.02
2.84
3.09
3.21
3.25
3.04
3.06
3.20
3.27
3.02
3.18
2.93
2.97
3.03
2.99
3.23
3.21
3.23
3.10
3.08
3.31
3.25
3.07
3.06
2.99
3.10
3.03
3.09
2.99
3.16
3.09
3.16
1.04
0.73
0.82
0.88
0.79
0.73
0.72
0.82
0.81
0.77
0.71
0.84
0.80
0.95
1.01
0.81
0.81
0.77
0.79
0.75
0.78
0.75
0.67
0.72
0.77
0.79
0.95
0.88
0.88
0.77
0.99
0.75
0.78
0.76
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.05
0.26
0.12
0.07
0.02
0.42
0.04
0.03
0.02
0.03
0.10
0.09
0.06
0.05
0.03
0.10
0.09
0.03
0.10
0.14
0.07
0.12
0.14
0.41
0.09
0.13
0.11
0.06
0.13
0.17
0.04
0.15
0.17
0.04
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
0.13
0.01
0.02
0.11
0.11
0.00
0.15
0.14
0.18
0.16
0.06
0.06
0.04
0.07
0.05
0.06
0.01
0.06
0.02
0.02
0.01
0.02
0.02
0.01
0.01
0.01
0.01
0.01
0.00
0.02
0.02
0.01
0.03
0.05
0.00
0.00
0.02
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
3.07
3.23
2.94
3.16
3.15
3.25
3.16
3.12
3.02
3.02
2.96
2.79
2.98
2.83
2.83
2.84
2.75
2.74
2.68
2.59
2.62
2.69
2.59
2.79
2.68
2.64
2.66
2.66
2.69
3.38
3.26
3.12
3.18
3.22
0.80
0.76
1.02
0.73
0.74
0.74
0.69
0.74
0.80
0.82
0.98
1.14
0.97
1.11
1.12
1.10
1.24
1.20
1.30
1.39
1.37
1.29
1.40
1.19
1.31
1.35
1.33
1.33
1.30
0.60
0.72
0.88
0.79
0.73
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.03
0.06
0.01
0.00
0.06
0.06
0.05
0.03
0.02
0.31
0.03
0.10
0.01
0.04
0.04
0.13
0.11
0.07
0.02
0.00
0.07
0.00
0.01
0.06
0.02
0.03
0.03
0.08
0.05
0.03
0.14
0.02
0.04
0.01
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.01
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
0.07
0.02
0.05
0.06
0.04
0.03
0.02
0.04
0.06
0.04
0.04
0.03
0.04
0.03
0.03
0.02
0.00
0.04
0.02
0.09
0.02
0.04
0.07
0.03
0.02
0.05
0.04
0.01
0.06
0.06
0.02
0.04
0.12
0.08
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.72
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
3.03
3.07
3.13
3.04
3.16
3.12
3.14
3.12
3.17
2.83
3.12
3.19
2.99
3.13
2.92
3.10
3.14
2.96
3.05
2.91
3.03
2.98
2.98
3.01
3.05
3.05
2.96
3.25
3.16
3.05
3.18
3.12
3.19
3.14
0.91
0.91
0.81
0.90
0.80
0.85
0.83
0.84
0.77
0.41
0.85
0.78
0.96
0.84
1.05
0.88
0.86
0.99
0.92
1.00
0.94
0.99
0.95
0.96
0.92
0.89
1.00
0.74
0.77
0.89
0.80
0.85
0.69
0.78
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.14
0.05
0.14
0.07
0.05
0.01
0.04
0.18
0.07
0.02
0.04
0.04
0.08
0.04
0.02
0.01
0.06
0.04
0.00
0.06
0.02
0.04
0.03
0.04
0.06
0.05
0.09
0.04
0.03
0.05
0.11
0.14
0.17
0.15
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
0.01
0.11
0.00
0.08
0.07
0.09
0.05
0.00
0.04
0.08
0.07
0.00
0.08
0.09
0.10
0.06
0.03
0.00
0.09
0.05
0.10
0.03
0.02
0.10
0.03
0.06
0.03
0.03
0.07
0.03
0.01
0.00
0.05
0.05
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
3.18
3.05
3.21
3.08
3.18
3.12
3.15
3.24
3.18
3.13
3.22
3.03
3.07
3.13
3.02
3.12
3.08
3.03
3.16
3.17
3.14
2.91
2.99
3.14
3.01
3.04
3.16
3.01
3.11
3.02
3.12
3.38
2.86
2.82
0.81
0.84
0.79
0.84
0.74
0.79
0.79
0.76
0.78
0.79
0.70
0.97
0.85
0.77
0.88
0.81
0.89
0.97
0.75
0.78
0.75
1.06
0.99
0.76
0.96
0.90
0.81
0.95
0.82
0.95
0.86
0.61
1.10
1.12
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.13
0.14
0.20
0.14
0.15
0.04
0.12
0.13
0.10
0.10
0.10
0.11
0.11
0.18
0.18
0.25
0.31
0.12
0.14
0.17
0.12
0.03
0.03
0.05
0.07
0.05
0.03
0.05
0.09
0.04
0.06
0.12
0.11
0.07
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
0.06
0.04
0.06
0.08
0.00
0.01
0.00
0.06
0.07
0.08
0.07
0.07
0.02
0.02
0.04
0.01
0.02
0.05
0.00
0.03
0.00
0.03
0.06
0.03
0.05
0.04
0.03
0.05
0.04
0.04
0.04
0.03
0.03
0.03
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.01
0.00
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.02
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
2.78
2.85
2.95
2.77
3.23
3.35
3.39
2.84
2.71
2.82
2.77
2.72
3.02
2.85
2.93
3.25
3.24
2.74
3.38
2.66
3.36
2.85
2.89
2.85
2.85
2.95
2.94
2.93
2.95
2.91
2.94
3.01
3.04
3.05
1.17
1.11
0.98
1.15
0.77
0.64
0.61
1.10
1.21
1.09
1.16
1.21
0.96
1.12
1.02
0.74
0.74
1.21
0.62
1.31
0.62
1.12
1.05
1.12
1.11
1.01
1.03
1.02
1.00
1.05
1.02
0.95
0.93
0.92
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
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4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.18
0.08
0.11
0.20
0.15
0.17
0.20
0.15
0.17
0.09
0.16
0.24
0.06
0.16
0.17
0.12
0.11
0.11
0.66
0.70
0.72
0.72
0.72
0.66
0.60
0.64
0.55
0.62
0.64
0.76
0.72
0.72
0.86
0.71
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
0.01
0.00
0.00
0.01
0.03
0.02
0.00
0.04
0.03
0.03
0.00
0.01
0.01
0.00
0.03
0.02
0.03
0.00
0.18
0.14
0.13
0.13
0.17
0.06
0.03
0.02
0.11
0.19
0.04
0.14
0.16
0.04
0.00
0.16
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.02
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.01
0.00
3.26
3.21
3.09
3.33
3.28
3.18
3.16
3.11
3.34
3.17
3.44
3.29
3.23
3.25
3.13
3.02
3.06
3.05
3.16
3.20
3.19
2.96
2.92
3.18
3.29
3.15
3.15
2.92
3.25
2.96
2.90
3.42
3.32
2.96
0.72
0.78
0.91
0.66
0.69
0.79
0.84
0.83
0.63
0.80
0.56
0.69
0.76
0.75
0.83
0.96
0.91
0.95
0.66
0.66
0.67
0.91
0.91
0.76
0.69
0.83
0.74
0.89
0.70
0.89
0.93
0.54
0.67
0.88
4.00
4.00
4.00
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4.00
4.00
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4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.73
0.72
0.08
0.10
0.10
0.11
0.11
0.07
0.06
0.08
0.05
0.06
0.06
0.07
0.18
0.06
0.10
0.02
0.06
0.08
0.13
0.09
0.08
0.07
0.08
0.04
0.07
0.03
0.10
0.03
0.08
0.07
0.21
0.11
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
0.18
0.20
0.02
0.02
0.04
0.03
0.01
0.02
0.03
0.01
0.05
0.04
0.00
0.03
0.03
0.04
0.04
0.03
0.03
0.02
0.01
0.04
0.06
0.02
0.04
0.02
0.02
0.06
0.02
0.05
0.03
0.04
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2.92
2.92
3.11
2.99
3.14
3.02
3.21
3.12
3.16
3.07
3.12
3.05
3.32
3.10
3.01
3.04
3.14
3.33
3.14
2.92
2.90
3.12
3.10
3.15
3.18
3.27
3.26
3.36
3.22
3.27
3.10
3.17
3.07
3.06
0.90
0.88
0.87
0.99
0.82
0.96
0.78
0.86
0.81
0.92
0.84
0.91
0.68
0.87
0.97
0.92
0.81
0.64
0.83
1.06
1.10
0.84
0.84
0.83
0.78
0.72
0.73
0.57
0.76
0.67
0.87
0.80
0.92
0.92
4.00
4.00
4.00
4.00
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4.00
4.00
4.00
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4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.09
0.11
0.16
0.09
0.10
0.08
0.04
0.06
0.19
0.19
0.04
0.02
0.04
0.10
0.01
0.02
0.10
0.15
0.10
0.06
0.08
0.05
0.16
0.08
0.06
0.04
0.41
0.36
0.04
0.05
0.02
0.02
0.24
0.03
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
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1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
0.06
0.03
0.02
0.02
0.02
0.01
0.07
0.08
0.06
0.00
0.08
0.05
0.08
0.03
0.06
0.04
0.08
0.01
0.02
0.09
0.08
0.08
0.02
0.05
0.07
0.05
0.02
0.02
0.08
0.08
0.06
0.07
0.02
0.18
0.00
0.00
0.00
0.00
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0.00
0.00
0.00
0.03
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0.01
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0.00
0.06
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3.04
3.11
3.12
2.97
3.17
3.29
2.59
2.75
2.68
2.83
2.57
2.55
2.53
2.82
2.54
2.55
2.62
2.65
2.72
2.64
2.69
2.71
2.68
2.67
2.58
2.60
3.10
3.09
3.19
3.21
3.19
3.17
3.00
2.52
0.91
0.86
0.86
1.01
0.81
0.71
1.34
1.16
1.23
1.17
1.34
1.40
1.38
1.15
1.39
1.41
1.30
1.33
1.26
1.27
1.22
1.21
1.29
1.27
1.35
1.35
0.89
0.89
0.73
0.71
0.74
0.76
0.92
1.30
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.09
0.03
0.01
0.04
0.13
0.00
0.01
0.01
0.04
0.04
0.10
0.11
0.07
0.06
0.06
0.02
0.07
0.03
0.03
0.04
0.03
0.03
0.08
0.03
0.02
0.02
0.00
0.03
0.05
0.02
0.14
0.16
0.19
0.22
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
0.03
0.15
0.07
0.14
0.02
0.15
0.11
0.09
0.08
0.06
0.00
0.02
0.02
0.00
0.02
0.07
0.03
0.13
0.04
0.05
0.03
0.05
0.04
0.04
0.05
0.06
0.01
0.01
0.05
0.03
0.06
0.03
0.02
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2.82
2.55
2.74
2.52
2.82
2.46
2.52
2.43
3.01
3.01
2.95
3.03
2.87
3.14
3.00
2.82
2.74
2.45
2.58
2.82
2.75
2.60
2.85
2.67
2.62
2.58
2.99
2.87
2.81
2.56
2.11
2.09
2.15
2.20
1.14
1.30
1.19
1.34
1.15
1.38
1.37
1.48
0.92
0.92
1.05
0.95
1.11
0.85
0.97
1.11
1.23
1.42
1.37
1.12
1.22
1.35
1.11
1.28
1.32
1.36
1.00
1.11
1.14
1.41
1.81
1.86
1.82
1.77
4.00
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4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.21
0.15
0.16
0.11
0.17
0.08
0.12
0.16
0.10
0.04
0.10
0.07
0.07
0.10
0.08
0.13
0.04
0.12
0.03
0.08
0.09
0.07
0.08
0.04
0.08
0.18
0.02
0.05
0.01
0.04
0.04
0.00
0.02
0.03
1.00
1.00
1.00
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1.00
1.00
1.00
1.00
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1.00
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1.00
1.00
1.00
1.00
1.00
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1.00
1.00
1.00
1.00
1.00
0.01
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0.02
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0.00
0.04
0.03
0.00
0.01
0.02
0.04
0.08
0.05
0.01
0.05
0.03
0.00
0.03
0.03
0.01
0.03
0.01
0.03
0.08
0.04
0.00
0.03
0.07
0.08
0.08
0.04
0.05
0.09
0.05
0.00
0.00
0.03
0.01
0.01
0.03
0.01
0.00
0.04
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0.01
0.02
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0.02
0.02
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0.01
0.00
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0.00
0.00
0.00
0.00
0.00
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2.08
2.10
2.10
2.20
2.19
2.09
2.24
2.21
1.81
2.26
2.30
2.26
2.26
2.41
1.98
2.15
2.23
2.12
2.27
1.99
2.14
2.35
2.26
2.21
2.11
2.01
2.20
2.11
2.06
2.22
2.11
2.04
2.02
2.04
1.91
1.90
1.85
1.79
1.80
1.85
1.72
1.78
2.14
1.70
1.64
1.65
1.67
1.58
1.95
1.81
1.77
1.84
1.70
1.99
1.81
1.64
1.70
1.69
1.83
1.97
1.77
1.83
1.86
1.70
1.85
1.91
1.89
1.91
4.00
4.00
4.00
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4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.02
0.05
0.09
0.08
0.09
0.09
0.23
0.20
0.07
0.15
0.15
0.21
0.14
0.15
0.16
0.16
0.14
0.15
0.16
0.45
0.06
0.14
0.09
0.13
0.05
0.12
0.14
0.18
0.13
0.44
0.24
0.06
0.17
0.13
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
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1.00
1.00
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1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
0.04
0.05
0.02
0.02
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0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.01
0.00
0.00
0.01
0.03
0.04
0.02
0.04
0.03
0.00
0.02
0.03
0.03
0.01
0.03
0.03
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0.01
0.01
0.01
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0.00
0.00
0.02
0.00
0.01
0.02
0.01
0.00
0.00
0.00
0.00
0.00
0.00
2.06
2.10
2.43
2.08
2.36
3.01
3.10
3.15
3.09
3.02
3.01
3.10
3.00
3.18
3.16
3.08
3.10
2.95
2.97
3.06
2.93
2.93
3.02
2.96
3.10
2.89
2.91
2.92
2.98
3.05
3.31
3.38
2.87
2.93
1.90
1.85
1.56
1.90
1.64
0.99
0.90
0.85
0.91
0.98
0.98
0.90
0.99
0.81
0.84
0.89
0.87
0.97
0.99
0.91
1.05
1.07
0.96
0.98
0.87
1.10
1.04
1.05
0.99
0.93
0.68
0.61
1.12
1.05
4.00
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4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.16
0.28
0.29
0.17
0.11
0.12
0.21
0.14
0.13
0.22
0.09
0.13
0.12
0.08
0.11
0.18
0.12
0.18
0.28
0.14
0.13
0.12
0.26
0.21
0.18
0.08
0.15
0.28
0.22
0.24
0.16
0.28
0.19
0.21
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
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1.00
1.00
1.00
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1.00
1.00
1.00
1.00
1.00
0.04
0.02
0.01
0.01
0.00
0.01
0.04
0.02
0.03
0.02
0.02
0.00
0.02
0.03
0.03
0.02
0.04
0.02
0.04
0.04
0.01
0.04
0.04
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0.00
0.00
0.00
0.03
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0.01
0.00
0.00
0.00
3.16
3.15
3.19
3.18
3.09
2.98
2.92
3.03
3.06
3.26
3.35
3.36
3.26
3.17
3.01
3.11
3.16
2.94
2.97
2.98
3.01
2.97
2.95
3.02
2.81
3.04
3.01
2.80
2.76
2.99
2.84
2.92
2.91
2.97
0.80
0.83
0.80
0.81
0.91
1.01
1.04
0.95
0.91
0.71
0.62
0.64
0.72
0.79
0.95
0.87
0.80
1.03
0.99
0.97
0.98
0.99
1.01
0.93
1.16
0.93
0.98
1.18
1.20
1.01
1.13
1.06
1.07
1.03
4.00
4.00
4.00
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4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.29
0.25
0.21
0.24
0.17
0.16
0.23
0.20
0.19
0.29
0.43
0.24
0.25
0.33
0.18
0.35
0.15
0.17
0.31
0.29
0.35
0.15
0.19
0.41
0.31
0.21
0.45
0.24
0.17
0.33
0.20
0.17
0.29
0.26
1.00
1.00
1.00
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1.00
0.00
0.01
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0.05
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0.01
0.01
0.01
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0.00
0.01
0.02
0.04
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0.01
0.04
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0.02
0.03
0.01
0.02
0.00
0.00
0.04
0.02
0.02
0.00
0.04
0.03
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.01
0.02
0.00
0.00
0.01
0.01
0.01
0.00
0.00
0.01
0.01
0.01
0.00
0.00
0.02
0.01
0.01
0.02
0.00
0.00
0.00
0.00
0.04
0.01
0.00
2.94
2.97
2.97
2.95
2.83
2.81
3.03
2.95
3.06
2.84
2.78
2.93
2.90
2.86
2.73
2.81
2.79
2.81
2.88
2.76
2.80
2.80
2.77
2.66
2.72
2.78
2.75
2.77
2.79
2.84
2.78
2.69
2.94
2.80
1.06
1.02
1.01
1.04
1.11
1.18
0.97
1.04
0.93
1.13
1.18
1.07
1.09
1.11
1.23
1.16
1.19
1.19
1.10
1.19
1.18
1.18
1.19
1.30
1.26
1.21
1.24
1.19
1.19
1.14
1.21
1.23
1.03
1.18
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.11
0.52
0.15
0.48
0.23
0.13
0.26
0.36
0.19
0.24
0.18
0.19
0.15
0.25
0.29
0.21
0.18
0.18
0.17
0.17
0.16
0.15
0.28
0.29
0.32
0.61
0.38
0.33
0.40
0.41
0.33
0.37
0.31
0.48
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
0.03
0.02
0.00
0.03
0.02
0.03
0.00
0.01
0.03
0.04
0.04
0.03
0.02
0.00
0.22
0.02
0.06
0.03
0.02
0.01
0.02
0.01
0.01
0.02
0.00
0.04
0.00
0.02
0.04
0.04
0.06
0.05
0.03
0.03
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.02
0.01
0.00
0.00
0.00
0.01
0.00
0.01
0.01
0.01
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.01
2.98
2.97
2.86
3.02
2.94
2.85
2.95
2.99
2.98
2.84
2.88
2.87
3.27
3.37
2.81
2.97
3.27
3.01
3.44
3.23
3.36
2.83
3.20
2.94
2.84
3.04
2.95
2.80
3.09
2.96
3.01
2.97
3.00
2.97
0.99
1.02
1.14
0.96
1.04
1.13
1.05
1.00
0.99
1.11
1.08
1.10
0.71
0.63
0.96
1.01
0.65
0.96
0.54
0.76
0.62
1.16
0.79
1.04
1.15
0.91
1.04
1.16
0.87
1.00
0.93
0.97
0.97
0.99
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.52
0.34
0.43
0.47
0.52
0.50
1.00
1.00
1.00
1.00
1.00
1.00
0.03
0.04
0.00
0.01
0.02
0.04
0.00
0.00
0.00
0.00
0.00
0.00
2.93
3.03
2.96
2.99
2.98
2.95
1.04
0.93
1.04
0.99
0.99
1.01
4.00
4.00
4.00
4.00
4.00
4.00
Table A3. Chemical analyses of framework silicates and andalusite from Copiapó, Chile
Locality
Cerro Bronce Estrella
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Sample
C2B-298
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-287
C2B-576c
C2B-576c
C2B-576c
C2B-576c
C2B-576c
C2J-124
C2J-124
C2J-124
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
Spot no.
1
1
1
1
2
2
2
2
2
1
1
2
2
2
1
1
3
1
1
1
1
1
2
2
2
2
2
2
2
3
3
Analysis no.
p1
p1
p2
p3
t7
p1
p2
p3
p5
m1
k1
k1
k1-1
t4
p1
t9
tour2bp
k1
m1
p1
k2
p4
p1
p2
p3
p4
p5
p6
p7
p1
p2
Mineral
Oligoclase
Albite
Albite
Albite
Albite
Albite
Albite
Albite
Albite
K-feldspar
K-feldspar
K-feldspar
K-feldspar
Oligoclase
Albite
Albite
Albite
K-feldspar
K-feldspar
K-feldspar
K-feldspar
Oligoclase
K-feldspar
Andesine
Andesine
Albite
K-feldspar
Albite
K-feldspar
K-feldspar
Oligoclase
SiO2
64.61
68.78
68.44
68.28
68.37
68.18
68.15
68.76
68.84
62.93
63.69
63.89
61.52
59.65
68.41
67.88
68.43
62.21
64.71
64.38
63.46
62.64
62.71
55.28
55.08
53.91
63.31
59.61
64.12
64.38
61.63
TiO2
0.00
0.02
0.01
0.01
0.03
0.00
0.00
0.01
0.01
0.01
0.01
0.11
0.05
0.00
0.00
0.01
0.00
0.05
0.03
0.03
0.01
0.02
0.01
0.06
0.06
0.12
0.02
0.03
0.05
0.04
0.03
Al2O3
20.90
19.95
19.95
20.05
20.11
20.04
19.89
19.92
19.93
18.52
18.76
17.97
19.79
24.81
19.67
20.25
19.81
17.27
19.04
18.79
18.34
23.18
17.91
27.52
27.90
27.95
18.43
25.53
18.65
18.73
24.18
Cr2O3
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.00
0.00
0.01
0.00
0.00
0.00
0.00
Fe2O3
1.07
0.00
0.01
0.03
0.16
0.06
0.05
0.08
0.02
0.13
0.05
0.85
0.43
0.00
0.17
0.24
0.15
0.00
0.05
0.03
0.32
0.15
0.00
0.28
0.37
0.10
0.07
0.07
0.12
0.18
0.10
FeO
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.09
0.00
0.00
0.00
1.74
0.00
0.00
0.27
0.00
0.45
0.12
0.00
0.16
0.00
0.00
0.00
0.00
0.00
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Granate
Cerro Granate
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Española
Española
Española
Española
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Jesus Maria
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C3B-072a
C3B-072a
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C3B-381a
C3B-381a
C3B-381a
C3B-381a
C6B-101b
C6B-101b
C6B-101b
C6B-101b
C7B-003a
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
3
3
3
3
3
2
3
1
1
2
3
3
3
4
4
2
3
3
3
1
1
2
2
3
1
1
1
1
1
2
2
2
2
2
p3
m3
p4
a3
p5
q1
p1
t2
p1
k2
p1
p2
p3
p1
p2
p1
p1
p2
p3
p1
k1
k1
p1
t5
q2
p1
p2
p3
p4
p1
p2
p3
p4
p5
K-feldspar
K-feldspar
Oligoclase
K-feldspar
K-feldspar
Albite
Albite
Albite
Albite
Albite
Albite
Oligoclase
Oligoclase
Oligoclase
Oligoclase
Albite
Albite
Albite
Albite
Albite
K-feldspar
K-feldspar
Albite
Andalusite
Albite
Albite
K-feldspar
Albite
Albite
Albite
Albite
Albite
Albite
Albite
64.13
64.05
61.36
63.72
64.12
69.41
68.35
67.05
65.77
66.89
65.42
61.56
61.31
64.96
61.79
68.17
68.30
67.98
69.40
67.41
64.12
64.46
68.89
36.05
68.59
69.74
64.57
68.31
68.10
68.87
68.16
68.18
67.90
68.48
0.07
0.03
0.02
0.02
0.04
0.00
0.01
0.02
0.02
0.00
0.01
0.00
0.01
0.01
0.01
0.02
0.00
0.01
0.01
0.02
0.00
0.00
0.00
0.02
0.00
0.00
0.00
0.02
0.00
0.02
0.00
0.02
0.00
0.00
19.16
18.56
24.51
18.62
18.56
19.93
19.96
21.08
21.29
20.56
21.76
23.99
24.26
22.06
24.19
20.13
19.92
19.68
20.04
20.29
18.60
18.65
20.37
61.83
20.29
20.24
19.27
20.44
20.63
20.20
20.33
20.44
20.43
20.41
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.12
0.05
0.20
0.05
0.07
0.08
0.15
0.46
0.49
0.00
0.37
0.26
0.29
0.10
0.20
0.28
0.22
0.06
0.10
0.09
0.00
0.01
0.08
2.59
0.11
0.13
0.04
0.10
0.17
0.30
0.13
0.09
0.19
0.11
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.06
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
Ojancos Viejo
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
C3B-429.5
C3B-429.5
C3B-429.5
C3B-429.5
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-352e
C2B-655
C2B-655
C2B-671
C2B-808.2
2
2
2
2
1
1
1
1
1
1
2
2
2
2
2
3
3
3
3
3
3
3
3
3
4
4
4
4
4
4
1
1
1
1
p6
p7
p8
p9
t1
q1
p1
p2
p2
p3
p1
p3
p5
k1
k2
k1
k2
t2
p1
p2
p3
t5
t6
p4
p1
p2
p3
k1
k2
k3
p1
p2
p1
p1
Albite
Albite
Albite
Albite
Albite
Albite
Albite
K-feldspar
Oligoclase
K-feldspar
Albite
K-feldspar
K-feldspar
K-feldspar
K-feldspar
K-feldspar
K-feldspar
K-feldspar
Albite
Albite
Albite
K-feldspar
K-feldspar
Albite
Albite
Albite
Albite
K-feldspar
K-feldspar
K-feldspar
Albite
Albite
Albite
Andesine
68.76
67.88
68.33
68.14
68.82
69.04
67.87
64.16
62.77
64.55
68.21
64.65
64.11
64.04
64.13
64.08
64.12
64.48
68.69
68.37
68.93
64.17
64.07
68.93
68.85
68.56
68.84
64.02
64.32
63.70
68.65
67.39
67.84
59.98
0.02
0.00
0.02
0.00
0.00
0.01
0.02
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.03
0.00
0.00
0.01
0.00
0.01
0.01
0.00
0.01
0.00
0.01
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.05
20.44
20.52
20.33
20.65
20.00
20.12
20.18
18.57
23.83
18.62
20.48
18.68
18.62
18.64
18.65
18.71
18.40
18.66
20.08
20.24
19.90
18.56
18.56
19.99
19.96
19.99
19.99
18.43
18.70
18.79
19.80
19.97
19.93
25.44
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.00
0.01
0.11
0.14
0.30
0.27
0.07
0.04
0.06
0.07
0.00
0.08
0.07
0.08
0.04
0.07
0.40
0.04
0.11
0.32
0.23
0.23
0.22
0.26
0.25
0.02
0.08
0.04
0.17
0.08
0.07
0.15
0.29
0.07
0.04
0.21
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
DDH289-037.5a
DDH289-037.5a
DDH384-004.2
DDH384-004.2
DDH628-094.2
DDH628-151.6
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH643-595.5
DDH684-079.8
DDH684-079.8
ME013-538
ME013-538
ME013-538
2
2
2
3
3
3
3
3
1
2
1
1
1
1
1
1
1
1
1
1
1
1
1
1
2
2
2
2
2
2
3
1
1
2
p1
p2
p3
p1
k1
k2
p1
p2
k1
k1
k1
k1
k1
p1
p2
sc1
sc2
sc3
sc4
sc5
sc6
sc1
sc2
sc3
t1
t2
t3
t4
m1
t2
k1
k1
p1
p1
Andesine
Andesine
K-feldspar
Andesine
K-feldspar
K-feldspar
Albite
Albite
K-feldspar
K-feldspar
K-feldspar
K-feldspar
K-feldspar
K-feldspar
K-feldspar
K-feldspar
K-feldspar
K-feldspar
K-feldspar
K-feldspar
K-feldspar
Scapolite
Scapolite
Scapolite
Andesine
K-feldspar
K-feldspar
Oligoclase
K-feldspar
K-feldspar
K-feldspar
K-feldspar
Andesine
Albite
60.45
59.68
64.83
60.01
64.03
65.03
69.19
69.64
63.30
63.88
64.18
63.67
63.79
65.44
66.32
65.82
65.71
66.19
65.82
65.13
65.65
57.02
56.73
56.95
59.15
62.72
64.14
64.19
63.77
63.20
63.58
64.05
58.68
68.42
0.05
0.03
0.07
0.04
0.00
0.00
0.00
0.02
0.00
0.00
0.00
0.02
0.00
0.00
0.00
0.00
0.01
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.01
0.01
0.01
0.00
0.00
0.02
0.00
0.02
0.00
25.34
25.85
19.27
25.25
18.80
18.82
20.01
20.16
18.46
18.55
18.57
18.37
18.44
19.02
18.61
18.87
18.74
19.27
18.77
18.89
18.74
22.12
22.29
22.21
26.92
19.42
19.88
23.73
18.48
18.59
18.48
18.74
26.23
20.29
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.23
0.21
0.05
0.22
0.08
0.11
0.11
0.24
0.07
0.07
0.30
0.24
0.00
0.57
0.46
0.16
0.23
0.47
0.27
0.13
0.24
0.00
0.00
0.00
0.28
1.17
0.39
0.32
0.13
0.14
0.26
0.10
0.19
0.24
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.10
0.03
0.12
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Vinita Azul
Vinita Azul
Vinita Azul
Vinita Azul
Vinita Azul
Vinita Azul
C6B-160b
C6B-160b
C6B-160b
C6B-160b
C6B-160b
C6B-160b
1
1
2
2
2
2
a1
a3
a1
a2
a3
a4
Andalusite
Andalusite
Andalusite
Andalusite
Andalusite
Andalusite
35.25
35.77
36.10
36.23
36.04
35.69
0.02
0.02
0.00
0.00
0.01
0.01
64.81
64.42
64.11
63.81
64.19
64.55
0.00
0.01
0.01
0.00
0.00
0.01
0.68
0.65
0.63
0.79
0.91
0.63
0.00
0.00
0.00
0.00
0.00
0.00
MgO
0.10
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.15
0.09
0.00
0.00
0.21
0.01
1.33
0.00
0.01
0.26
0.01
0.25
0.02
0.01
0.02
0.00
0.01
0.00
0.01
0.00
MnO
0.00
0.01
0.01
0.01
0.17
0.02
0.00
0.00
0.00
0.00
0.01
0.02
0.02
0.00
0.09
0.01
0.01
0.06
0.01
0.00
0.02
0.02
0.00
0.02
0.00
0.01
0.00
0.00
0.02
0.00
0.01
CaO
2.20
0.14
0.09
0.09
0.17
0.21
0.03
0.11
0.03
0.00
0.00
0.01
0.00
6.15
0.16
0.09
0.22
1.20
0.12
0.03
0.34
4.45
0.27
9.59
9.86
10.18
0.01
6.86
0.01
0.03
5.48
Na2O
10.22
11.67
11.55
11.78
11.59
11.70
11.57
11.60
11.64
1.01
1.21
0.80
1.11
8.25
10.57
10.24
10.28
0.82
2.38
1.30
0.97
8.73
1.02
6.12
5.92
5.68
0.77
7.75
1.06
1.12
8.21
K2O
0.14
0.05
0.04
0.03
0.04
0.07
0.03
0.05
0.05
15.29
15.12
14.83
14.65
0.19
0.10
0.06
0.05
13.83
12.96
14.69
14.78
0.12
14.66
0.15
0.14
0.17
15.48
0.09
14.98
14.93
0.13
F
0.04
0.00
0.03
0.01
0.03
0.01
0.03
0.01
0.02
0.03
0.00
0.02
0.05
0.02
0.00
0.04
0.06
0.08
0.04
0.00
0.00
0.00
0.04
0.00
0.00
0.03
0.03
0.00
0.01
0.00
0.02
Cl
0.08
0.07
0.00
0.05
0.02
0.08
0.00
0.02
0.00
0.02
0.00
0.01
0.00
0.00
1.14
0.03
0.27
0.01
0.25
0.02
0.00
0.02
0.01
0.07
0.03
0.03
0.04
0.03
0.00
0.01
0.01
Subtotal O=F+Cl Total
99.36
-0.03
99.32
100.71
-0.02
100.70
100.14
-0.01
100.13
100.33
-0.01
100.32
100.71
-0.02
100.69
100.38
-0.02
100.36
99.75
-0.01
99.73
100.58
-0.01
100.57
100.56
-0.01
100.55
97.94
-0.02
97.92
98.86
0.00
98.86
98.65
-0.01
98.64
97.71
-0.02
97.69
99.17
-0.01
99.16
100.34
-0.26
100.08
99.09
-0.02
99.07
99.31
-0.09
99.22
98.61
-0.03
98.58
99.59
-0.07
99.52
99.29
0.00
99.29
98.81
0.00
98.81
99.37
0.00
99.37
97.33
-0.02
97.31
99.26
-0.02
99.25
99.37
-0.01
99.36
98.38
-0.02
98.36
98.16
-0.02
98.14
99.98
-0.01
99.97
99.04
0.00
99.04
99.44
0.00
99.44
99.79
-0.01
99.78
Si
2.87
2.98
2.98
2.98
3.98
2.97
2.97
2.97
3.99
2.97
2.97
2.98
2.89
2.68
2.98
2.95
2.98
2.96
2.97
2.97
2.97
2.78
2.98
2.51
2.50
2.47
2.98
2.66
2.97
2.97
2.73
3+
Fe
0.04
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.03
0.02
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.01
0.00
Al
1.09
1.02
1.02
1.02
0.02
1.03
1.03
1.02
0.01
1.03
1.03
0.99
1.10
1.32
1.01
1.04
1.02
1.04
1.03
1.02
1.02
1.21
1.02
1.48
1.49
1.52
1.02
1.34
1.02
1.02
1.26
Sum
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
Na
0.88
0.05
0.98
0.97
0.00
0.97
0.99
0.98
0.00
0.09
0.11
0.07
0.10
0.72
0.89
0.86
0.87
0.08
0.21
0.12
0.09
0.75
0.09
0.54
0.52
0.51
0.07
0.67
0.10
0.10
0.71
K
0.01
0.90
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.92
0.90
0.88
0.88
0.01
0.01
0.00
0.00
0.84
0.76
0.87
0.88
0.01
0.89
0.01
0.01
0.01
0.93
0.01
0.89
0.88
0.01
0.00
0.01
0.01
0.00
0.00
0.00
0.01
0.03
0.06
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.02
0.00
0.00
0.00
0.00
0.00
0.02
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.03
0.00
0.00
0.02
0.01
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.42
0.03
5.62
0.02
0.01
0.02
0.24
1.01
1.76
1.07
2.02
5.11
5.24
2.47
5.14
0.18
0.13
0.14
0.11
0.63
0.00
0.00
0.52
0.01
0.35
0.25
0.04
0.41
0.48
0.18
0.39
0.36
0.41
0.38
1.78
0.97
8.35
0.75
1.26
11.10
11.74
10.89
10.36
10.55
10.18
8.62
8.61
10.26
8.78
8.48
11.05
10.41
10.53
11.11
0.38
0.32
10.54
0.00
9.85
10.55
4.10
11.04
10.69
10.89
9.87
9.76
10.06
10.12
13.71
15.22
0.14
15.39
14.80
0.07
0.07
0.05
0.08
1.22
0.21
0.29
0.24
0.10
0.18
0.31
0.08
0.09
0.07
0.26
16.22
16.31
0.48
0.01
0.29
0.12
11.14
0.14
0.16
0.08
0.35
0.35
0.31
0.29
0.05
0.03
0.04
0.00
0.03
0.03
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.04
0.00
0.02
0.06
0.04
0.00
0.05
0.02
0.02
0.03
0.00
0.00
0.00
0.00
0.02
0.01
0.00
0.00
0.07
0.00
0.04
0.01
0.00
0.02
0.01
0.02
0.02
0.02
0.00
0.00
0.00
0.00
0.07
0.05
0.15
0.08
0.00
0.00
0.00
0.00
0.01
0.00
0.02
0.01
0.02
0.00
0.05
0.00
0.00
0.00
0.00
99.47
99.04
100.30
98.61
98.94
100.67
100.56
100.61
99.86
100.39
100.02
99.85
99.98
99.97
100.29
97.67
99.75
98.59
100.36
99.84
99.42
99.81
100.88
100.58
99.52
101.08
99.23
100.48
100.22
100.60
99.24
99.22
99.31
99.82
-0.02
-0.03
-0.02
-0.01
-0.02
-0.01
0.00
0.00
0.00
-0.01
0.00
0.00
0.00
0.00
0.00
-0.02
-0.01
-0.05
-0.02
-0.01
-0.02
-0.02
0.00
-0.02
-0.01
-0.01
-0.01
0.00
0.00
-0.01
0.00
-0.01
0.00
0.00
99.45
99.02
100.29
98.60
98.92
100.65
100.56
100.60
99.86
100.38
100.01
99.85
99.98
99.96
100.29
97.65
99.74
98.53
100.34
99.83
99.40
99.79
100.88
100.55
99.51
101.06
99.22
100.48
100.22
100.59
99.24
99.21
99.31
99.82
2.95
2.98
2.71
2.97
2.98
2.99
2.97
2.91
2.88
2.93
2.86
2.73
2.72
2.85
2.73
2.96
2.97
2.98
2.98
2.95
2.98
2.98
2.96
0.98
2.96
2.98
2.96
2.95
2.94
2.96
2.96
2.95
2.95
2.96
0.00
0.00
0.01
0.00
0.00
0.00
0.01
0.02
0.02
0.00
0.01
0.01
0.01
0.00
0.01
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.05
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.01
0.00
1.04
1.02
1.28
1.03
1.02
1.01
1.02
1.08
1.10
1.07
1.12
1.26
1.27
1.14
1.26
1.03
1.02
1.02
1.01
1.05
1.02
1.02
1.03
1.97
1.03
1.02
1.04
1.04
1.05
1.03
1.04
1.04
1.05
1.04
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
3.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.16
0.09
0.72
0.07
0.11
0.93
0.99
0.92
0.88
0.90
0.86
0.74
0.74
0.87
0.75
0.71
0.93
0.89
0.88
0.94
0.03
0.03
0.88
0.00
0.83
0.87
0.36
0.93
0.90
0.91
0.83
0.82
0.85
0.85
0.81
0.90
0.01
0.92
0.88
0.00
0.00
0.00
0.00
0.07
0.01
0.02
0.01
0.01
0.01
0.02
0.00
0.00
0.00
0.01
0.96
0.96
0.03
0.00
0.02
0.01
0.65
0.01
0.01
0.00
0.02
0.02
0.02
0.02
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.02
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.03
0.01
0.02
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.02
0.00
0.00
0.00
0.02
0.01
0.02
0.01
0.02
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.01
0.01
0.00
0.39
0.38
0.32
0.64
0.17
0.17
0.45
0.00
4.57
0.03
0.63
0.00
0.01
0.00
0.02
0.11
0.07
0.00
0.15
0.44
0.14
0.00
0.00
0.05
0.23
0.19
0.09
0.00
0.00
0.02
0.03
0.42
0.34
6.72
10.10
10.00
10.29
10.23
11.43
11.78
10.96
0.69
9.00
0.62
11.19
0.67
0.25
0.34
0.24
0.50
0.38
0.20
11.66
11.43
11.62
0.18
0.16
11.85
11.32
11.47
11.56
0.23
0.45
0.34
11.59
11.53
11.47
7.55
0.34
0.34
0.19
0.27
0.14
0.21
0.18
15.70
0.06
15.65
0.06
15.59
16.32
16.14
16.24
15.62
15.58
16.38
0.06
0.06
0.04
16.31
16.31
0.04
0.06
0.07
0.07
16.30
16.12
16.13
0.05
0.10
0.07
0.42
0.01
0.01
0.00
0.04
0.01
0.03
0.00
0.00
0.00
0.02
0.03
0.05
0.01
0.00
0.03
0.00
0.02
0.05
0.02
0.01
0.01
0.00
0.01
0.00
0.00
0.04
0.02
0.03
0.01
0.00
0.05
0.01
0.03
0.00
0.00
0.00
0.00
0.01
0.04
0.00
0.01
0.02
0.02
0.06
0.02
0.01
0.06
0.00
0.02
0.26
0.35
0.00
0.01
0.00
0.00
0.01
0.01
0.00
0.03
0.00
0.01
0.02
0.16
0.10
0.01
0.04
0.02
0.00
100.17
99.28
99.79
100.25
100.71
101.44
99.75
99.25
100.28
99.65
100.72
99.74
99.44
99.26
99.80
99.35
99.05
100.13
100.89
100.82
100.90
99.53
99.43
100.91
100.58
100.37
100.77
99.15
99.85
99.25
100.47
99.55
99.76
100.38
0.00
0.00
0.00
-0.02
-0.01
-0.01
0.00
0.00
0.00
-0.02
-0.02
-0.02
-0.02
0.00
-0.02
-0.06
-0.09
-0.02
-0.01
-0.01
-0.01
0.00
-0.01
0.00
-0.01
-0.02
-0.01
-0.02
-0.04
-0.02
-0.02
-0.01
-0.02
0.00
100.17
99.28
99.79
100.23
100.70
101.43
99.75
99.24
100.28
99.63
100.70
99.72
99.42
99.26
99.78
99.30
98.96
100.11
100.88
100.81
100.90
99.53
99.42
100.91
100.57
100.36
100.76
99.13
99.81
99.22
100.45
99.54
99.74
100.38
2.96
2.95
2.95
2.94
2.98
2.98
2.96
2.98
2.76
2.98
2.95
2.98
2.98
2.98
2.97
2.97
2.99
2.97
2.97
2.96
2.98
2.98
2.97
2.98
2.98
2.98
2.98
2.98
2.98
2.96
2.98
2.96
2.97
2.66
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.01
0.01
0.01
0.01
0.01
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.01
0.00
0.00
0.01
1.04
1.05
1.04
1.05
1.02
1.02
1.04
1.02
1.24
1.01
1.05
1.02
1.02
1.02
1.02
1.02
1.01
1.02
1.02
1.03
1.01
1.01
1.02
1.02
1.02
1.02
1.02
1.01
1.02
1.03
1.01
1.04
1.03
1.33
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.84
0.84
0.86
0.86
0.96
0.98
0.93
0.06
0.77
0.06
0.94
0.06
0.02
0.03
0.02
0.05
0.03
0.02
0.98
0.96
0.97
0.02
0.01
0.99
0.95
0.97
0.97
0.02
0.04
0.03
0.98
0.98
0.97
0.65
0.02
0.02
0.01
0.01
0.01
0.01
0.01
0.93
0.00
0.92
0.00
0.92
0.97
0.96
0.96
0.93
0.93
0.96
0.00
0.00
0.00
0.96
0.97
0.00
0.00
0.00
0.00
0.97
0.95
0.96
0.00
0.01
0.00
0.02
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.02
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.59
0.11
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.02
0.03
0.02
0.00
0.03
0.01
0.00
0.00
0.00
0.00
0.00
0.02
0.01
0.03
0.02
0.00
0.03
0.00
0.00
0.01
0.01
0.00
0.03
0.01
0.00
0.00
0.00
0.02
0.01
0.00
0.01
6.35
6.91
0.25
6.62
0.25
0.04
0.27
0.28
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.05
0.00
0.00
0.00
5.68
6.02
5.86
7.74
0.10
0.40
4.26
0.00
0.06
0.06
0.00
7.35
0.63
7.89
7.79
2.41
7.68
1.06
0.56
10.93
10.99
0.26
0.24
0.13
0.57
0.77
0.58
0.39
0.36
0.31
0.72
0.34
0.67
0.67
10.32
9.86
9.98
7.04
0.46
0.98
9.18
0.30
0.30
0.33
0.88
6.71
11.16
0.36
0.30
12.82
0.44
14.49
15.43
0.08
0.10
16.45
16.43
16.59
15.94
15.54
15.90
15.91
16.08
16.09
15.66
16.14
15.73
15.60
1.22
1.23
1.33
0.62
15.04
14.24
0.20
16.30
15.20
16.00
15.18
1.43
0.14
0.00
0.00
0.02
0.03
0.10
0.02
0.05
0.02
0.01
0.00
0.00
0.00
0.00
0.05
0.04
0.03
0.00
0.03
0.10
0.00
0.04
0.00
0.03
0.03
0.00
0.02
0.02
0.02
0.02
0.03
0.02
0.08
0.07
0.00
0.01
0.00
0.00
0.00
0.18
0.22
0.03
0.06
0.00
0.00
0.00
0.01
0.00
0.01
0.04
0.01
0.01
0.00
0.00
0.01
0.10
4.09
3.93
4.05
0.01
0.02
0.09
0.01
0.01
0.14
0.23
0.00
0.00
0.14
100.69
100.79
99.73
100.35
99.07
100.29
100.69
101.54
98.57
99.18
99.79
98.81
98.54
101.59
101.82
101.36
101.14
102.44
101.47
100.61
101.07
100.55
100.13
100.54
101.78
99.58
100.28
101.94
99.01
97.69
99.00
99.06
100.71
101.05
0.00
0.00
-0.01
-0.01
-0.08
-0.06
-0.03
-0.02
0.00
0.00
0.00
0.00
0.00
-0.02
-0.02
-0.01
0.00
-0.01
-0.04
0.00
-0.04
-0.92
-0.90
-0.93
0.00
-0.01
-0.03
-0.01
-0.01
-0.04
-0.06
-0.03
-0.03
-0.03
100.68
100.79
99.72
100.33
98.99
100.23
100.66
101.52
98.56
99.18
99.79
98.80
98.54
101.57
101.79
101.35
101.14
102.43
101.42
100.61
101.03
99.62
99.23
99.62
101.78
99.57
100.26
101.93
99.00
97.64
98.94
99.02
100.68
101.02
2.67
2.64
2.96
2.67
2.97
2.98
2.98
2.98
2.97
2.98
2.97
2.98
2.98
2.96
2.99
2.99
2.99
2.97
2.99
2.98
2.99
8.23
8.20
8.21
2.60
2.90
2.92
2.78
2.98
2.97
2.97
2.97
2.62
2.96
0.01
0.01
0.00
0.01
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.01
0.00
0.02
0.02
0.01
0.01
0.02
0.01
0.00
0.01
0.00
0.00
0.00
0.01
0.04
0.01
0.01
0.00
0.00
0.01
0.00
0.01
0.01
1.32
1.35
1.04
1.32
1.03
1.02
1.02
1.02
1.02
1.02
1.02
1.01
1.02
1.02
0.99
1.01
1.00
1.02
1.00
1.02
1.01
3.76
3.80
3.77
1.39
1.06
1.07
1.21
1.02
1.03
1.02
1.02
1.38
1.03
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
11.99
12.00
11.99
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
0.68
0.67
0.21
0.66
0.10
0.05
0.91
0.91
0.02
0.02
0.01
0.05
0.07
0.05
0.03
0.03
0.03
0.06
0.03
0.06
0.06
2.89
2.76
2.79
0.60
0.04
0.09
0.77
0.03
0.03
0.03
0.08
0.58
0.94
0.02
0.02
0.75
0.03
0.86
0.90
0.00
0.01
0.99
0.98
0.98
0.95
0.93
0.92
0.92
0.93
0.93
0.90
0.93
0.92
0.91
0.23
0.23
0.24
0.03
0.89
0.83
0.01
0.97
0.91
0.95
0.90
0.08
0.01
0.00
0.00
0.01
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.02
0.01
0.00
0.02
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.06
0.05
0.00
0.00
0.02
0.00
0.00
0.00
0.00
0.00
0.01
100.79
100.94
100.94
100.87
101.19
100.97
0.00
-0.02
-0.02
0.00
0.00
-0.01
100.79
100.91
100.92
100.87
101.19
100.96
0.94
0.96
0.97
0.97
0.96
0.95
0.01
0.01
0.01
0.02
0.02
0.01
2.04
2.03
2.02
2.01
2.02
2.03
3.00
3.00
3.00
3.00
3.00
3.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Ca
0.10
0.00
0.01
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.30
0.01
0.00
0.01
0.06
0.01
0.00
0.02
0.21
0.01
0.47
0.48
0.50
0.00
0.33
0.00
0.00
0.26
Mg
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.01
0.00
0.09
0.00
0.00
0.02
0.00
0.02
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Ti
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Cr
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
2+
Fe
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Mn
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Sum
0.99
0.95
0.99
0.98
0.00
0.99
1.00
0.98
0.00
1.01
1.01
0.96
0.98
1.03
0.91
0.87
0.88
0.98
0.98
0.98
0.99
0.97
1.00
1.01
1.01
1.02
1.00
1.00
0.98
0.98
0.97
F
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.01
0.01
0.01
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Cl
0.01
0.02
0.01
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.08
0.00
0.02
0.00
0.02
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
O
7.99
7.98
7.99
8.00
8.00
7.99
7.99
8.00
8.00
7.99
8.00
8.00
7.99
8.00
7.92
7.99
7.97
7.99
7.98
8.00
8.00
8.00
7.99
7.99
8.00
7.99
7.99
8.00
8.00
8.00
8.00
Total
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
0.02
0.00
0.27
0.00
0.00
0.00
0.01
0.05
0.08
0.05
0.09
0.24
0.25
0.12
0.24
0.01
0.01
0.01
0.00
0.03
0.00
0.00
0.02
0.00
0.02
0.01
0.00
0.02
0.02
0.01
0.02
0.02
0.02
0.02
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.98
0.99
0.99
0.98
0.99
0.93
1.00
0.97
0.97
1.02
0.97
1.00
1.00
1.00
1.01
0.74
0.94
0.90
0.89
0.99
1.00
0.99
0.93
0.00
0.86
0.89
1.02
0.95
0.93
0.92
0.87
0.86
0.88
0.88
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
7.99
7.99
7.99
8.00
7.99
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
7.99
8.00
7.98
7.99
8.00
7.99
7.99
8.00
8.00
8.00
8.00
7.99
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
0.02
0.02
0.01
0.03
0.01
0.01
0.02
0.00
0.22
0.00
0.03
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.02
0.01
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.02
0.02
0.32
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.88
0.88
0.89
0.90
0.97
1.00
0.96
0.99
0.99
0.98
0.97
0.98
0.99
0.99
0.98
0.98
0.96
0.98
0.99
0.98
0.98
0.98
0.98
1.00
0.96
0.98
0.98
0.99
0.99
0.99
0.98
1.01
0.99
0.99
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.01
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.02
0.03
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
8.00
8.00
8.00
7.99
8.00
8.00
8.00
8.00
8.00
7.99
8.00
7.99
7.99
8.00
7.99
7.98
7.97
7.99
8.00
8.00
8.00
8.00
8.00
8.00
8.00
7.99
8.00
7.99
7.99
7.99
7.99
8.00
7.99
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
0.30
0.33
0.01
0.32
0.01
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.88
0.93
0.91
0.36
0.00
0.02
0.20
0.00
0.00
0.00
0.00
0.35
0.03
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.04
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
1.00
1.01
0.97
1.00
0.97
0.95
0.93
0.93
1.01
1.00
0.99
1.00
1.00
0.97
0.95
0.96
0.96
0.96
0.96
0.98
0.96
4.00
3.93
3.95
1.00
0.93
0.93
0.98
1.00
0.94
0.99
0.98
1.01
0.97
0.00
0.00
0.00
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.01
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.02
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
1.00
0.96
0.99
0.00
0.00
0.01
0.00
0.00
0.01
0.02
0.00
0.00
0.01
8.00
8.00
8.00
8.00
7.97
7.98
7.99
7.99
8.00
8.00
8.00
8.00
8.00
7.99
7.99
8.00
8.00
8.00
7.99
8.00
7.99
0.00
0.02
0.00
8.00
8.00
7.99
8.00
8.00
7.98
7.98
7.99
7.99
7.99
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
1.00
1.00
1.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
Table A4. Chemical analyses of sheet silicates and dumortierite from Copiapó, Chile
Locality
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Negro Norte
Cerro Negro Norte
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
Jesus Maria
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
Sample
C2B-708
C2B-708
C2B-708
C2B-708
C2B-576c
C2B-576c
C2B-576c
C2B-576c
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-124
C2J-334
C2J-334
C6B-076
C6B-076
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C7B-003a
C2B-352e
C2B-352e
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
Spot no. Analysis no.
Mineral
2
m1
Mica
2
m1-1
Mica
2
b1
Mica
2
b2
Mica
1
b1
Mica
1
b2
Mica
1
m2
Mica
2
b1
Mica
3
tour1be
Mica
3
m1
Chlorite
3
m2
Mica
3
m4
Mica
3
k
Mica
3
k2
Mica
1
c2
Mica
2
a1
Mica
4
m1
Chlorite
4
m3
Chlorite
4
a1
Diaspore
2
d1
Pyrophyllite
2
d2
Pyrophyllite
1
d3
Pyrophyllite
1
d2
Dumortierite
4
d1
Dumortierite
4
d2
Dumortierite
1
b1
Chlorite
3
m1
Chlorite
2
b3
Mica
2
b4
Mica
2
b5
Mica
2
b6
Mica
SiO2
44.88
46.81
44.35
43.79
35.02
34.75
45.24
34.07
42.58
28.36
47.08
45.45
45.77
49.53
36.88
36.29
27.44
28.60
0.03
65.72
67.47
66.02
30.01
30.69
28.19
33.37
27.07
35.45
35.80
34.68
34.67
TiO2
0.00
0.00
0.00
0.00
2.22
2.11
0.55
2.22
0.12
0.04
0.24
0.47
0.34
0.25
2.78
2.52
0.02
0.01
0.06
0.00
0.01
0.01
2.32
2.38
2.03
4.41
0.01
4.62
4.73
4.13
4.77
Al2O3
32.44
33.24
30.95
31.71
18.86
18.21
34.14
18.18
25.75
23.30
31.00
31.78
30.98
31.92
14.17
14.32
19.15
18.69
85.05
27.89
28.87
29.50
61.42
60.00
62.04
12.35
16.41
13.07
12.86
13.60
12.48
B2O3
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
6.28
6.28
6.28
0.00
0.00
0.00
0.00
0.00
0.00
Cr2O3
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.01
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
Fe2O3
0.88
0.55
0.92
0.91
2.50
2.51
0.47
2.59
0.56
0.71
0.28
0.42
0.41
0.36
2.38
2.45
2.51
2.45
0.30
0.49
0.37
0.28
0.84
0.92
0.93
0.00
2.03
2.95
2.91
3.06
2.94
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH291-188.4
DDH291-188.4
DDH291-188.4
DDH291-188.4
DDH384-004.2
DDH628-094.2
DDH628-094.2
2
2
2
2
3
3
1
1
1
1
1
1
1
1
1
1
1
1
1
2
2
2
2
2
2
2
2
1
1
1
2
2
2
2
c1
b7
b8
b9
b1
b2
b1
b2
b3
b4
b5
b6
b7
b8
b9
m1
m2
m3
b11
b1
b2
m1
t7
b3
b4
m4
t10
b1
b2
b3
b1
c1
b1
b2
Mica
Mica
Mica
Mica
Mica
Mica
Mica
Mica
Mica
Chlorite
Mica
Mica
Mica
Mica
Mica
Chlorite
Chlorite
Mica
Mica
Mica
Mica
Chlorite
Chlorite
Mica
Chlorite
Mica
Mica
Mica
Mica
Mica
Mica
Chlorite
Chlorite
Mica
46.42
36.64
36.46
36.32
36.53
36.33
35.79
36.20
36.26
25.97
37.25
36.97
35.06
36.78
38.59
26.12
26.57
35.58
35.64
35.49
35.94
25.44
26.14
36.37
28.15
37.76
35.92
37.89
38.17
38.51
37.87
27.15
28.22
35.98
1.16
4.90
4.79
4.77
4.19
4.60
1.67
1.77
1.65
0.08
1.65
1.53
1.75
1.73
1.55
0.08
0.08
1.83
1.75
1.20
1.82
0.07
0.17
1.40
0.37
1.22
1.80
1.23
1.37
1.25
1.18
0.07
0.08
1.88
6.42
13.54
13.38
13.28
13.34
13.09
18.16
17.42
17.99
21.97
17.61
17.69
18.12
17.14
18.23
22.43
23.09
17.76
17.84
18.03
17.57
21.65
21.54
17.50
21.05
16.63
18.25
16.68
16.85
16.85
17.29
20.92
19.18
16.46
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.01
0.00
0.00
0.03
0.06
0.03
0.03
0.04
0.04
0.04
0.06
0.04
0.10
0.13
0.04
0.07
0.03
0.04
0.04
0.03
0.01
0.06
0.01
0.03
0.03
0.12
0.07
0.09
0.00
0.00
0.00
2.53
2.71
2.91
3.02
2.97
2.88
2.35
2.49
2.53
3.00
2.18
2.34
2.49
2.31
2.28
2.69
3.02
2.44
2.55
2.44
2.47
2.89
2.84
2.48
2.92
2.43
2.53
1.98
1.98
2.11
2.23
2.65
2.54
2.40
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
DDH628-094.2
DDH628-151.6
DDH628-151.6
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH628-626.3
DDH643-595.5
DDH684-079.8
ME013-538
ME013-538
ME013-538
ME013-538
ME013-538
ME013-538
2
2
2
1
1
1
1
1
1
1
2
2
2
2
1
1
1
1
3
1
1
1
2
2
2
b1
c1
c2
b1
b2
b3
b4
b5
b6
b7
b1
b2
b3
b4
sc1
sc2
sc3
c1
b2
b1
b2
b3
b1
t5
t6
Mica
Chlorite
Mica
Mica
Mica
Chlorite
Mica
Mica
Chlorite
Mica
Mica
Mica
Mica
Mica
Scapolite
Scapolite
Scapolite
Chlorite
Chlorite
Mica
Mica
Mica
Mica
Mica
Chlorite
37.42
26.85
36.99
36.36
36.51
28.32
39.09
38.43
26.46
37.88
37.39
37.31
36.37
36.99
57.02
56.73
56.95
26.78
28.15
35.49
35.88
35.30
35.47
37.63
27.94
0.47
0.02
0.07
1.30
1.52
0.02
0.01
0.06
0.01
0.08
1.40
1.41
1.21
1.48
0.00
0.00
0.00
0.02
0.05
1.17
0.58
1.50
1.67
2.04
0.02
17.10
19.67
17.99
17.11
17.61
21.04
16.77
17.93
22.20
18.25
17.55
18.16
17.42
17.35
22.12
22.29
22.21
19.29
19.54
17.86
18.46
20.54
17.52
16.48
19.35
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
2.06
2.70
2.35
2.31
2.41
2.75
2.02
2.10
2.62
2.18
3.35
2.29
2.48
2.35
0.00
0.00
0.00
3.20
2.83
2.63
2.48
2.18
2.55
2.34
2.71
IV
FeO
6.28
4.06
6.27
6.39
17.54
17.33
3.16
18.09
3.72
5.27
2.27
3.01
3.05
2.85
16.54
16.92
16.66
17.38
0.11
0.00
0.00
0.00
0.00
0.00
0.00
22.41
33.14
20.56
20.28
21.56
21.27
MgO
0.36
0.35
1.71
0.93
9.87
9.59
0.63
9.16
16.82
28.39
1.74
1.52
6.29
1.85
11.81
11.84
19.31
19.78
0.00
0.19
0.07
0.01
0.11
0.12
0.13
9.44
9.12
9.03
9.37
9.29
8.47
MnO
0.00
0.03
0.03
0.05
0.16
0.10
0.00
0.12
0.20
0.37
0.01
0.02
0.11
0.01
0.38
0.38
0.08
0.14
0.00
0.02
0.00
0.00
0.00
0.00
0.00
0.27
0.36
0.17
0.19
0.24
0.18
CaO
0.00
0.08
0.00
0.00
0.06
0.01
0.00
0.00
0.13
0.01
0.00
0.01
0.01
0.05
0.14
0.07
0.08
0.12
0.01
0.20
0.09
0.29
0.30
0.00
0.01
0.33
0.06
0.01
0.00
0.01
0.02
Na2O
0.11
0.11
0.11
0.11
0.10
0.15
0.43
0.07
1.63
0.01
0.17
0.35
0.19
0.12
0.14
0.06
0.02
0.00
0.00
0.07
0.06
0.04
0.02
0.00
0.01
0.24
0.09
0.14
0.16
0.15
0.12
K2O
10.31
10.55
10.88
10.83
8.45
9.13
10.51
9.68
1.72
0.02
9.34
9.98
8.71
9.62
9.10
9.43
0.01
0.00
0.00
0.07
0.05
0.01
0.00
0.00
0.00
7.74
0.03
9.10
9.12
7.89
9.20
H2O
4.36
4.44
4.30
4.29
3.82
3.78
4.44
3.75
4.38
12.43
4.37
4.32
4.50
4.51
3.80
3.78
11.49
11.74
15.09
4.91
5.08
5.03
0.56
0.56
0.56
10.11
10.90
3.60
3.64
3.62
3.56
F
0.03
0.05
0.06
0.02
0.18
0.14
0.00
0.14
0.10
0.14
0.01
0.08
0.01
0.13
0.17
0.18
0.08
0.04
0.00
0.07
0.02
0.03
0.07
0.10
0.22
0.12
0.03
0.16
0.22
0.20
0.15
Cl
0.02
0.01
0.04
0.09
0.16
0.16
0.01
0.17
0.04
0.00
0.00
0.01
0.02
0.01
0.14
0.14
0.01
0.01
0.00
0.05
0.00
0.00
0.00
0.01
0.00
0.44
0.02
0.69
0.52
0.45
0.58
Subtotal O=F+Cl Total
99.70
-0.02
99.68
100.27
-0.02 100.25
99.60
-0.03
99.57
99.11
-0.03
99.08
98.93
-0.11
98.82
97.96
-0.09
97.87
99.58
0.00
99.58
98.25
-0.10
98.15
97.84
-0.05
97.79
99.11
-0.06
99.05
96.77
-0.01
96.76
97.69
-0.04
97.66
100.55
-0.01 100.54
101.38
-0.06 101.33
98.66
-0.10
98.56
98.58
-0.11
98.47
96.90
-0.03
96.86
99.01
-0.02
98.99
100.65
0.00
100.65
99.69
-0.04
99.64
102.09
-0.01 102.08
101.21
-0.01 101.20
101.94
-0.03 101.91
101.06
-0.04 101.02
100.41
-0.09 100.32
101.48
-0.15 101.33
99.52
-0.02
99.50
99.85
-0.22
99.62
100.11
-0.21
99.90
99.17
-0.19
98.99
98.70
-0.19
98.50
Si
3.07
3.14
3.06
3.04
2.66
2.68
3.06
2.65
2.88
2.72
3.23
3.12
3.05
3.24
2.82
2.79
2.86
2.92
0.00
3.97
3.97
3.92
2.75
2.85
2.62
3.89
2.97
2.76
2.77
2.71
2.75
B
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Al
0.93
0.86
0.94
0.96
1.34
1.32
0.94
1.35
1.12
1.28
0.77
0.88
0.95
0.76
1.18
1.21
1.14
1.08
1.00
0.03
0.03
0.08
0.25
0.15
0.38
0.11
1.03
1.20
1.17
1.25
1.17
Fe3+
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.04
0.06
0.03
0.09
Sum
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
1.00
4.00
4.00
4.00
3.00
3.00
3.00
4.00
4.00
4.00
4.00
4.00
4.00
17.47
20.16
20.00
19.94
19.96
20.11
17.93
16.82
17.53
20.67
17.07
16.60
18.06
16.22
15.66
21.02
20.16
17.13
18.19
17.46
17.95
20.32
20.38
16.73
20.17
16.41
18.16
15.07
13.92
14.41
14.93
17.94
17.10
16.16
10.36
9.79
9.78
9.71
10.06
9.76
9.72
9.77
9.87
16.15
10.15
10.28
9.55
9.65
10.11
15.65
15.55
9.93
10.46
10.20
9.78
15.74
16.10
10.38
15.14
10.99
9.98
12.30
12.42
12.49
12.40
18.36
20.10
11.56
0.46
0.21
0.21
0.14
0.18
0.17
0.18
0.15
0.18
0.28
0.22
0.13
0.25
0.21
0.21
0.30
0.27
0.15
0.23
0.19
0.19
0.26
0.28
0.18
0.26
0.13
0.18
0.15
0.14
0.12
0.14
0.18
0.34
0.25
10.93
0.01
0.02
0.01
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.06
0.15
0.01
0.04
0.01
0.00
0.01
0.04
0.04
0.01
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.03
0.00
1.19
0.16
0.13
0.13
0.07
0.11
0.08
0.12
0.09
0.00
0.08
0.08
0.11
0.09
0.32
0.05
0.08
0.07
0.09
0.11
0.09
0.03
0.01
0.07
0.00
0.09
0.08
0.08
0.04
0.09
0.07
0.00
0.01
0.11
0.64
9.16
9.11
9.08
9.32
9.22
9.67
9.24
9.60
0.14
9.64
9.62
9.64
9.58
9.43
0.02
0.00
9.48
8.85
9.19
9.61
0.11
0.43
9.66
1.90
9.05
9.62
9.56
9.01
9.62
9.84
0.01
0.01
9.64
4.03
3.70
3.69
3.64
3.64
3.62
3.72
3.71
3.77
11.63
3.78
3.79
3.67
3.68
3.81
11.69
11.82
3.71
3.74
3.74
3.69
11.41
11.58
3.74
11.81
3.78
3.74
3.86
3.85
3.88
3.90
11.70
11.80
3.77
0.12
0.27
0.25
0.32
0.30
0.28
0.24
0.25
0.21
0.05
0.33
0.26
0.24
0.32
0.37
0.00
0.01
0.26
0.26
0.17
0.20
0.02
0.04
0.26
0.05
0.23
0.20
0.21
0.26
0.24
0.22
0.03
0.03
0.18
0.31
0.54
0.56
0.55
0.62
0.66
0.47
0.34
0.40
0.04
0.25
0.26
0.53
0.32
0.36
0.03
0.03
0.35
0.38
0.37
0.62
0.05
0.05
0.32
0.10
0.35
0.60
0.13
0.11
0.18
0.15
0.04
0.01
0.26
102.20
102.14
101.60
101.22
101.49
101.13
100.19
98.55
100.32
100.10
100.47
99.80
99.72
98.33
101.35
100.31
100.94
98.98
100.28
98.81
100.24
98.15
99.70
99.29
102.08
99.26
101.29
99.21
98.24
99.83
100.33
99.04
99.45
98.64
-0.12
-0.24
-0.23
-0.26
-0.27
-0.26
-0.21
-0.18
-0.18
-0.03
-0.20
-0.17
-0.22
-0.21
-0.24
-0.01
-0.01
-0.19
-0.20
-0.16
-0.22
-0.02
-0.03
-0.18
-0.04
-0.18
-0.22
-0.12
-0.13
-0.14
-0.13
-0.02
-0.01
-0.13
102.08
101.90
101.37
100.96
101.22
100.86
99.99
98.37
100.14
100.07
100.28
99.63
99.49
98.12
101.12
100.30
100.93
98.79
100.09
98.65
100.01
98.13
99.67
99.11
102.03
99.08
101.07
99.09
98.10
99.69
100.20
99.02
99.43
98.51
3.34
2.77
2.77
2.77
2.78
2.78
2.72
2.77
2.74
2.67
2.79
2.79
2.68
2.81
2.84
2.68
2.69
2.72
2.70
2.72
2.73
2.67
2.70
2.77
2.85
2.85
2.70
2.84
2.86
2.86
2.81
2.78
2.86
2.75
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.54
1.21
1.20
1.19
1.20
1.18
1.28
1.23
1.26
1.33
1.21
1.21
1.32
1.19
1.16
1.32
1.31
1.28
1.30
1.28
1.27
1.33
1.30
1.23
1.15
1.15
1.30
1.16
1.14
1.14
1.19
1.22
1.14
1.25
0.11
0.03
0.03
0.04
0.02
0.04
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
14.52
19.30
15.57
16.64
16.60
18.46
14.55
14.82
18.48
15.01
15.20
16.29
16.78
15.85
0.10
0.03
0.12
22.30
17.45
17.90
17.63
17.18
18.61
17.62
21.27
13.02
17.19
11.72
13.25
11.97
17.46
14.34
13.23
17.96
12.86
11.86
12.32
12.34
12.04
0.00
0.00
0.00
15.83
19.21
10.33
10.53
8.47
10.11
10.55
16.56
0.25
0.22
0.17
0.23
0.17
0.20
0.12
0.11
0.16
0.11
0.11
0.12
0.16
0.09
0.00
0.01
0.01
0.32
0.36
0.25
0.23
0.22
0.27
0.25
0.35
0.07
0.03
0.00
0.92
0.00
0.01
0.00
0.00
0.02
0.00
0.00
0.00
0.01
0.01
5.68
6.02
5.86
0.01
0.00
0.01
0.00
0.10
0.01
0.04
0.04
0.13
0.03
0.04
0.02
0.01
0.00
0.08
0.10
0.03
0.11
0.06
0.09
0.03
0.09
10.32
9.86
9.98
0.00
0.00
0.07
0.04
0.39
0.12
0.11
0.00
9.30
0.04
9.76
8.14
9.56
1.03
8.68
9.60
0.06
9.49
9.85
9.63
8.72
9.33
1.22
1.23
1.33
0.01
0.02
9.58
9.84
8.18
9.48
9.23
0.01
3.88
11.42
3.83
3.85
3.87
11.91
3.94
3.94
11.77
3.89
3.92
3.95
3.78
3.91
0.00
0.00
0.00
11.43
11.77
3.77
3.84
3.84
3.80
3.85
11.67
0.16
0.03
0.20
0.22
0.17
0.03
0.23
0.23
0.03
0.21
0.18
0.15
0.15
0.10
0.00
0.03
0.03
0.06
0.03
0.22
0.15
0.12
0.13
0.23
0.03
0.08
0.02
0.17
0.28
0.24
0.04
0.11
0.11
0.02
0.24
0.17
0.24
0.53
0.18
4.09
3.93
4.05
0.03
0.02
0.20
0.19
0.16
0.31
0.17
0.01
98.46
97.51
98.84
100.73
100.74
101.28
99.97
100.67
99.84
100.34
101.16
102.07
100.05
99.88
100.55
100.13
100.54
99.29
99.42
99.53
99.94
98.21
100.11
100.54
100.58
-0.09
-0.02
-0.12
-0.16
-0.13
-0.02
-0.12
-0.12
-0.02
-0.14
-0.11
-0.12
-0.19
-0.08
-0.92
-0.90
-0.93
-0.03
-0.02
-0.14
-0.11
-0.09
-0.12
-0.14
-0.01
98.37
97.50
98.72
100.57
100.61
101.26
99.85
100.54
99.82
100.20
101.05
101.96
99.86
99.79
99.62
99.23
99.62
99.26
99.40
99.39
99.83
98.12
99.99
100.41
100.56
2.82
2.81
2.80
2.71
2.73
2.85
2.88
2.83
2.69
2.80
2.77
2.74
2.73
2.77
8.23
8.20
8.21
2.80
2.86
2.71
2.72
2.69
2.70
2.82
2.87
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
1.18
1.19
1.20
1.29
1.27
1.15
1.12
1.17
1.31
1.20
1.23
1.26
1.27
1.23
3.76
3.80
3.77
1.20
1.14
1.29
1.28
1.31
1.30
1.18
1.13
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
11.99
12.00
11.99
4.00
4.00
4.00
4.00
4.00
4.00
4.00
4.00
Oct
Al
1.69
1.77
1.58
1.63
0.35
0.34
1.77
0.31
0.93
1.36
1.73
1.70
1.48
1.71
0.10
0.09
1.20
1.16
0.00
1.96
1.98
1.99
6.39
6.41
6.43
1.59
1.10
0.00
0.00
0.00
0.00
X
Mg
0.04
0.03
0.18
0.10
1.12
1.10
0.06
1.06
1.69
4.06
0.18
0.16
0.62
0.18
1.35
1.36
2.99
3.01
0.00
0.02
0.01
0.00
0.01
0.02
0.02
1.64
1.49
1.05
1.08
1.08
1.00
Fe2+
0.36
0.23
0.36
0.37
1.12
1.12
0.18
1.17
0.21
0.42
0.13
0.17
0.17
0.16
1.06
1.09
1.45
1.48
0.00
0.00
0.00
0.00
0.00
0.00
0.00
2.19
3.04
1.34
1.31
1.41
1.41
Fe3+
0.05
0.03
0.05
0.05
0.14
0.15
0.02
0.15
0.03
0.05
0.01
0.02
0.02
0.02
0.14
0.14
0.20
0.19
0.00
0.02
0.02
0.01
0.06
0.06
0.07
0.00
0.17
0.13
0.11
0.15
0.09
Mn
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.01
0.01
0.03
0.00
0.00
0.01
0.00
0.02
0.02
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.03
0.03
0.01
0.01
0.02
0.01
Ti
0.00
0.00
0.00
0.00
0.13
0.12
0.03
0.13
0.01
0.00
0.01
0.02
0.02
0.01
0.16
0.15
0.00
0.00
0.00
0.00
0.00
0.00
0.16
0.17
0.14
0.39
0.00
0.27
0.28
0.24
0.28
Cr
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
□
0.86
0.94
0.83
0.85
0.13
0.17
0.93
0.17
0.12
0.07
0.92
0.91
0.68
0.92
0.16
0.14
0.14
0.15
3.00
1.00
1.00
1.00
0.37
0.34
0.34
0.14
0.14
0.18
0.19
0.09
0.19
Sum
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
6.00
3.00
3.00
3.00
3.00
3.00
3.00
6.00
6.00
3.00
3.00
3.00
3.00
7.00
7.00
7.00
6.00
6.00
3.00
3.00
3.00
3.00
Na
0.01
0.01
0.01
0.01
0.01
0.02
0.06
0.01
0.21
0.00
0.02
0.05
0.02
0.02
0.02
0.01
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.05
0.02
0.02
0.02
0.02
0.02
K
0.90
0.90
0.96
0.96
0.82
0.90
0.91
0.96
0.15
0.00
0.82
0.87
0.74
0.80
0.89
0.93
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
1.15
0.00
0.90
0.90
0.79
0.93
Ca
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.01
0.01
0.00
0.01
0.01
0.02
0.03
0.00
0.00
0.04
0.01
0.00
0.00
0.00
0.00
□
0.08
0.08
0.03
0.03
0.16
0.08
0.04
0.03
0.63
0.99
0.16
0.08
0.24
0.18
0.08
0.06
0.99
0.99
1.00
0.97
0.98
0.98
0.97
1.00
1.00
0.00
0.97
0.08
0.08
0.19
0.05
Sum
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.25
1.00
1.00
1.00
1.00
1.00
OH
F
0.01
0.01
0.01
0.00
0.04
0.03
0.00
0.04
0.02
0.04
0.00
0.02
0.00
0.03
0.04
0.04
0.03
0.01
0.00
0.01
0.00
0.01
0.02
0.03
0.06
0.04
0.01
0.04
0.05
0.05
0.04
Cl
0.00
0.00
0.00
0.01
0.02
0.02
0.00
0.02
0.00
0.00
0.00
0.00
0.00
0.00
0.02
0.02
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.09
0.00
0.09
0.07
0.06
0.08
OH
1.99
1.99
1.98
1.99
1.94
1.95
2.00
1.94
1.97
7.96
2.00
1.98
2.00
1.97
1.94
1.94
7.97
7.98
1.00
1.98
2.00
1.99
0.34
0.35
0.35
7.87
7.99
1.87
1.88
1.89
1.88
0.00
0.00
0.00
0.00
0.00
0.00
0.34
0.34
0.34
1.34
0.35
0.36
0.32
0.36
0.42
1.39
1.45
0.32
0.29
0.35
0.30
1.35
1.32
0.33
1.36
0.33
0.32
0.32
0.35
0.33
0.32
1.30
1.16
0.24
1.11
1.10
1.11
1.10
1.14
1.11
1.10
1.11
1.11
2.48
1.13
1.15
1.09
1.10
1.11
2.39
2.35
1.13
1.18
1.16
1.11
2.46
2.48
1.18
2.28
1.24
1.12
1.38
1.39
1.38
1.37
2.80
3.04
1.32
1.05
1.27
1.27
1.27
1.27
1.29
1.14
1.08
1.11
1.78
1.07
1.05
1.16
1.04
0.96
1.80
1.71
1.10
1.15
1.12
1.14
1.78
1.76
1.06
1.71
1.04
1.14
0.95
0.87
0.89
0.93
1.53
1.45
1.03
0.03
0.13
0.13
0.14
0.15
0.12
0.13
0.14
0.14
0.23
0.12
0.13
0.14
0.13
0.13
0.21
0.23
0.14
0.14
0.14
0.14
0.23
0.22
0.14
0.22
0.14
0.14
0.11
0.11
0.12
0.12
0.20
0.19
0.14
0.03
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.02
0.01
0.01
0.02
0.01
0.01
0.03
0.02
0.01
0.01
0.01
0.01
0.02
0.02
0.01
0.02
0.01
0.01
0.01
0.01
0.01
0.01
0.02
0.03
0.02
0.06
0.28
0.27
0.27
0.24
0.26
0.10
0.10
0.09
0.01
0.09
0.09
0.10
0.10
0.09
0.01
0.01
0.11
0.10
0.07
0.10
0.01
0.01
0.08
0.03
0.07
0.10
0.07
0.08
0.07
0.07
0.01
0.01
0.11
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.71
0.19
0.19
0.19
0.17
0.18
0.17
0.20
0.18
0.14
0.20
0.20
0.16
0.24
0.26
0.16
0.21
0.17
0.11
0.14
0.17
0.15
0.17
0.18
0.37
0.17
0.16
0.17
0.18
0.19
0.17
0.14
0.12
0.15
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
6.00
3.00
3.00
3.00
3.00
3.00
6.00
6.00
3.00
3.00
3.00
3.00
6.00
6.00
3.00
6.00
3.00
3.00
3.00
3.00
3.00
3.00
6.00
6.00
3.00
0.17
0.02
0.02
0.02
0.01
0.02
0.01
0.02
0.01
0.00
0.01
0.01
0.02
0.01
0.05
0.01
0.02
0.01
0.01
0.02
0.01
0.01
0.00
0.01
0.00
0.01
0.01
0.01
0.01
0.01
0.01
0.00
0.00
0.02
0.06
0.88
0.88
0.88
0.90
0.90
0.94
0.90
0.92
0.02
0.92
0.93
0.94
0.93
0.89
0.00
0.00
0.93
0.85
0.90
0.93
0.01
0.06
0.94
0.25
0.87
0.92
0.92
0.86
0.91
0.93
0.00
0.00
0.94
0.84
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.09
0.10
0.10
0.08
0.08
0.05
0.08
0.06
0.98
0.07
0.06
0.04
0.05
0.06
0.98
0.98
0.06
0.13
0.08
0.05
0.98
0.94
0.05
0.75
0.12
0.07
0.07
0.13
0.07
0.06
1.00
0.99
0.04
1.07
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
0.03
0.06
0.06
0.08
0.07
0.07
0.06
0.06
0.05
0.02
0.08
0.06
0.06
0.08
0.09
0.00
0.00
0.06
0.06
0.04
0.05
0.01
0.01
0.06
0.02
0.05
0.05
0.05
0.06
0.06
0.05
0.01
0.01
0.04
0.04
0.07
0.07
0.07
0.08
0.09
0.06
0.04
0.05
0.01
0.03
0.03
0.07
0.04
0.04
0.01
0.01
0.05
0.05
0.05
0.08
0.01
0.01
0.04
0.02
0.04
0.08
0.02
0.01
0.02
0.02
0.01
0.00
0.03
1.93
1.87
1.87
1.85
1.85
1.85
1.88
1.90
1.90
7.98
1.89
1.90
1.87
1.88
1.87
7.99
7.99
1.89
1.89
1.91
1.87
7.98
7.98
1.90
7.97
1.90
1.88
1.93
1.92
1.92
1.93
7.98
7.99
1.92
0.34
1.24
0.40
0.21
0.28
1.34
0.33
0.38
1.35
0.40
0.30
0.31
0.28
0.30
0.00
0.00
0.00
1.18
1.21
0.32
0.37
0.53
0.27
0.27
1.21
1.46
2.69
1.32
1.47
1.33
2.62
1.57
1.45
2.72
1.42
1.31
1.35
1.38
1.34
0.00
0.00
0.00
2.47
2.91
1.18
1.19
0.96
1.15
1.18
2.53
0.92
1.69
0.98
1.04
1.04
1.55
0.90
0.91
1.57
0.93
0.94
1.00
1.05
0.99
0.01
0.00
0.01
1.95
1.48
1.14
1.12
1.09
1.19
1.10
1.83
0.12
0.21
0.13
0.13
0.14
0.21
0.11
0.12
0.20
0.12
0.19
0.13
0.14
0.13
0.00
0.00
0.00
0.25
0.22
0.15
0.14
0.12
0.15
0.13
0.21
0.02
0.02
0.01
0.01
0.01
0.02
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.00
0.00
0.00
0.03
0.03
0.02
0.01
0.01
0.02
0.02
0.03
0.03
0.00
0.00
0.07
0.09
0.00
0.00
0.00
0.00
0.00
0.08
0.08
0.07
0.08
0.00
0.00
0.00
0.00
0.00
0.07
0.03
0.09
0.10
0.11
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.13
0.14
0.14
0.06
0.12
0.27
0.08
0.13
0.13
0.12
0.18
0.13
0.07
0.14
0.00
0.00
0.00
0.12
0.15
0.13
0.13
0.19
0.13
0.18
0.15
3.00
6.00
3.00
3.00
3.00
6.00
3.00
3.00
6.00
3.00
3.00
3.00
3.00
3.00
0.01
0.01
0.02
6.00
6.00
3.00
3.00
3.00
3.00
3.00
6.00
0.02
0.01
0.01
0.00
0.00
0.00
0.01
0.01
0.01
0.02
0.01
0.01
0.00
0.01
2.89
2.76
2.79
0.00
0.00
0.01
0.01
0.06
0.02
0.02
0.00
0.89
0.00
0.94
0.77
0.91
0.13
0.82
0.90
0.01
0.90
0.93
0.90
0.84
0.89
0.23
0.23
0.24
0.00
0.00
0.93
0.95
0.79
0.92
0.88
0.00
0.01
0.00
0.00
0.07
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.88
0.93
0.91
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.08
0.99
0.05
0.15
0.09
0.87
0.17
0.08
0.98
0.09
0.06
0.09
0.16
0.09
0.00
0.07
0.05
1.00
1.00
0.06
0.04
0.14
0.06
0.10
0.99
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
3.99
3.99
3.98
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
0.04
0.01
0.05
0.05
0.04
0.01
0.05
0.05
0.01
0.05
0.04
0.04
0.04
0.02
0.00
0.01
0.01
0.02
0.01
0.05
0.04
0.03
0.03
0.05
0.01
0.01
0.00
0.02
0.04
0.03
0.01
0.01
0.01
0.00
0.03
0.02
0.03
0.07
0.02
1.00
0.96
0.99
0.01
0.00
0.03
0.02
0.02
0.04
0.02
0.00
1.95
7.99
1.93
1.91
1.93
7.98
1.93
1.93
7.99
1.92
1.94
1.93
1.90
1.95
0.00
0.02
0.00
7.97
7.99
1.92
1.94
1.95
1.93
1.92
7.99
Sum
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
8.00
2.00
2.00
2.00
2.00
2.00
2.00
8.00
8.00
1.00
2.00
2.00
2.00
0.36
0.38
0.41
8.00
8.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
8.00
2.00
2.00
2.00
2.00
2.00
8.00
8.00
2.00
2.00
2.00
2.00
8.00
8.00
2.00
8.00
2.00
2.00
2.00
2.00
2.00
2.00
8.00
8.00
2.00
2.00
8.00
2.00
2.00
2.00
8.00
2.00
2.00
8.00
2.00
2.00
2.00
2.00
2.00
1.00
1.00
1.00
8.00
8.00
2.00
2.00
2.00
2.00
2.00
8.00
Table A5. Chemical analyses of pyroxenes from Copiapó, Chile
Locality
Cerro Bronce Estrella
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
Sample
C2B-298
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
Spot no. Analysis no.
Mineral
SiO2
1
s2
Augite
53.78
2
c4
Augite
51.74
2
o1
Orthopyroxene 50.17
2
o2
Orthopyroxene 50.82
2
o3
Orthopyroxene 50.86
3
o1
Augite
51.67
3
o2
Augite
51.86
3
o3
Augite
51.54
3
o4
Augite
50.03
3
o5
Augite
52.02
TiO2
0.03
0.10
0.30
0.39
0.30
0.09
0.09
0.25
0.78
0.03
Al2O3
0.26
0.46
0.42
0.46
0.62
0.51
0.45
0.93
3.88
0.22
B2O3
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Cr2O3 Fe2O3
0.03
1.13
0.00
1.03
0.00
0.71
0.00
0.73
0.00
0.14
0.00
1.19
0.00
0.46
0.00
1.27
0.00
0.00
0.01
0.65
FeO
2.78
12.89
30.84
28.19
27.07
12.41
12.46
10.43
16.98
12.41
MgO
16.07
11.46
14.81
16.48
16.33
11.61
11.73
12.35
13.01
11.43
MnO
0.27
0.64
1.39
0.95
0.93
0.64
0.62
0.51
0.45
0.65
CaO
24.65
21.12
1.22
1.97
2.82
21.06
21.26
21.78
10.99
21.92
Na2O
0.23
0.25
0.00
0.00
0.07
0.27
0.23
0.22
0.86
0.15
K2O
0.00
0.00
0.00
0.01
0.00
0.01
0.00
0.00
0.35
0.00
F
0.00
0.05
0.00
0.00
0.00
0.04
0.06
0.01
0.19
0.00
Cl
0.00
0.01
0.01
0.00
0.01
0.00
0.00
0.00
0.17
0.00
Subtotal O=F+Cl Total
99.24
0.00
99.24
99.79
-0.02
99.77
99.96
0.00
99.96
100.08
0.00
100.08
99.23
0.00
99.23
99.56
-0.02
99.54
99.28
-0.03
99.25
99.35
0.00
99.35
97.82
-0.12
97.70
99.56
0.00
99.55
IV
Si
1.99
1.98
1.97
1.97
1.98
1.98
1.98
1.96
1.94
1.99
A
3+
Fe
0.03
0.03
0.02
0.02
0.00
0.03
0.01
0.04
0.00
0.02
Al
0.00
0.00
0.01
0.01
0.02
0.00
0.00
0.00
0.06
0.00
Sum
2.02
2.01
2.00
2.00
2.00
2.01
2.00
2.00
2.00
2.01
Al
0.01
0.02
0.01
0.01
0.01
0.02
0.02
0.04
0.12
0.01
2+
Fe
0.09
0.41
1.01
0.91
0.88
0.40
0.40
0.33
0.55
0.40
Na
0.02
0.02
0.00
0.00
0.01
0.02
0.02
0.02
0.06
0.01
K
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.02
0.00
Ca
0.98
0.86
0.05
0.08
0.12
0.86
0.87
0.89
0.46
0.90
Mg
0.88
0.65
0.87
0.95
0.95
0.66
0.67
0.70
0.75
0.65
Sc
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Ti
0.00
0.00
0.01
0.01
0.01
0.00
0.00
0.01
0.02
0.00
V
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Cr
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Mn
0.01
0.02
0.05
0.03
0.03
0.02
0.02
0.02
0.01
0.02
Cu
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Zn
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Sum
1.98
1.99
2.00
2.00
2.00
1.99
2.00
2.00
2.00
1.99
O
F
0.00
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.02
0.00
Cl
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
O
6.00
5.99
6.00
6.00
6.00
6.00
5.99
6.00
5.96
6.00
Total
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
Table A6. Chemical analyses of epidote from Copiapó, Chile
Locality
Sample
Spot no. Analysis no.
Cerro Bronce Estrella
C2B-298
2
e1
Cerro Negro Norte
C6B-076
2
e1
Cerro Negro Norte
C6B-076
2
e2
Cerro Negro Norte
C6B-076
2
e3
San Gregorio S Granate
C2B-352e
1
m1
San Gregorio S Granate
C2B-671
1
e1
Santos PdC
DDH289-037.5a
2
e1
Santos PdC
DDH289-037.5a
2
e2
Santos PdC
DDH291-188.4
1
e1
Santos PdC
DDH291-188.4
1
e2
Santos PdC
DDH384-004.2
1
e1
Santos PdC
DDH384-004.2
1
e2
Santos PdC
DDH384-004.2
1
e3
Santos PdC
DDH384-004.2
1
x1
Santos PdC
DDH628-094.2
2
e1
Santos PdC
DDH643-595.5
2
e1
Santos PdC
DDH643-595.5
2
e2
Santos PdC
DDH643-595.5
3
e1
Santos PdC
DDH684-079.8
1
s1
Santos PdC
ME013-538
1
e1
Santos PdC
ME013-538
2
e1
Santos PdC
ME013-538
2
e2
Santos PdC
ME013-538
2
e3
Santos PdC
ME013-538
2
e4
SiO2
37.70
36.19
36.56
36.78
38.65
38.19
37.25
37.16
37.82
38.14
35.86
37.35
36.75
37.01
37.12
37.08
36.26
36.97
37.25
37.46
37.85
37.63
37.31
37.93
TiO2
0.07
0.00
0.01
0.02
0.01
0.03
0.12
0.12
0.17
0.30
0.00
0.00
0.02
0.02
0.52
0.05
0.00
0.07
0.01
0.03
0.08
0.00
0.07
0.05
Al2O3
26.04
25.54
26.84
23.58
31.29
25.79
24.37
24.36
24.85
27.11
15.99
26.28
21.48
21.56
21.52
23.94
20.26
21.82
22.89
23.37
24.41
25.56
22.77
23.86
Cr2O3
0.00
0.01
0.00
0.00
0.00
0.01
0.04
0.06
0.04
0.03
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Fe2O3
10.31
10.99
9.73
13.33
1.74
11.12
12.28
12.11
11.98
9.09
22.80
9.54
15.50
15.29
16.08
12.87
17.02
15.84
15.26
13.91
12.63
11.32
14.87
13.86
FeO
0.00
0.00
0.00
0.00
0.25
0.07
0.00
0.00
0.18
0.12
0.01
0.00
0.10
0.39
0.07
0.00
0.20
0.07
0.12
0.20
0.24
0.00
0.00
0.13
MgO
0.05
0.03
0.05
0.02
0.00
0.00
0.02
0.02
0.03
0.02
0.00
0.00
0.00
0.00
0.03
0.00
0.02
0.07
0.01
0.03
0.02
0.00
0.05
0.03
MnO
0.03
0.26
0.24
0.11
1.62
0.06
0.15
0.15
0.18
0.12
0.01
0.01
0.10
0.39
0.06
0.06
0.48
0.06
0.12
0.19
0.23
0.10
0.06
0.13
CaO
23.84
22.97
23.37
23.22
23.52
23.56
23.52
23.72
23.11
23.67
22.28
23.39
22.58
22.39
23.02
23.34
22.36
22.21
22.93
22.86
22.99
23.56
23.25
23.14
IV
Na2O
0.01
0.00
0.02
0.00
0.02
0.00
0.00
0.00
0.03
0.00
0.00
0.03
0.01
0.00
0.00
0.03
0.01
0.00
0.00
0.03
0.00
0.00
0.00
0.00
K2O
0.00
0.00
0.00
0.00
0.07
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.01
0.00
0.02
0.01
0.01
0.00
0.00
H2O
1.89
1.79
1.81
1.85
1.94
1.92
1.87
1.89
1.89
1.91
1.76
1.86
1.82
1.85
1.85
1.85
1.81
1.80
1.86
1.85
1.89
1.89
1.86
1.91
F
0.04
0.16
0.17
0.04
0.00
0.00
0.04
0.00
0.03
0.04
0.07
0.06
0.04
0.00
0.04
0.05
0.04
0.10
0.05
0.06
0.02
0.04
0.03
0.00
Cl
0.00
0.00
0.00
0.00
0.02
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.02
0.00
0.03
0.00
0.00
0.04
0.00
Subtotal O=F+Cl Total
99.97
-0.02
99.95
97.97
-0.07
97.90
98.86
-0.07
98.79
99.03
-0.02
99.01
99.20
-0.01
99.20
100.76
0.00
100.76
99.95
-0.02
99.93
99.86
0.00
99.86
100.33
-0.01
100.31
100.55
-0.02
100.53
98.79
-0.03
98.76
98.52
-0.03
98.50
98.42
-0.02
98.40
98.90
0.00
98.90
100.31
-0.02
100.29
99.27
-0.02
99.24
98.45
-0.02
98.44
99.03
-0.05
98.98
100.51
-0.02
100.49
100.06
-0.03
100.03
100.38
-0.01
100.37
100.15
-0.02
100.13
100.32
-0.02
100.30
101.43
0.00
101.43
Si
2.96
2.91
2.90
2.95
2.98
2.98
2.95
2.95
2.98
2.97
3.00
2.97
3.00
3.00
2.98
2.96
2.97
3.00
2.96
2.98
2.99
2.96
2.97
2.98
Al
0.04
0.09
0.10
0.05
0.02
0.02
0.05
0.05
0.02
0.03
0.00
0.03
0.00
0.00
0.02
0.04
0.03
0.00
0.04
0.02
0.01
0.04
0.03
0.02
Sum
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
3.00
Oct
Al
2.37
2.33
2.41
2.18
2.82
2.36
2.23
2.22
2.29
2.46
1.57
2.43
2.06
2.06
2.01
2.22
1.93
2.08
2.11
2.18
2.26
2.33
2.11
2.19
Mg
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.01
0.00
2+
Mn
0.00
0.00
0.00
0.00
0.02
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.01
0.03
0.00
0.00
0.01
0.00
0.01
0.01
0.02
0.00
0.00
0.01
Mn3+
0.00
0.02
0.02
0.01
0.09
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.02
0.00
0.00
0.00
0.00
0.01
0.00
0.00
A
3+
Fe
0.61
0.67
0.58
0.80
0.12
0.66
0.73
0.72
0.72
0.54
1.43
0.57
0.96
0.96
0.97
0.77
1.06
0.97
0.92
0.85
0.77
0.67
0.89
0.83
Ti
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.01
0.02
0.00
0.00
0.00
0.00
0.03
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Cr
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Sum
2.99
3.02
3.01
3.00
3.05
3.03
3.00
2.99
3.04
3.03
3.01
3.00
3.03
3.05
3.02
3.00
3.03
3.07
3.04
3.04
3.05
3.01
3.02
3.05
Na
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
K
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Ca
2.01
1.98
1.98
2.00
1.94
1.97
2.00
2.01
1.95
1.97
1.99
1.99
1.97
1.95
1.98
2.00
1.97
1.93
1.96
1.95
1.95
1.99
1.98
1.95
Sum
2.01
1.98
1.99
2.00
1.95
1.97
2.00
2.01
1.96
1.97
1.99
2.00
1.97
1.95
1.98
2.00
1.97
1.93
1.96
1.96
1.95
1.99
1.98
1.95
OH
F
0.01
0.04
0.04
0.01
0.00
0.00
0.01
0.00
0.01
0.01
0.02
0.02
0.01
0.00
0.01
0.01
0.01
0.03
0.01
0.02
0.00
0.01
0.01
0.00
Cl
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
OH
0.99
0.96
0.96
0.99
1.00
1.00
0.99
1.00
0.99
0.99
0.98
0.98
0.99
1.00
0.99
0.99
0.99
0.97
0.99
0.98
1.00
0.99
0.99
1.00
Sum
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
Table A7. Chemical analyses of amphiboles from Copiapó, Chile
Locality
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
Sample
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C2J-334
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C2B-655
C2B-655
C2B-655
Spot no. Analysis no.
1
c1
1
b1
1
m2
1
b2
1
b3
1
b4
1
b6
1
a2
2
a2
2
a3
2
a4
2
a5
2
a6
2
c1
3
a1
3
a2
3
a4
3
a1
3
a2
3
a3
3
a4
3
a5
4
a1
4
a2
4
a3
4
a4
4
a5
4
t15
1
cpx1
1
cpx2
1
a1
Mineral
Magnesiohornblende
Magnesiohornblende
Magnesiohornblende
Magnesiohornblende
Magnesiohornblende
Magnesiohornblende
Magnesiohornblende
Actinolite
Magnesiohornblende
Magnesiohornblende
Magnesiohornblende
Actinolite
Magnesiohornblende
Magnesiohornblende
Magnesiohornblende
Magnesiohornblende
Magnesiohornblende
Magnesiohornblende
Magnesiohornblende
Magnesiohornblende
Magnesiohornblende
Actinolite
Magnesiohornblende
Magnesiohornblende
Actinolite
Magnesiohornblende
Magnesiohornblende
Magnesiohornblende
Actinolite
Actinolite
Actinolite
SiO2
45.87
48.56
49.57
48.80
46.97
49.15
46.96
52.04
47.87
48.24
47.25
51.83
49.46
50.85
49.96
48.95
51.25
50.17
49.40
50.98
51.43
52.41
52.00
50.46
53.13
49.62
50.74
49.97
52.69
52.54
52.82
TiO2
0.28
0.28
0.25
0.31
0.17
0.19
0.68
0.17
0.29
0.26
0.11
0.19
0.20
0.24
0.20
0.23
0.21
0.43
0.45
0.33
0.31
0.27
0.24
0.43
0.05
0.46
0.40
0.21
0.02
0.02
0.02
Al2O3
7.86
5.31
4.89
5.44
7.16
5.42
6.68
2.37
5.61
5.83
6.66
3.43
4.91
4.39
4.59
5.62
4.67
4.61
5.21
3.97
3.63
3.15
4.22
4.81
2.70
5.25
4.64
6.97
1.38
1.19
1.19
B2O3
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Cr2O3 Fe2O3
0.01
5.50
0.01
4.33
0.00
3.84
0.00
4.29
0.01
5.53
0.00
5.72
0.00
0.00
0.01
2.81
0.00
4.57
0.01
4.51
0.00
3.29
0.00
3.53
0.00
3.13
0.01
3.14
0.00
3.40
0.00
5.28
0.01
3.98
0.00
3.96
0.00
5.85
0.00
4.16
0.00
1.89
0.00
2.74
0.00
3.13
0.00
4.36
0.00
2.08
0.01
4.58
0.00
4.81
0.00
0.00
0.00
1.84
0.01
0.91
0.00
1.34
FeO
11.97
10.90
10.94
10.91
11.74
10.00
15.15
9.58
11.46
11.70
12.44
9.92
11.69
10.94
11.31
10.48
10.15
6.44
5.30
5.83
7.89
6.43
6.70
6.34
8.17
6.33
5.97
10.90
15.38
17.07
15.61
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
C2B-655
C2B-655
C2B-655
C2B-671
C2B-671
C2B-671
C2B-671
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
2
2
2
1
2
2
2
1
1
2
2
2
2
2
3
3
3
a1
a2
e1
a1
a1
a2
a3
c1
c2
b1
b2
c1
c2
c3
c1
c2
c3
Actinolite
Magnesiohornblende
Actinolite
Actinolite
Actinolite
Magnesiohornblende
Actinolite
Chloro-potassichastingsite
Chloro-potassichastingsite
Actinolite
Actinolite
Ferrohornblende
Magnesiohornblende
Magnesiohornblende
Ferro-edenite
Ferro-edenite
Edenite
53.06
50.83
53.18
51.39
52.65
50.62
52.20
35.13
35.15
52.90
51.80
46.42
47.35
47.14
46.33
46.09
46.85
0.05
0.07
0.03
0.05
0.15
0.20
0.23
0.06
0.03
0.18
0.30
1.16
0.93
1.10
1.34
1.34
1.24
1.40
3.59
1.21
3.25
2.44
3.78
2.63
10.22
11.89
1.08
1.72
6.42
5.74
5.82
6.44
6.53
6.02
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.74
3.60
0.00
2.21
1.30
4.56
1.38
8.62
8.48
1.28
2.65
0.35
0.51
0.00
0.14
0.57
0.00
14.13
12.57
13.37
12.74
10.21
10.81
10.52
25.59
24.57
17.09
18.35
19.42
19.10
19.05
19.33
19.43
18.87
IV
MgO
11.31
13.19
13.58
13.24
11.93
13.68
13.16
15.58
12.62
12.64
12.20
14.87
13.20
14.01
13.49
13.22
14.56
16.88
16.70
17.31
17.16
17.77
17.02
17.01
17.25
16.63
17.12
15.38
13.07
12.09
12.95
MnO
0.53
0.59
0.56
0.51
0.46
0.50
0.52
0.54
0.54
0.51
0.47
0.59
0.53
0.55
0.54
0.58
0.67
0.02
0.04
0.05
0.04
0.03
0.03
0.05
0.04
0.02
0.02
0.04
0.22
0.28
0.27
CaO
11.86
12.07
12.14
12.05
12.10
12.24
10.36
12.46
12.03
12.11
12.30
12.23
12.11
12.19
12.10
12.07
12.18
12.13
11.84
12.09
12.71
12.42
12.42
12.21
12.79
12.14
12.21
10.69
12.56
12.38
12.44
Na2O
0.97
0.72
0.67
0.71
0.87
0.66
0.44
0.32
0.72
0.77
0.79
0.43
0.61
0.51
0.56
0.74
0.35
0.93
1.03
0.78
0.60
0.52
0.44
0.99
0.33
0.94
0.86
0.68
0.16
0.15
0.16
K2O
0.58
0.36
0.30
0.38
0.46
0.36
1.70
0.11
0.39
0.38
0.35
0.20
0.30
0.30
0.31
0.30
1.16
0.38
0.41
0.32
0.29
0.23
0.10
0.42
0.08
0.48
0.39
0.19
0.07
0.08
0.06
H2O
1.97
1.97
1.96
2.00
1.97
2.02
1.90
2.00
1.94
1.97
1.93
2.02
1.97
1.99
2.01
1.97
2.03
1.94
1.95
1.95
1.96
1.97
2.05
1.95
2.00
1.93
1.94
1.94
1.96
1.95
1.98
F
0.03
0.09
0.12
0.04
0.08
0.05
0.14
0.09
0.11
0.09
0.11
0.08
0.09
0.13
0.04
0.14
0.12
0.22
0.18
0.20
0.17
0.20
0.08
0.24
0.14
0.22
0.26
0.15
0.09
0.06
0.05
Cl Subtotal O=F+Cl Total
0.09
98.95
-0.03
98.91
0.05
98.52
-0.05
98.47
0.07
99.00
-0.07
98.94
0.05
98.84
-0.03
98.81
0.07
99.66
-0.05
99.61
0.06 100.16
-0.03 100.13
0.05
97.85
-0.07
97.78
0.02
98.26
-0.04
98.22
0.06
98.31
-0.06
98.25
0.07
99.19
-0.05
99.13
0.05
98.03
-0.06
97.97
0.03
99.41
-0.04
99.37
0.04
98.31
-0.05
98.26
0.03
99.36
-0.06
99.30
0.04
98.62
-0.02
98.60
0.04
99.74
-0.07
99.67
0.04 101.48
-0.06 101.43
0.10
98.25
-0.11
98.14
0.11
98.50
-0.10
98.40
0.10
98.10
-0.11
97.99
0.09
98.21
-0.09
98.12
0.06
98.21
-0.10
98.11
0.00
98.47
-0.03
98.44
0.10
99.40
-0.12
99.28
0.07
98.86
-0.07
98.79
0.14
98.77
-0.12
98.65
0.10
99.49
-0.13
99.36
0.11
97.28
-0.09
97.19
0.11
99.55
-0.06
99.49
0.11
98.86
-0.05
98.81
0.10
98.98
-0.04
98.94
Si
6.86
7.20
7.29
7.20
6.95
7.16
7.10
7.61
7.15
7.14
7.09
7.51
7.33
7.42
7.37
7.17
7.34
7.29
7.16
7.38
7.46
7.55
7.47
7.25
7.63
7.19
7.27
7.36
7.76
7.83
7.82
B
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Al
1.14
0.80
0.71
0.80
1.05
0.84
0.90
0.39
0.85
0.86
0.91
0.49
0.67
0.58
0.63
0.83
0.66
0.71
0.84
0.62
0.54
0.45
0.53
0.75
0.37
0.81
0.73
0.64
0.24
0.17
0.18
M1, M2, M3, M4
Sum
Al
Mg
8.00
0.25
2.52
8.00
0.13
2.92
8.00
0.14
2.98
8.00
0.15
2.91
8.00
0.20
2.63
8.00
0.09
2.97
8.00
0.29
2.96
8.00
0.02
3.40
8.00
0.13
2.81
8.00
0.16
2.79
8.00
0.26
2.73
8.00
0.10
3.21
8.00
0.19
2.92
8.00
0.17
3.05
8.00
0.16
2.96
8.00
0.14
2.89
8.00
0.13
3.11
8.00
0.08
3.65
8.00
0.05
3.61
8.00
0.06
3.74
8.00
0.08
3.71
8.00
0.08
3.81
8.00
0.18
3.64
8.00
0.07
3.64
8.00
0.09
3.69
8.00
0.09
3.59
8.00
0.06
3.66
8.00
0.56
3.37
8.00
0.00
2.87
8.00
0.04
2.69
8.00
0.03
2.86
13.94
13.51
14.64
13.89
16.07
13.71
15.65
0.48
0.75
11.94
10.46
10.36
10.86
11.17
10.74
10.38
11.15
0.18
0.15
0.12
0.15
0.09
0.41
0.14
0.46
0.53
0.38
0.44
0.46
0.55
0.43
0.40
0.48
0.44
12.42
12.42
12.44
12.51
12.56
11.94
12.48
10.58
10.92
12.33
12.11
10.93
10.80
10.78
10.82
10.85
10.79
0.18
0.42
0.22
0.31
0.38
0.43
0.38
0.99
0.65
0.07
0.15
1.19
1.08
1.23
1.28
1.23
1.32
0.08
0.14
0.05
0.22
0.13
0.23
0.14
3.02
3.27
0.05
0.08
0.64
0.55
0.63
0.73
0.70
0.66
1.97
1.94
1.98
1.96
1.98
1.96
1.97
0.35
0.87
1.97
1.98
1.84
1.83
1.79
1.79
1.81
1.82
0.09
0.17
0.09
0.05
0.11
0.10
0.12
0.02
0.04
0.09
0.05
0.12
0.19
0.27
0.25
0.20
0.19
0.07
0.08
0.02
0.20
0.08
0.15
0.08
5.51
3.57
0.03
0.05
0.31
0.26
0.29
0.30
0.32
0.29
98.31
99.51
97.34
98.94
98.16
98.89
97.92
101.09
100.78
99.45
100.18
99.80
99.87
99.82
100.07
100.08
99.83
-0.05
-0.09
-0.04
-0.07
-0.06
-0.08
-0.07
-1.25
-0.82
-0.05
-0.03
-0.12
-0.14
-0.18
-0.18
-0.15
-0.15
98.26
99.42
97.30
98.87
98.10
98.81
97.86
99.84
99.96
99.40
100.15
99.68
99.73
99.64
99.89
99.93
99.69
7.83
7.46
7.88
7.56
7.67
7.44
7.65
5.99
5.88
7.84
7.71
7.03
7.14
7.11
7.00
6.98
7.07
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.17
0.54
0.12
0.44
0.33
0.56
0.35
2.01
2.12
0.16
0.29
0.97
0.86
0.89
1.00
1.02
0.93
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
8.00
0.08
0.08
0.09
0.12
0.09
0.09
0.10
0.04
0.22
0.03
0.01
0.18
0.16
0.15
0.15
0.14
0.14
3.07
2.96
3.23
3.05
3.49
3.00
3.42
0.12
0.19
2.64
2.32
2.34
2.44
2.51
2.42
2.34
2.51
A
2+
Fe
1.50
1.35
1.35
1.35
1.45
1.22
1.92
1.17
1.43
1.45
1.56
1.20
1.45
1.33
1.39
1.28
1.22
0.78
0.64
0.71
0.96
0.77
0.80
0.76
0.98
0.77
0.72
1.34
1.90
2.13
1.93
Fe3+
0.62
0.48
0.42
0.48
0.62
0.63
0.00
0.31
0.51
0.50
0.37
0.38
0.35
0.34
0.38
0.58
0.43
0.43
0.64
0.45
0.21
0.30
0.34
0.47
0.22
0.50
0.52
0.00
0.20
0.10
0.15
Mn
0.07
0.07
0.07
0.06
0.06
0.06
0.07
0.07
0.07
0.06
0.06
0.07
0.07
0.07
0.07
0.07
0.08
0.00
0.00
0.01
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.01
0.03
0.04
0.03
Ti
0.03
0.03
0.03
0.03
0.02
0.02
0.08
0.02
0.03
0.03
0.01
0.02
0.02
0.03
0.02
0.02
0.02
0.05
0.05
0.04
0.03
0.03
0.03
0.05
0.01
0.05
0.04
0.02
0.00
0.00
0.00
Cr
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Ca
1.90
1.92
1.91
1.91
1.92
1.91
1.68
1.95
1.92
1.92
1.98
1.90
1.92
1.90
1.91
1.89
1.87
1.89
1.84
1.88
1.98
1.92
1.91
1.88
1.97
1.88
1.87
1.69
1.98
1.98
1.97
Sum
6.90
6.92
6.91
6.91
6.92
6.91
7.00
6.95
6.92
6.92
6.98
6.90
6.92
6.90
6.91
6.89
6.87
6.89
6.84
6.88
6.98
6.92
6.91
6.88
6.97
6.88
6.87
7.00
6.98
6.98
6.97
Na
0.28
0.21
0.19
0.20
0.25
0.19
0.13
0.09
0.21
0.22
0.23
0.12
0.18
0.14
0.16
0.21
0.10
0.26
0.29
0.22
0.17
0.14
0.12
0.28
0.09
0.26
0.24
0.20
0.05
0.04
0.05
K
0.11
0.07
0.06
0.07
0.09
0.07
0.33
0.02
0.07
0.07
0.07
0.04
0.06
0.06
0.06
0.06
0.21
0.07
0.08
0.06
0.05
0.04
0.02
0.08
0.02
0.09
0.07
0.04
0.01
0.02
0.01
□
0.61
0.72
0.75
0.73
0.66
0.75
0.54
0.89
0.72
0.71
0.70
0.84
0.77
0.80
0.78
0.73
0.69
0.67
0.64
0.72
0.78
0.81
0.86
0.65
0.89
0.65
0.69
0.77
0.94
0.94
0.94
Sum
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
OH
F
0.02
0.04
0.05
0.02
0.04
0.02
0.07
0.04
0.05
0.04
0.05
0.04
0.04
0.06
0.02
0.06
0.05
0.10
0.08
0.09
0.08
0.09
0.03
0.11
0.06
0.10
0.12
0.07
0.04
0.03
0.02
Cl
0.02
0.01
0.02
0.01
0.02
0.01
0.01
0.00
0.02
0.02
0.01
0.01
0.01
0.01
0.01
0.01
0.01
0.02
0.03
0.02
0.02
0.02
0.00
0.02
0.02
0.03
0.03
0.03
0.03
0.03
0.03
OH
1.96
1.94
1.93
1.97
1.94
1.96
1.92
1.95
1.93
1.94
1.94
1.96
1.95
1.93
1.97
1.93
1.94
1.88
1.89
1.88
1.90
1.89
1.97
1.87
1.92
1.87
1.86
1.91
1.93
1.94
1.95
Sum Mg/Mg+Fe
2.00
0.63
2.00
0.68
2.00
0.69
2.00
0.68
2.00
0.64
2.00
0.71
2.00
0.61
2.00
0.74
2.00
0.66
2.00
0.66
2.00
0.64
2.00
0.73
2.00
0.67
2.00
0.70
2.00
0.68
2.00
0.69
2.00
0.72
2.00
0.82
2.00
0.85
2.00
0.84
2.00
0.79
2.00
0.83
2.00
0.82
2.00
0.83
2.00
0.79
2.00
0.82
2.00
0.84
2.00
0.72
2.00
0.60
2.00
0.56
2.00
0.60
1.74
1.54
1.66
1.57
1.25
1.33
1.29
3.65
3.44
2.12
2.28
2.46
2.41
2.40
2.44
2.46
2.38
0.08
0.40
0.00
0.24
0.14
0.50
0.15
1.11
1.07
0.14
0.30
0.04
0.06
0.00
0.02
0.07
0.00
0.02
0.02
0.01
0.02
0.01
0.05
0.02
0.07
0.08
0.05
0.06
0.06
0.07
0.06
0.05
0.06
0.06
0.01
0.01
0.00
0.01
0.02
0.02
0.03
0.01
0.00
0.02
0.03
0.13
0.11
0.13
0.15
0.15
0.14
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
1.97
1.95
1.97
1.97
1.96
1.88
1.96
1.93
1.96
1.96
1.93
1.77
1.74
1.74
1.75
1.76
1.74
6.97
6.95
6.97
6.97
6.96
6.88
6.96
6.93
6.96
6.96
6.93
7.00
7.00
7.00
7.00
7.00
7.00
0.05
0.12
0.06
0.09
0.11
0.12
0.11
0.33
0.21
0.02
0.04
0.35
0.32
0.36
0.38
0.36
0.39
0.02
0.03
0.01
0.04
0.02
0.04
0.03
0.66
0.70
0.01
0.02
0.12
0.11
0.12
0.14
0.13
0.13
0.93
0.85
0.93
0.87
0.87
0.83
0.87
0.02
0.09
0.97
0.94
0.53
0.58
0.52
0.48
0.50
0.49
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
1.00
0.04
0.08
0.04
0.02
0.05
0.05
0.06
0.01
0.02
0.04
0.02
0.06
0.09
0.13
0.12
0.09
0.09
0.02
0.02
0.01
0.05
0.02
0.04
0.02
1.59
1.01
0.01
0.01
0.08
0.07
0.07
0.08
0.08
0.07
1.94
1.90
1.95
1.93
1.93
1.92
1.92
0.40
0.97
1.95
1.96
1.86
1.84
1.80
1.80
1.82
1.83
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
0.64
0.66
0.66
0.66
0.74
0.69
0.73
0.03
0.05
0.55
0.50
0.49
0.50
0.51
0.50
0.49
0.51
Table A8. Chemical analyses of oxides from Copiapó, Chile
Locality
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Bronce Estrella
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Buitre Radio Tower
Cerro Granate
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Cerro Negro Norte
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Falla Ojancos Transito San Francisco
Jesus Maria
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
Sample
C2B-298
C2B-298
C2B-708
C2J-124
C2J-334
C2J-334
C2J-334
C2J-334
C2B-576c
C3B-072a
C6B-076
C6B-076
C6B-076
C6B-076
C6B-076
C6B-101b
C6B-160b
C6B-160b
C6B-160b
C6B-160b
C6B-160b
C7B-003a
C2B-352e
C2B-352e
C2B-655
C2B-671
C2B-671
C2B-671
C2B-671
C2B-808.2
C2B-808.2
Spot no. Analysis no.
1
s1
1
r1
2
h1
3
h2
1
h1
2
m1
3
m1
3
m2
1
h1
2
h1
1
o1
1
o2
2
m1
2
m2
4
m2
1
i1
1
r1
1
h1
1
h2
2
h1
2
s1
3
m1
1
h1
1
s1
1
m1
2
s1
4
s1
4
s2
4
s3
2
s1
2
s2
Mineral
Titanite
Rutile
Hematite
Hematite
Magnetite
Magnetite
Titanite
Ilmenite
Magnetite
Hematite
Titanite
Titanite
Magnetite
Magnetite
Magnetite
Ilmenite
Rutile
Hematite
Hematite
Hematite
Rutile
Hematite
Ilmenite
Titanite
Magnetite
Titanite
Titanite
Titanite
Titanite
Titanite
Titanite
SiO2
29.95
0.06
0.00
0.06
0.07
0.09
29.79
0.04
0.25
0.31
29.84
29.77
1.98
0.14
0.12
0.15
0.26
0.09
0.07
0.07
0.36
0.00
0.03
31.31
1.01
29.91
29.39
29.50
29.93
30.34
30.21
TiO2
35.23
99.15
0.03
9.01
0.12
0.15
39.08
48.25
0.13
0.53
36.18
37.48
0.04
0.04
0.02
47.45
97.80
10.04
8.40
15.39
97.64
4.52
49.03
28.66
0.07
37.40
36.56
37.40
37.60
37.50
36.78
Al2O3
2.95
0.00
0.59
0.12
0.09
0.05
0.71
0.00
0.23
0.64
2.03
1.42
0.47
0.15
0.06
0.08
0.02
0.16
0.14
0.09
0.00
0.35
0.00
7.87
0.40
0.94
1.02
0.91
1.02
1.38
1.98
Cr2O3
0.01
0.03
0.00
0.02
0.03
0.06
0.00
0.00
0.01
0.00
0.00
0.00
0.01
0.02
0.01
0.04
0.01
0.03
0.03
0.03
0.00
0.03
0.00
0.00
0.01
0.07
0.00
0.00
0.00
0.00
0.00
Fe2O3
1.12
0.64
98.01
79.92
100.13
99.00
1.00
7.67
96.63
96.44
1.05
0.86
96.15
100.03
98.77
6.36
1.07
79.00
83.12
67.77
0.98
90.17
6.56
0.73
99.84
0.81
1.56
1.20
1.33
1.33
1.50
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
San Gregorio S Granate
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
Santos PdC
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
C2B-808.2
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH289-037.5a
DDH291-188.4
DDH291-188.4
DDH384-004.2
DDH628-094.2
DDH628-151.6
DDH643-595.5
DDH684-079.8
ME013-538
2
3
3
3
3
3
1
1
1
1
1
2
2
3
3
3
2
2
1
2
1
1
3
3
1
2
h1
i1
m1
m2
i2
m3
h1
r1
r2
r3
r4
r1
r2
r1
r2
r3
h1
h2
h1
m1
h1
h1
m1
m1
m1
s1
Magnetite
Ilmenite
Magnetite
Magnetite
Ilmenite
Magnetite
Magnetite
Rutile
Rutile
Rutile
Rutile
Ilmenite
Ilmenite
Rutile
Ilmenite
Rutile
Magnetite
Magnetite
Magnetite
Magnetite
Hematite
Hematite
Magnetite
Magnetite
Magnetite
Titanite
0.07
0.03
0.08
0.07
0.05
0.06
0.47
0.13
6.95
0.06
0.15
0.02
0.04
0.06
8.94
0.32
1.15
0.19
0.51
0.36
0.02
0.94
0.15
0.17
2.95
30.31
1.35
51.12
1.75
1.78
49.11
1.43
3.59
97.10
66.77
98.73
97.86
50.34
49.87
98.18
36.36
91.91
0.09
0.03
0.07
0.03
0.00
0.08
0.02
0.02
0.05
38.17
1.36
0.00
0.74
0.77
0.00
0.49
0.26
0.02
0.19
0.00
0.02
0.00
0.02
0.02
8.62
0.04
0.48
0.07
0.17
0.04
0.08
0.47
0.04
0.04
0.07
1.23
0.03
0.00
0.03
0.04
0.00
0.04
0.16
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.02
0.05
0.62
0.49
0.00
0.01
0.00
0.01
0.01
0.07
98.00
3.60
97.35
97.78
6.62
98.01
96.35
2.46
18.53
0.60
0.77
4.62
4.99
1.36
8.56
4.92
99.30
100.75
101.50
101.53
99.67
100.29
100.38
101.76
92.33
1.16
VI
FeO
0.00
0.00
0.00
7.80
0.00
0.00
0.00
39.25
0.20
0.66
0.00
0.00
0.58
0.04
0.00
37.65
0.00
9.10
7.42
13.81
0.00
4.01
42.05
0.00
0.31
0.00
0.00
0.00
0.00
0.00
0.00
MgO
0.00
0.02
0.03
0.04
0.00
0.03
0.00
0.36
0.03
0.00
0.03
0.00
0.46
0.03
0.00
0.05
0.00
0.02
0.05
0.01
0.00
0.02
0.05
0.00
0.07
0.00
0.00
0.00
0.00
0.01
0.00
MnO
0.00
0.00
0.01
0.04
0.18
0.11
0.09
3.37
0.04
0.00
0.00
0.00
0.00
0.04
0.00
4.95
0.03
0.00
0.01
0.01
0.01
0.00
1.88
0.00
0.05
0.00
0.00
0.03
0.04
0.03
0.01
CaO
28.53
0.18
0.00
0.01
0.05
0.16
27.83
0.02
0.08
0.02
27.92
27.88
0.29
0.03
0.08
0.05
0.01
0.00
0.00
0.02
0.03
0.02
0.00
28.54
0.22
27.94
27.34
27.49
27.91
28.21
28.42
Na2O
0.01
0.01
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.02
0.00
0.00
0.05
0.00
0.01
0.00
0.03
0.00
0.02
0.01
0.00
0.00
0.01
0.02
0.07
0.00
0.03
0.00
0.00
0.00
0.02
K2O
0.01
0.01
0.04
0.07
0.01
0.01
0.14
0.01
0.00
0.02
0.00
0.01
0.14
0.00
0.06
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.06
0.00
0.00
0.00
0.01
0.01
0.01
H2O
0.53
0.00
0.01
0.00
0.00
0.01
0.23
0.01
0.00
0.02
0.30
0.13
0.06
0.00
0.02
0.00
0.03
0.00
0.00
0.00
0.04
0.02
0.01
1.52
0.01
0.23
0.23
0.16
0.06
0.47
0.54
Cl
0.01
0.01
0.00
0.01
0.01
0.00
0.00
0.01
0.01
0.01
0.00
0.00
0.08
0.00
0.10
0.02
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.01
0.00
0.01
0.00
Subtotal O=F+Cl
98.35
-0.23
100.12
0.00
98.72
0.00
98.00
0.00
101.12
0.00
100.00
-0.01
100.62
-0.10
101.06
-0.01
97.62
0.00
98.66
-0.01
99.03
-0.13
99.21
-0.06
100.34
-0.04
100.61
0.00
99.31
-0.03
96.79
0.00
103.90
-0.01
99.28
0.00
100.08
0.00
98.20
0.00
103.51
-0.02
99.15
-0.01
101.70
0.00
99.99
-0.64
102.11
0.00
97.31
-0.10
96.13
-0.10
96.70
-0.07
97.90
-0.03
101.02
-0.20
101.26
-0.23
Total
98.13
100.12
98.72
98.00
101.12
99.99
100.52
101.05
97.61
98.65
98.91
99.16
100.30
100.61
99.28
96.79
103.88
99.28
100.08
98.20
103.50
99.14
101.70
99.36
102.11
97.21
96.04
96.63
97.88
100.83
101.03
Si
0.98
0.00
0.00
0.00
0.00
0.00
0.97
0.00
0.01
0.01
0.98
0.98
0.05
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
1.00
0.03
1.00
1.00
0.99
0.99
0.98
0.97
3+
Fe
0.03
0.01
1.98
1.61
1.98
1.98
0.02
0.14
1.97
1.94
0.03
0.02
1.89
1.98
1.99
0.12
0.01
1.57
1.64
1.36
0.01
1.81
0.12
0.02
1.94
0.02
0.04
0.03
0.03
0.03
0.04
Fe2+
0.00
0.00
0.00
0.18
0.00
0.00
0.00
0.82
0.00
0.01
0.00
0.00
0.01
0.00
0.00
0.82
0.00
0.20
0.16
0.31
0.00
0.09
0.88
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.87
41.08
1.32
1.26
40.21
1.18
3.05
0.00
0.00
0.00
0.00
33.69
33.11
0.00
22.80
0.00
0.44
0.00
0.24
0.45
0.00
0.27
0.14
0.06
3.51
0.00
0.04
0.02
0.00
0.02
0.11
0.00
0.05
0.00
0.02
0.00
0.00
0.00
0.00
0.00
6.60
0.00
0.06
0.01
0.02
0.00
0.00
0.05
0.00
0.00
0.03
0.00
0.12
4.48
0.20
0.17
3.57
0.12
0.04
0.04
3.60
0.00
0.03
11.36
11.52
0.04
7.89
1.54
0.04
0.10
0.05
0.00
0.00
0.04
0.01
0.05
0.00
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.04
0.06
6.39
0.03
0.11
0.06
0.00
0.06
0.64
0.13
0.19
0.03
0.04
0.01
0.24
0.29
0.00
0.08
0.00
28.31
0.01
0.02
0.01
0.03
0.03
0.00
0.09
0.00
0.01
0.00
0.01
0.00
0.00
0.01
0.00
0.04
0.05
0.01
0.04
0.00
0.01
0.07
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.04
0.01
0.00
0.01
0.00
0.00
0.04
0.00
0.00
0.02
0.13
0.10
0.04
0.00
0.00
0.04
0.01
0.00
0.00
0.05
0.01
0.02
0.00
0.01
0.06
0.00
0.00
0.00
0.31
0.04
0.04
0.04
0.01
0.00
0.02
0.01
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.28
0.01
0.00
0.00
0.00
0.00
0.00
0.05
0.04
0.02
0.00
0.02
0.00
0.00
0.00
0.03
0.06
0.00
0.21
0.00
0.00
0.01
0.03
0.00
0.01
0.00
0.00
102.86
102.97
102.43
102.87
101.98
102.17
104.51
104.21
104.82
103.54
103.20
102.29
101.72
104.09
102.52
103.52
101.99
101.60
103.30
102.92
100.03
102.59
100.75
102.21
98.97
99.59
-0.01
-0.01
0.00
0.00
-0.03
0.00
-0.01
-0.01
-0.14
-0.02
-0.02
-0.02
0.00
0.00
-0.02
-0.02
0.00
-0.05
0.00
0.00
0.00
-0.01
0.00
0.00
0.00
-0.12
102.85
102.96
102.43
102.87
101.95
102.17
104.50
104.20
104.68
103.52
103.17
102.28
101.72
104.09
102.51
103.50
101.99
101.55
103.30
102.92
100.02
102.59
100.75
102.20
98.97
99.47
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.08
0.00
0.00
0.00
0.00
0.00
0.20
0.00
0.03
0.01
0.01
0.01
0.00
0.02
0.00
0.00
0.08
0.99
1.89
0.07
1.89
1.89
0.12
1.91
1.83
0.02
0.17
0.01
0.01
0.09
0.09
0.01
0.14
0.05
1.93
1.98
1.96
1.97
1.99
1.94
1.99
1.99
1.84
0.03
0.02
0.84
0.03
0.03
0.83
0.03
0.06
0.00
0.00
0.00
0.00
0.70
0.69
0.00
0.42
0.00
0.01
0.00
0.01
0.01
0.00
0.01
0.00
0.00
0.08
0.00
O
Ti
0.87
0.99
0.00
0.18
0.00
0.00
0.96
0.91
0.00
0.01
0.89
0.92
0.00
0.00
0.00
0.93
0.94
0.20
0.17
0.31
0.94
0.09
0.92
0.69
0.00
0.94
0.93
0.95
0.94
0.91
0.89
Mg
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.02
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Mn
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.07
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.11
0.00
0.00
0.00
0.00
0.00
0.00
0.04
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Ca
1.00
0.00
0.00
0.00
0.00
0.00
0.97
0.00
0.00
0.00
0.98
0.98
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.97
0.01
1.00
0.99
0.99
0.99
0.98
0.98
Al
0.11
0.00
0.02
0.00
0.00
0.00
0.03
0.00
0.01
0.02
0.08
0.05
0.01
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.01
0.00
0.29
0.01
0.04
0.04
0.04
0.04
0.05
0.08
Na
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
K
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Cr
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
Sum
3.00
1.00
2.00
2.00
2.00
2.00
3.00
2.00
2.00
2.00
3.00
3.00
2.00
2.00
2.00
2.00
1.00
2.00
2.00
2.00
1.00
2.00
2.00
3.00
2.00
3.00
3.00
3.00
3.00
3.00
3.00
F
0.06
0.00
0.00
0.00
0.00
0.00
0.02
0.00
0.00
0.00
0.03
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.15
0.00
0.02
0.02
0.02
0.01
0.05
0.06
Cl
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
O
5.94
6.00
6.00
6.00
6.00
6.00
5.98
6.00
6.00
6.00
5.97
5.99
5.99
6.00
5.99
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
5.85
6.00
5.98
5.98
5.98
5.99
5.95
5.94
Total
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
0.03
0.94
0.03
0.03
0.92
0.03
0.07
0.93
0.61
0.95
0.95
0.94
0.93
0.94
0.60
0.88
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.94
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.22
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.09
0.00
0.00
0.08
0.00
0.00
0.00
0.04
0.00
0.00
0.24
0.24
0.00
0.15
0.02
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.08
0.00
0.00
0.00
0.00
0.00
0.02
0.00
0.01
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.99
0.04
0.00
0.02
0.02
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.22
0.00
0.01
0.00
0.01
0.00
0.00
0.01
0.00
0.00
0.00
0.05
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.01
0.00
0.00
0.00
0.00
0.00
0.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
1.00
1.00
1.00
1.00
2.00
2.00
1.00
2.00
1.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
2.00
3.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.03
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.01
0.00
0.00
0.00
0.00
0.00
0.00
0.00
0.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
5.99
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
5.99
6.00
6.00
6.00
6.00
6.00
6.00
6.00
5.97
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00
6.00