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LOS ALAMOS NATIONAL LABORATORYSUBMITTAL FORM FOR LA-SERIES REPORTS
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D. L. Bish and D. T. Vannan, ESS-1, MS J978Program Code
TITLEMINERALOGIC SUMMARY OF YUCCA MOUNTAIN, EVADA
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Form S95R11 Block No. ST-28432/62
MINERALOGIC SUMMARY OF YUCCA MOUNTAIN, NEVADA
by
D. L. Bish and D. T. Vaniman
ABSTRACT
Quantitative x-ray powder diffraction analysis of tuffs andsilicic lavas, using matrix-flushing techniques, has been used toobtain a model of three-dimensional mineral distributions at YuccaMountain, Nevada. This method of analysis is especially useful intuff, where the most abundant phases are commonly too fine grainedfor optical determination. The three-dimensional distributions ofprimary glass and of tridymite are particularly well constrained.Vitric nonwelded glasses occur above and below the welded devitrifiedTopopah Spring Membef, but the glass in the lower nonwelded vitriczone is progressively altered to zeolites to the east where the zoneis closer to the static water level. The zeolites clinoptilolite,mordenite, heulandite, and erionite have all been found at YuccaMountain, but only mordenite and clinoptilolite are abundant and canbe mapped between many drill holes and at many depths. Heulanditedistribution is also mappable, but only below the densely weldeddevitrified part of the Topopah Spring Member. Erionite has beenconfirmed only once, as a fracture coating. There is a fairlycontinuous smectite-rich interval nmuediately above the basalvitrophyre of the Topopah Spring Member, but no evidence suggeststhat the smectites can provide information on the paleogroundwatertable. There are at least four mappable zeolitized zones in YuccaMountain, and the thicker zones tend to coincide with intervals thatretained glass following early tuff devitrification. Problems inextrapolation occur where zones of welding pinch out. No phillipsitehas been found, and some samples previously reported to containphillipsite or erionite were reexamined with negative results. Thedeeper alteration to albite and analcime was not sampled in everydrill hole, and the distribution of these phases is difficult to map.
I. INTRODUCTION
Yucca ountain and surroundings, near the southwestern boundary of the
Nevada Test Site (NTS) in south-central Nevada, are being studied to assess
1
the suitability of the area to host a geologic repository for high-level radio-
active waste. Research In this area, sponsored by the Nevada Nuclear Waste
Storage Investigations (NNWSI) project of the U.S. Department of Energy
(DOE), includes detailed studies of the mineralogy and petrology of the rocks
in and surrounding Yucca Mountain. Results of these studies (Bish et al.
1981; Caporusclo et al. 1982; Levy 1984a; Vaniman et al. 1984) are yielding a
detailed three-dimensional model of the Yucca Mountain area and are par-
ticularly mportant in predicting the effects a repository would have on the
ground-water/rock system (Bish et al. 1984a). An integral part of
mineralogy-petrology studies is the analysis of the rocks to determine the
phases present. This has been done by x-ray powder diffraction (XRD) on the
rocks at Yucca Mountain, which often have a very fine-grained groundmass that
is not amenable to quantitative mineral analysis by optical techniques (Byers,1985). Because rocks in Yucca Mountain will provide the ultimate containment
of radioactive wastes, it is important that we have a thorough knowledge ofthe distribution of potentially sorptive and changeable phases. To understand
the relationship between retardation of radionuclides and the phases present
in the repository environment, studies are underway to test the correlation
between mineralogy and sorption for numerous radionuclides (Bish et al.
1984b). These investigations have shown that the minerals clinoptilolite,
mordenite, and smectite have particularly high sorption ratios for many
cationic radionuclides.
Smyth (1982) and Bish et al. (1981) have discussed the potential for
reaction of clinoptilolite and smectite to other minerals (e.g., analcime and
lite) in a repository environment in the rocks at Yucca Mountain. These
reactions occur primarily in response to increased temperatures and can pro-
duce significant amounts of water and result in volume decreases. Therefore,
it s necessary to know the mineral distribution near the proposed repository
horizon to avoid or plan for such potential reactions in construction. Lappin
(1982) and Lappin et al. (1982) related the thermal properties of tuff,
including matrix thermal conductivity and thermal expansion, to the bulk-rock
mineralogy. They also discussed the relationship between mechanical proper-
ties and mineralogy, pointing out that additional data on rock fabric arerequired to predict bulk properties accurately. X-ray data on Yucca Mountain
tuff samples also explain some variations in mechanical properties of the
tuffs (Price et al. 1984).
2
This preliminary report summarizes current investigations of Yucca
Mountain mineralogy. In addition, this report describes the methods used to
obtain the data and the limitations of the data. Finally, it addresses
questions about the occurrence of erionite and the relationship of mineralogy
to paleogroundwater table.
II. ANALYTICAL TECHNIQUES
Sample Handling, Analysis, and Identification
The x-ray data presented in the appendix were obtained either on core
and sidewall samples, for which accurate depth designations are given, or on
drill cuttings samples, for which depths are approximate within a range of
about 10 ft (3.28 m). Where core was available, 15 to 20 of material were
crushed n a shatterbox to provide a large, homogeneous sample. A portion of
this powder was ground in a mortar and pestle under acetone to approximately
-325 mesh (45 m). A modification of this procedure was applied to the most
recent analysis of samples from USW T-1 and USW W1-2, which were ground under
acetone in an automatic Binkmann Retsch mill with agate mortar and pestle to
less than S um. This fine crystallite size is necessary to ensure adequate
particle statistics (Klug and Alexander, 1974, pp. 365-367).
The resultant fine powder was gently packed into a 22- X 44-mm cavity in
a glass slide; this cavity area is sufficient for the sample area to fully
contain the x-ray beam at the lowest angle of interest. All unused powdered
samples were stored in plastic vials. Samples from Drill Hole USW G-4 were
mounted on a sample spinner in the diffractometer; the other samples were
examined stationary.
All diffraction patterns were obtained on a Siemens D-500 powder diffrac-
tometer using a copper-target x-ray tube and a diffracted-beam onochromater.
The diffractometer was run from 2.0' to 36.0 2 in the continuous scan mode
at a scanning rate of 1/min for samples from Drill Hole USW G-2 and G-4.
Data for the remaining samples were collected automatically in the step scan
mode with a step size of 0.02* 20 and count times between 1.2 and 2.0 s per
step. Several samples were run for count times up to 55 s per step to improve
detection limits and to check for trace phases.
Minerals were identified by comparison of observed patterns to standard
patterns produced in this laboratory and by comparison to published standards
from the Joint Committee on Powder Diffraction Standards (JCPDS). Clay
3
mineral standards were obtained from the Clay Minerals Society Source Clay
Repository, and zeolite standards were recently obtained from Minerals
Research Corporation, Clarkson, New York.
Quantitative Measurements
In contrast to qualitative identifications of the phases present in
tuffs, quantitative multicomponent analysis is more difficult, time consuming,
and s not straightforward because of a number of factors. These factors
include variations in the degree of preferred orientation of crystallites,
variations in crystallite size, variations in degree of crystallinity, and
variations in composition (crystalline solid solution). In addition, the
complex diffraction patterns often show peaks from at least six major phases,
and the method of intensity measurement where there are complex peak overlaps
affects quantitative results. Finally, because standards are required for
quantitative analysis, the choice of standards plays a critical role. In our
investigation, both natural materials and computer-calculated patterns were
used as standards.
In order to eliminate or minimize the above sample problems, samples were
finely ground as described above. Variations in feldspar composition were
partially overcome by choosing x-ray diffraction lines that are not signifi-
cantly affected by crystalline solid solution. Variations in the compositions
of other minerals, e.g., clinoptilolite, mordenite, and smectite, were not
compensated for, but errors thus introduced are likely to be smaller than
those introduced by orientation effects and by problems with peak overlap.
All of our analyses used integrated peak intensities (area measurements)
rather than peek heights to compensate for variations in the degree of
crystallinity.
Integrated intensities for all but USW G-2 and G-1 samples were obtained
using the Siemens first derivative peak search routine; this algorithm yields
fairly precise integrated intensities for resolved peaks (e.g., *%). Data
for USW G-2 and G-1 samples employed peak intensities, and the results are not
as accurate or precise as the more recent data. Precisions are listed in the
appendix tables and are based on errors due to counting statistics, sample
preparation, and compositional variations.
Most of our data on overlapping peaks were obtained using the first
derivative routine, which divides the intensity of overlapping peaks at the
midpoint between the peaks. Closely overlapping but partially resolved peaks
4
are a probl. mainly with rocks containing tridymite, cristobalite, quartz,
and alkali feldspar. Overlapping peaks of these phases are now decomposed
using a Gaussian peak profile, and this technique was used for data from USW
WiT-1 and USW T-2. Completely overlapping peaks of ordenite and clinop-tilolite or of the several alkali feldspars were not decomposed. Instead, thenonoverlapping peaks were used for estimating the abundances of mordenite andclinoptilolite. Because peaks of the alkali feldspars were chosen that arerelatively insensitive to compositional changes, overlapping peaks could beused. In many tuff samples, there are at least four separate feldspar speciespresent: groundmass and phenocryst feldspar, both of which have exsolvedan additional feldspar. The resultant diffraction pattern is so complex thatIt is usually difficult to determine the exact nature of the individualfeldspar phases.
The technique employed in our laboratory for quantitative analysis isknown as the matrix-flushing method or the external standard method (Chung
1974a). This technique requires the use of reference intensities that, asChung (1974a) pointed out, vary depending on instrumental conditions anddesign. We have determined the reference intensity ratios (RIR) (the ratio ofthe integrated intensity of a given reflection of a phase to the integratedintensity of the 113 reflection of Linde A corundum in a 1:1 mixture, byweight,) for several phases found in Yucca Mountain tuffs, but many mineralscould not be isolated in pure form. Smectite from Drill Hole USW G-1 1415 wasisolated by centrifugation, clinoptilolite was obtained from the Nevada TestSite in Drill Hole UE4P-1660, and quartz crystals were obtained from Hot
Springs, Arkansas. The value of the RIR for calcite was taken from Chung(1974a). Calculated RIR values were used for the remaining phases, the datacoming mainly from Borg and Smith (1969). Where possible, RIR values wereobtained for more than one peak per phase; for example, the RR for the quartz100 reflection is 0.95 and the RIR for the 101 reflection is 4.32. We haverecently obtained pure samples of sanidine, cristobalite, clinoptilolite,mordenite, analcime, biotite, and albite; and RIR values will be experi-mentally determined for all of these phases in the near future. Estimates ofthe percentage of glass in samples were based on the intensity of the
amorphous hump" centered on 23 2e, and precision is poorer forglass-containing samples than for those containing no glass.
5
To analyze the x-ray data, we solve the following equation, which is
derived by Chung (1974b):
xi (I E )
where X is the unknown weight fraction of phase i in a mixture, k is the RIR
for phase , and is the integrated intensity of the appropriate line of
phase . This equation is derived using the constraint that ZX1 C 1, and the
resultant equation flushes" out the absorption coefficients by ratioing the
reference intensity ratios k for each phase. This technique is commonly
referred to as the matrix-flushing method.
Norm Calculations
To test the validity of our quantitative results, CIPW norms (Barth 1952)
were calculated for a suite of samples from the devitrified Topopah Spring
Member in Drill Hole USW G-I using x-ray fluorescence analyses from Zelinsky
(1983). Results of these calculations are presented in Table I, and they show
that the Topopah Spring Member contains -^57 to 59X normative feldspar. This
calculation is valid for comparison with the x-ray diffraction data because
the devitrified Topopah Spring Member consists of 981 feldspar plus silica
polymorphs. The feldspar values in Appendix A for samples from the devitri-
fied Topopah Spring Member agree well with the norm calculations. However,
the most recent analyses for feldspar are slightly high, suggesting that the
RIR for feldspar used in our analyses may be too small. This will be checked
with our new standards.
Precision of Results
Quantitative x-ray diffraction traditionally yields only semiquantitative
results, and, because of the problems discussed above, quantitative x-ray
diffraction results will never have the high precision of typical chemical
analyses. When estimating uncertainties of our determined values, errors due
to peak integration, crystalline solution, sample-to-standard variability, and
peak overlap were considered. Quartz has no significant crystalline solution,
quartz standards should be similar to samples, and the quartz peaks are easily
integrated. Our new peak-decomposition technique allows greater precision to
be obtained in feldspar, cristobalite, and tridymite analyses, although
feldspars exhibit exceptionally large amounts of crystalline solution and
sample-to-standard variability.
6
TABLE I
CALCULATED CIPW NORMATIVE COMPOSITIONS OF WELDED, DEVITRIFIED PORTIONSOF THE TOPOPAH SPRING MEMBER, PAINTBRUSH TUFF
Gl-755 Gl-765 Gl-9288 Gl-1185a G-1252
S102 minerals 37.3 37.5 37.7 38.5 38.1
Corundum 0.9 1.0 1.2 1.4 1.2
Orthoclase 29.3 29.4 29.4 29.1 28.7
Plagioclase 29.9 29.7 29.4 28.1 29.5
(Total Feldspar) (59.2) (59.2) (58.8) (57.2) (58.2)
Orthopyroxene 0.4 0.4 0.4 0.8 0.6
Ilmenite 0.1 0.1 0.1 0.2 0.1
Hematite 2.1 1.8 1.8 1.9 1.8
aBased on x-ray fluorescence analyses reported in Zielinsky (1983).Normative compositions are reported as weight percentages forcomparison to x-ray diffraction data.
III. A THREE-DIMENSIONAL INTERPRETATION OF MINERAL DISTRIBUTIONS AT YUCCA
MOUNTAIN
Geologic cross sections In Appendix B show six mineral types plus glass
at Yucca Mountain. These cross sections are based on recent mapping by Scott
and Bonk (1984). Several drill holes shown in Fig. B-1 provide the database
for these cross-sections. Some of the drill holes for which x-ray data are
tabulated in this report have. been projected onto these cross sections (Fig.
B-1) in order to make the most use of available data. Where such projections
occur, an attempt was made to align the projections along the strike of major
structural blocks. The only exception is the projection of UE-25b#1 directly
onto the trace of Drill Hole UE-25a#1 because these drill holes are so closely
spaced.
The cross sections in Appendix B show the apparent distribution of pri-
mary glass and tridymite; primary and secondary quartz; secondary smectite,
clinoptilolite plus mordenite, analcime, and albite. Nearly ubiquitous
minerals such as alkali feldspars and cristobalite or rare minerals such as
fluorite and cryptomelane are not shown.
7
The basic data for this report are found in the tables of Appendix A;
Appendix B is an interpretation of the tabular data in a form that is easier
to visualize. Other data sources have also been used to help construct
Appendix (Bentley 1983; Bish et al. 1981; Caporuscio et al. 1982; Carroll et
al. 1981; Craig et al. 1983; Levy 1984a). One cross section showing the
apparent distribution of authigenic albite is based on microscope and electron
microprobe analyses from Bish et al. (1982) and Caporuscio et al. (1982)
rather than from the x-ray diffraction data in Appendix A. The cross sections
in Appendix are not final mineral distribution models and may be revised by
new data or interpretations.
Glass
Glass occurs both above and below the potential repository host rock at
Yucca Mountain (the welded devitrified Topopah Spring Member, or Tptw in
Appendix 8). In Appendix B Fig. -2, the glasses are divided into two cate-
*gories, vitrophyre and nonwelded. The vitrophyre is a zone of densely welded
glass at the base of the Tptw unit; this zone would first be encountered in
aqueous transport downward from a repository in the overlying devitrified
Tptw. The nonwelded glass occurs both above and below the Tptw unit. The
nonwelded porous glass is more abundant than the vitrophyre across most of
Yucca Mountain. However, the lower nonwelded vitric zone thins and disappears
to the east where the stratigraphic dip and structural displacements bring the
basal Tptw glassy zone closer to the static water level. The vitric nonwelded
material may have important paleohydrologic significance because the preserva-
tion of open shards and pumice made of nonwelded glass is rare below past
water levels (Hoover 1968). Glasses are more likely to be preserved in some
dense rock types (e.g., lavas and vitrophyres) well below the static water
level.
Both the vitrophyre and the nonwelded glass provide potentially reactive
material at Yucca Mountain. Although glass alteration rates are generally
slow, the thermal pulse of early repository history has the effect of
accelerating these reactions or of thermomechanically altering the current
exposure of glass to water either by fracturing the glass or by changing the
movement of water. Experimental data are being sought to determine whether
such effects could be significant for repository performance. The glasses are
also the only rock types that retain significant amounts of ferrous iron above
the deeper zones of reduced (sulfide) alteration (Caporuscio and Vaniman
8
1985); oxidation of the glasses' ferrous ron may be another consequence of
prolonged heating, removing one of the possible barriers that could retard the
transport of oxidized actinide elements.
Silica Polymorphs
The silica polymorphs, quartz, tridymite, and cristobalite are abundant
throughout Yucca Mountain. Solubility and thenmodynamic properties vary
slightly between the silica polymorphs, and experimental studies indicate that
silica concentrations in solution are controlled by cristobalite rather than
quartz when both are present (Knauss et al. 1984). Tridymite will be common
only in those parts of the repository workings that may extend into the middle
and upper parts of the Tptw unit (Fig. 8-3). Thermomechanical responses of
the silica polymorphs are not anticipated to lead to any significant problems;
transitions in cristobalite molar volume occur at temperatures above those
anticipated near the repository.
Cristobalite is ubiquitous above the water table except in Drill Hole
UE-25a#1, where cristobalite does not occur below the Tptw unit. Elsewhere
cristobalite persists to depths greater than 00 m above sea level. There is
a correlation between the loss of tridymite and the first appearance of
abundant groundmass quartz with increasing depth. This transition takes place
within the Tptw unit (Figs. B-3, -4) and represents a major transition in the
mineralogy of the proposed repository host rock (Bish et al. 1984a). This
transition in part reflects the passage from zones of common high-temperature
vapor-phase crystallization (tridymite) to zones of lower-temperature devitri-
fication (quartz) within the Tptw unit.
Smectite -
Previous studies have noted that smectite is a ubiquitous alteration
product at Yucca ountain, but one that is generally found in relatively small
quantities (Bish et al. 1982). Although this statement is generally true, the
data summarized here indicate that two zones of abundant smectite can be
mapped within Yucca Mountain. These zones occur at the top of the vitric
nonwelded base of the Tiva Canyon Member (lower Tpcw) that contains 7 to 35%
smectite and at the top of the basal vitrophyre of the Topopah Spring Member
that contains to 45X smectite (Fig. B-5). The smectite intervals that can
be traced through the cross sections are generally less than I m thick but are
notably thicker in Drill Holes USW G-1, G-2, and UE-25a1l. The continuity of
these two intervals is important, particularly the interval at the top of the
9
basal vitrophyre within the Tptw unit immediately below the proposed
repository horizon. The sorptive potential of this thin interval is high, and
it may provide an important supplement to the more abundant zeolitized zones
at greater depths. The thermal stability of this smectite zone and the
probable time-temperature-hydration history of the layer under repository
conditions are being studied as an important part of retardation modeling ofYucca Mountain.
In addition to these laterally continuous smectite-bearing intervals,
there is also a tendency for smectites to be concentrated near some major
structures. Smectite concentrations occur near Yucca Wash (USW G-2) and along
Drill Hole Wash (USW G-1, UE-25a#1 and bi1). Scott et al. (1984) propose thatmajor strike-slip faults may occur within Drill Hole Wash, and similar
structures may occur along Yucca Wash. Smectite abundances are exceptionally
high within the drill holes near these proposed structures, and the amount ofinterstritified, relatively nonsorptive illite ncreases with depth in these
locations (Caporuscio et al. 1982). It is still uncertain how these major
structures may interact with the transport pathways away from the repository.
Jones (1982) attempted to use clay-mineralogic criteria as evidence of
past variations of water-table elevation in alluvium in northern FrenchmanFlat, TS. He proposed that variations in the smectite 001 spacing would
reflect changes in the water-table elevation. Jones (1982) found slightly
more expanded basal spacings for smectites up to 50 m above the present water
table and suggested that this may be showing the effects of increased
hydration, but these small changes are of doubtful statistical significance.
It is well documented that smectite basal spacings are a function of the
interlayer cation and the partial pressure of water in contact with the
smectite (Gillery 1959; Suquet et al. 1975). Therefore, it is doubtful that
these variations can be attributed uniquely to variation in paleowater-table
level. The smectites in Yucca Mountain typically show no systematic trends inthe 001 spacing with depth near the water table (Carroll et al. 1981;Caporuscio et al. 1982; Vaniman et al. 1984) and have basal spacings charac-
teristic of mixed sodium-calcium nterlayers. The only apparent change in
phase assemblage near the water table in Yucca Mountain is the alteration of
vitric tuff of Calico Hills and lower Topopah Spring Member.
10
Clinoptilolite and Mordenite
Previous studies have emphasized the occurrence of at least four mappable
zones of clinoptilolite (or heulandite) plus mordenite zeolitization beneathYucca Mountain (Bish et al. 1984a; Vaniman et al. 1984). There is sufficientpetrologic evidence to show that these intervals occur principally whereglassy material remained outside the zones of devitrification in the centers
of ash flows. Therefore, there is a general correlation of zeolitizedmaterial with the nonwelded tops, bottoms, and distal edges of ash flows.This stratigraphic control is evident in Fig. -6, but exceptions to thisrelationship occur (e.g., the occurrence of zeolitized tuff in the devitrifiedTram Member, Tctw, of USW G-3). Indeed, the first zeolitized interval belowthe proposed repository horizon occurs within the densely welded Topopah
Spring Member, at the boundary between the devitrified zone and the vitrophyrelihtologies (compare Figs. -2 and B-6). The origins of this particularinterval may be very different from the deeper zeolite intervals (Levy 984b);at this boundary, water was liberated at elevated temperatures during -earlydevitrification to form heulandite in the adjacent vitrophyre. Zeolites alsoform in fractures crossing the devitrified intervals (Carlos 1985). Thesevarious occurrences point out the complexities of zeolite formation at YuccaMountain and suggest multiple origins involving both closed and open systems,high and low temperatures (e.g., Moncure et al. 1981). These varieties ofzeolitization will be described in future research.
The thicker zeolitized bands in Fig. B-6 tend to follow those intervalsthat retained glass following early tuff devitrification. This relationshipallows correlation of these zeolitized intervals between drill holes where thesame welded and nonwelded zones can be found. Problems with such correlationsoccur where some zones of greater welding pinch out (e.g., the welded Prow
Pass Member or Tcpw between UtISW G-1 and -5), where zones of zeolitization
pinch out between drill holes, or where zones of welding have no simpleanticorrelation with zeolitized intervals (compare the zeolitized and welded
zones in USW G-4 and UE-25bil, Fig. B-6). These are areas were alternatecorrelations between drill holes might be drawn. Future studies will addressthe problems of correlation.
Phillipsite and ErioniteAlthough phillipsite and erionite were previously reported to occur in
several samples from both UE25a#1 and J-13 (Heiken and Bevier 1979; Sykes et
11
al. 1979), we have found no evidence for the presence of these two zeolites in
these samples. Helken and Bevier (1979) reported erionite in samples JA-i5,
JA-32, and JA-33Bt and phillipsite in JA-13 all from Drill Hole J-13. These
analyses were based primarily on electron microprobe data, although the dis-
cussion of JA-32 ncluded an XRD identification they list as erionite(p).N
Sykes et al. (1979) reported the occurrence of erionite in YM-34 from rill
Hole UE-25a#1 based on scanning electron microscope (SEM) examination.
We have reexamined all the above samples by x-ray diffraction and found
no evidence for the occurrence of erionite or phillipsite (Table II). These
analyses agree with those published in Carroll et al. (1981). Minimum
detection limits for phases such as erionite, phillipsite, ordenite, and
clinoptilolite are on the order of 1. In addition, the x-ray patterns of
these zeolites are distinctive and their identification by XRD is usually
unambiguous.
There are several explanations for the previous erionite and phillipsite
Identifications. All of the JA erionite and phillipsite analyses relied upon
electron microprobe data. It is difficult to obtain reliable chemical data
for hydrous, finely intergrown materials, and distinctions between zeolites
based upon analyses of such materials are suspect. Furthermore, it is
possible for several different zeolites to yield similar chemical analyses,
particularly erionite and mordenite. The tentative identification of erionite
in YM-34 was based on the morphology observed with the SEM. However, we have
observed identical morphologies in mordenite-rich tuffs containing no erionite
(Caporuscio et al. 1982). Further studies have shown that erionite does occur
at Yucca Mountain, although not in the samples where it was previously
reported. Ertonite has been positively identified as a fracture-lining
mineral at the 1296 ft (395 m) depth in Drill Hole UE-25a1.
Analcime and Albite
Few drill holes have penetrated deep enough to intersect analcime-bearing
zones and fewer still are deep enough to contain secondary albite. Analcime
typically first occurs at a depth of about 250 m above sea level but appears
as high as 600 m above sea level in USW G-2 (Fig. -7). The shallower occur-
rence of analcime in USW G-2 agrees with other evidence of major hydrothermal
alteration up to the 600-m elevation (Bish and Semarge 1982). Authigenic
albite has been found only in USW G-1, G-2, and UE-25b#1 (Bish et al. 1981;
Caporuscio et al. 1982). Authigenic albite occurs only below 500 m above sea
12
TABLE II
X-RAY ANALYSIS OF JA AND YM SAMPLES
JA-13 JA-333inectite 1-3% 3Sectite 2-4%Mica 1-31 Mica 2-5%Quartz 10-20% Quartz 30-45%Alkali Feldspar 70-90% Alkali Feldspar 50-60%
JA-I YM-34fica 1-3% '3ectite "5%Quartz 30-40% Clinoptilolite 60-80%Alkali Feldspar 60-70% Mordenite 5-10%
Quartz 5-15%Alkali Feldspar 5-10%
JA-32§nectite 1-3%Mica 2-5%Quartz 30-40%Alkali Feldspar 55-65%
level and may generally occur at much greater depths throughout most of theexploration block. As with analcime, the shallowest occurrence of authigenic
albite is in USW G-2 (1080-m depth).
IV. SUMMARY
Quantitative treatment of x-ray diffraction data provides accurate
determination of mineral abundances within fine-grained rocks. This method is
exceptionally useful in rocks such as tuff where the most abundant primary and
secondary minerals are too fine grained for optical determination. Using this
method on samples from drill holes at Yucca Mountain, mineralogic zones have
been mapped in three dimensions. Both primary and secondary minerals at Yucca
Mountain are subject to significant vertical variation or stratigraphic
control. A thorough knowledge of where and why these variations occur will
allow more reliable predictions of the mineral types that may occur along flow
paths away from a repository in the Topopah Spring Member. Particularly
well-constrained zonation occurs in the preservation of primary glass and in
the transition from tridymite to quartz with depth. Zonation of smectite and
clinoptilolite/mordenite is relatively well constrained in some intervals but
may be difficult to correlate between some drill holes. The deeper alteration
13
products, analcime and albite, are less commonly sampled and are therefore
difficult to map.
ACKNOWLEDGMENTS
Thanks are due
diffraction analyses,
for helpful comments,
to E. Semarge and L. Haassen for help with x-ray
to D. Krier for reviewing the manuscript, to R. Scott
and to B. Hahn for typing the manuscript.
APPENDIX A
X-RAY DIFFRACTION ANALYSIS OF TUFF FROM CORE, CUTTINGS, AND SIDEWALL SAMPLES
X-RAY DIFFRACTION ANALYSIS OF TUFF
Cutt1ogs
Smle
3-12620-63C65t.66t710a-720770-78C860-870
105-915
9;.9921067.1077
103-1071123-3126
1136-1139
Oeptt1.)
192.0201.22195237.7265.2
275.-27.,299.6-3C2.4325.2-22.3333.1-334.4341.7-343.234t.3-347.2
Smec.tte
4
41III
e1
32
3fI3138 7
33:7
r-222 1
"I
41
'3
Cl 1ro- Tridy-ptilelite site Cuartz
2-1 1324 Il- * 14:2
.- 14:2
- 0-12- . 12:2
- - 24:3
- - 3A4
bl* O *5-210 2:1
54:10 * 2:1
Cri sto.balite
613
103723
4:2
4:2
3:2
6:3302
1134:2
1013
AlaelifOlWsPar
S3IC70:1078:10
El:IC16:10C3:1R
66c: 63:10
14:5
gloss hew.at t
3Z 2C -
* 1*1
* 1
1:3
*1
. 1
K:2C -
14
APPENDIX A (cont)
Car.*
* Sa.le
UE2S~e- In
245C
ZS2
2592M51
273725322F46.72Cst
Ise
2F7S
1919
2946
29S
298f3060
3092Fractwre
3092
30S9
3C9F312FFrocture
31263163Frimure
3162
31ftFra -.ue31F
319f3272i
322!2'
32V
329E3323362
33743393
34c1346S
Oeptl bS c.IU) tite Nice
Cl in. ritfe"- Anal-ptlolite Ite Cie*
Alto1s°uartl felespar
732.1746.6
769.6
791.3
608.0
834.2
663.2667.7
570.2
173.9
877.S
69.7897.9
900.1910.7
929.6942.4
942.4943.4
944.3
953.4
10-20 2.10S-15 6-10
6-16 *-16
6-16 2-10*-1S 2-102- 2-10
10-20 2.10723 211
10-26 2-610-26 2.1016-30 10-20
6S16
2-10 2-102-10 2-106-15 6S
6-16 5-15
2-10 S-10
- 2-10
<5 5-16
6.16 S-1SS-1S 5-15
2-6<2
2-S
5-15
tR.
2-6TR.
10-251s:910-252-S
5-15
20-40
- 30-St
- 30.50
- 30-60* 30-SC
- 30-S0- 20-40
15-30- 2924
- 16-30- 20-40
- 20-40
- l Q-30
- 30-S* 30-0
- 30-5
- 20-40- 40-60
30-IC
30-60,
30-50
20-St30.60
40-IC20-4c4411C
20-4040-60
20-4020.4C
30.60
30-SC
30.5040-6020-SC
toa4c4o-6C40-60
40.60
Calcite Uolinite Other
2.10
2-10 - -
2-10 . -
..
..1
2.5 .2-10 -
2-6S
2S-30 -
2-S .
2-S - -15-30 - -
- - 30-50
* * - 30-S0- - - 20-40
* * - 20-40
963.4 2-S 2-5
964.1 2-S S-1s
964.1 - 2-S
970.6 10-25 10-20
- - - 20-40 20-40 15-30 -
- - - 20-40 40-6C 2-6 -
- - 10-30 10-3C
-- - 20-40 30-SC
50.70
970.e *5 CS974.1 2-10 S-1S
182.1 2-! S-1S9t3.0 S -1S S-1
992.7 30-S0 S-1S
996.1 16-30 2-10
1005.2 S-1S 2-101013.6 6-16 S-161024.7 10-25 S-1S
1026.4 5-15 S-151034.2 S-1 6-10
1036.6 2-5 I-IC1054.3 %,16 -1
.- Yr.
.- 2.6
- 10-30- - 10-30
- 10-30
- 10-3C
5-1'
2C ZC
20-4C
20-4010-30
30-50
20-40
26-4C
20-40
20-40
20-40
2Q-40
20-40
4*C6C
S.-7C
*Q-6:
20-at
20-4C
*0-6C
40.6C
SO-SC20-4C
20-4
2C-40
152
60F-Q 2-t. C.t-3C
c2
2-62-62-10
5-162-6
2-10
15
APPENDIX A (cont)
Car (ont I
3530
Fracture
3530
3SAS
Inclusion
3W4S
3571
3572
Inclusion
3572
3602Fracture
3602
366CFracture
366L
370P376'
3792
363'
388C39Ci1
39023904
39103S26
3956
3963398EFracture
39ft
(n) tite Nice
1051.4
1066.6
1075.9
1075.9
1081.4
1081.4
101. 4
lOft.
1-15
10-25
10-20
S-IS
5-15
W-C0
ClIno. Noreen- AAi.ptilolite Ite, cloe
* * 10-30
- - 10.30
* - 1S-30
Wartz
20-40
20-40
20-40
AlkaliFeidloar Calcite 40l1nite Ot her
20-40
20-40
30-S0
2-10 2-10
2-10 2-104S '2
5-10
2-10 2-S
10-20 -
S-1S 5-15
- S-11 20-40 20-40- 2-S 20-40 30-S0
10-20
5-10
2-10
IOF.7 10-2;
1097.9 S-1
1097.9 *S
1115.6 S-IS
1111.6
1130.21148.2
IISS.E
1168.9
l182.6116.0
1289.31169.9
1191.6
1196.6
1205.6
1207.9121S.S
5-155-15
10-20
10-20
10-2030-S0
30-S020-40
5-110-20
15-30
20-40To-25
5-15
2-10
2-10
S-15
2-10
2-10
2-10
5-15
5-10
5-10
5-10
2-10
2-S
5-1S
5-15
S-15
10-25
- 15-302-S 30-S0
*2 20-40
30-S
15-30
30-5C
- - 20-40 20-40 S-1 '2- 10-30 20-40 20-40 S-1 <2
S-1 2-10
15-30 20-40- 30-S0
20-40 2-10
-1 30-S02-5
10-20
20.40
15-30
- - 15-30
- _ 1S-30- - S-15
- _ 15-30
- - 10-20- . Tr.
- 2-10 -
- - 15-30- . 2-10
-- 2-5- 10-2S
10-20
21-4526-4S
20-4020-40
20-40
20-40
1530
20-40
30-So
20-40
15-30
20-4020-40
2-10
40-601S-3030-S0
20-40
20-40
15-30
1-30
IS-30
30-So
20-4030-SC
20-dC30-S0
10-70
<2
-2
5-11
2-10
2-10
1-11
11-30
2.5
10-20
2-10
2-10
2-S
2-102-S
2-S
2-STr.
2-10
2-S
Tr.
1215.1 2-S 2-S _ 15-5 IC-2C' 70-9(
fluoriteb 70o0rokite
16
APPENDIX A (cont)
Care
Ototh Svmc- C I o- bfrden- Anal- Cristo- AlkaliSample r) tit, Nice plolft It, lac . Miarti bait, f.lspar Cl1cite Othe,
- -
Usih 6-
10
Joe
2DC230
270
304
331
33F35
395S1
147540
56162706723
743
76?
770822855
ese923951
984
1032
1Q771133
117e1234
12f11331
13P21420
14611S30
zses1634
166416911746135217sISO
t9s1952
2001
3.0 S-10
3C. s
63.0 .
70.1
12.3 2-10 -
92.7 .
100.9 30.10103.0 40-60 -
109.1 IS-30 -
120.4 -1S c2152.7 5-20 3
166.7 5-15 C5
167.0 45
171.0 10-20 *3191.1 5-15 CS
206.7 30-S0 *S220.4 5.1S *S226.5 30-S0 *S232.3 2. -
23'.? *2 5-102SG.5 5-10 *5
26C.6 <5 2-5
273.7 42 2-5
2s0.7 10-2029.9 2
299.9 2-10
314.f 2-10 4232t.7 2-10 <2
34!.3 1-11 42369.1 46 2
376.3 2-1039G.4 - -S -
405.7 1-15
421.2 S-1S *2432.0 5-1S
445.3 S5
468.2 10-20
413.1 S-1S499.0 30-50 *2
107.2 *2 -
516.4 5-15
531.9 10-20 -
534.0 -1S -
S48.0 *2
663.3
s78.8 *2 <2595.0 * *S
609.9 O *2
5-10
10-20 -
10-20 -
15-30
45 975-90
45 -
(5 -
: :
'Cs
* - ~30-10- - 30-SO
- . 30-50
- - 30-50
* - 30-50
* S-10 30-S0
Ti. 5-10*5 10-ZO
- - 20-40
* - 20-40- - ~20-40
-- 5-10
5-15 S-15
- . 5-15_ * 15-30
- 20-40* * 20-40- - 20-40- 20-4 15-30
- 15-30 20-40
- 15-30 10-20- 15-30 20-40* 20-40 S-IS
* 15-30 20-40- 10-25 20-40
. 10-2s 20-40- 15-30 15-30
15-30 20-4V
* 11-30 15-30* 15-30 20-80
- 10-20 30-10
* 10-2C 20-05- 10-25 20-40- - 15-30
-10 5-0- - 15-25* S-10 15-30
*CS 5-1S- 1-15 10-20
Tr. IS-30-10 10-20
10-20 10-2010-20 10-20
30-103D-SQ30-5030-SO
30-5030-SQ30-50
20.105.10
20-40I S-3C
10-2010-2030-SO
25.40
30-5015-30
5-10
10-20*S60.8030-6030.50
40-60
20.40
20-4015-30
20-dC
30-SC40-S00
30.50
30-SC30.50
KC-SO
40-6030-St
30-SC
30-SO
30-S0
10-201-11
10-20*-10
1i-30
10-2010-20
I-2015-30
- 1-2
6-6 1-160
- 5-lS15-30 -
- 10-20'10-20 -
- 30-50t
- 3Oh60e
3Q-S0 1S-3CbS-ts 15-30r
* 10-2C
- 10-20'- 5-15'
.- 5-10'
5-10 -
15-30 -
30-504240-60
30-1010-70
40.6040-6040-60
1-105-10
1-101-30
5-10
11-2I1-30
40-60
40-60
17
APPENDIX A cont)
- Ce fcot)
Orptb 5Mc. Cl iio- ioPdef- .Al Cristo. AlkaliSemple (a tto Olics Pt la)t# ite clue Quartz bal ite Fulipsa- Calcite Othe,
u3sb
207F 633.4 S IS 20-40 20.40 - S-10 10-20 10-20
215t 617. S CS 20-40 15-30 Ti. 1-10 15-30 10-2c - -
2241' 611.2 S *2 20.40 20-40 - *-IS 15-30 11-30
2313 717.2 *2 2-10 S-IS 20-40 I 3S-30 1.30 10-20
2430 740. CS S-1 20-40 S-1S 20-40 0-10 20-4* -
2W2e 770.S 4 1-IS *S 11.30 20-40 *S 20-40 -
2667 812.9 CS S-10 * 20-40 - 1-30 CS 30-SO2?44 f36.4 * *2 - - - 30-SO 1-10 40-6C .2620 s9.s *2 *2 - * 20-40 2-10 SO-70
2669 674.1 2 2-1 - * - 20-40 2- S0-70 -
2PF7 t8t.0 *S *2 - - - 20-40 2-S 50-702950 699.2 2-10 *3 . - - 20-40 2-10 40-60 - -
2970 901.3 5-1S *3 . - 30-50 0-10 40-60 -
3037 925.7 30-SG *2 - *S - 20-40 O.S 15-30 - -
3067 934.P - *2 S-10 20-40 - - 20-40 20-40
319? 972.9 S-10 - 20-40 S-IS Ti. 20-40 O-S 20-40 * -
3260 99:.6 15-30 *2 S-1S S-1 20-40 15-30 0-S IS-3C - -
33O 1006.3 2-S 10-20 - * - 1S-30 0-10 4C-60 -
3330 1011.0 * 2-10 - - - 2040 0-10 10-70 - -
Fracture3330
3349336f
34163464
34923512
35413 ?
3tt3t?1
3 723724
3710'37?2
3791
3P3
3575
390P
3933396E
40054090
4167
4199
42094287
4329
1015.0 1-11 2.10
1020.E 42 2-l0 -
1026.C * 2-10 -
1041.2 42 2-10 -
1052.e 20-35 *S
1064.4 10-21 CS
107V.1 10-20 1-10
175.3 S-IS S-10 -
109C.6 11-30 S-11S -
110S.1 10-20 S-IS -
111f.9 S-1 S-101133.9 "-15 S-10 -
131-.1 20-3C CS
1143.C 20-30 S-11 -
114.7 11-3C 1-10
14511.7 2S-40
116E.3 20-40 2-10
1181.1 20-30 S.1 -
1191.2 10-21 -
119e.t 10-20 -1209.' 10-21 2-10 -
122C.7 10-20 1S -
1248.6 11-30 10-25 -
1270.1 10-20 10-20 -
1279.9 10-20 S-IS
1262.9 1-11 1-101300.6 10-20 s-10131S.S S-1 2-10 -
- * 10-2C
* - 15-30 0-10- - 20-40 0-10
- * 20-4015-30 T. IS-35
15-30 S-10 20-40
2-10 10-20 20-40- 20-40 20-40
15-30 - 20-40* 51 20-40 - S-10 20-4C?
-Ti. 20-4
3C-SC
- - 20-40 -. 20.4G
- *2 30-SC- 20-4c
*S'1 3C-St* - 20-4C
- 20-40 20-4C0
- Tr. 30-St 11-30
- 2-10 IS-30- *2 1S-30
Ttr. 10-25
* 2-10 10-2* 5S 20-40
CS ro-4c
IS-30
S0-70
S0-7t
50.7C
15-3:
1s-3r
30-S015-30
15-3C
30-S0
30-St30-SC
20-40
30-S0
3G-SQ
20-40
20-40
15-30
30-.SO
20-40
30.1Q
SO-S-
tO-4030-SO
30-SO
40-60
30-S1
30-S
4 ( 5 C0
* (C
$.I 4( 6
2.10 -
-1 -
- .r.c
1-11 .
S
CsC
4 -
1-1 -
18
APPENDIX A (cont)
Co, CIcovit
Oeptl Suc- Cl o- t1dren. Aaul. Crsto.Son.-It (el tite mica itnl lt# Ite c1t.a oart2 bal te
1156 C-2
4467 131. 15-30 - 15-30
4467 1361.1 5-16 2-C . . 15.30 -
4570 192.g 6-1$ S-10 . - CS 20-40 -
478s 145S.a 10-20 CS r .t 20-40
43OS 1464.6 10.30 - . . tr. 30-504316 1467.9 15-30 - . rt. 30-SO -
43 1474.6 15-30 - - - '5 20-40 -
'173 125j.3 20-40 - . - *2 20-40 -
s~es 1486.9 20-40 - - - 2-40 -
423 1491.4 15-30 S-10 . . 42 20-40 -4924 IS00.f 10-25 S-IS - - 4 20-404949 ISQ.S 30-sr 1-15 . - - 15-30 -
S01? 1129.2 10-30 . . - - 20-40
Feldspar Calcite 0t p
30-5030-SO
30-SO30-SO
30-9020-4030-SC'
20-4020.4020-4015-3C30-10
5-15
S-IS10-25S-1
2-102-102CS
*5
S-10
sDpepul tt
S017
SC21144
S171S20t
5213
5305
1369
5379
434
5493
5105
553i
SWE
st3t
5657569t
5762
5W2E186!
594.5
5911
592(
5931
5951
5971
S9S
1525.2 2-10 -
1532.9 10-30 10-1167.9 2-10 10-
IS7.1 10-25 20-1586.0 10-20 10-
ISE.9 S-15 5-
1617.0 S-1 S-
1436.5 S-11 10-,
1639.5 2-10 10-
1651.3 2-10 IS-1674.3 *s I-'
1677.9 S-IS 10-:
166E.C 15-35 -
17?5.7 10-20 -
171t.9 10-25 -
172'.3 20-40 -
.173. 1 Ir-20 -
1756.3 S-15 -
1773.9 - -
1793.7 10-25 -
1756.F 10-25 -
ISC3.1 1-IS -
IE80.2 10-20 -
167.# 15-3C -
1613.9 1S-30 -
1820.0 10-25 -
1826.4 10-25 -
30
304C
25
-1
-5
20
20
30
30
*2
- - 20-40
- - ~20-40_ _ 15-3Q
-Tr. 15-30- 20.40
- - I5-30- - 20-40
- - 20-40- *2 11-30- - 20-40
_ 15-30
- _ IS-30
- - 15-30_ Tr. 10-25
* - 1-30- 2 15-30
- 1S-3C- _ 15-30_ _ 15-30- - 2*0-40- - 30-S0
- tr. 30-S0
- - 15-30- (2 tO-40- s 20-40
- 41 30-50
30-S020-40
30.1015-30
20-10
20-40
30-5s30-10
30-50
30-SO30-SO
2GJQV
30-SO
3 0-S0
0-1030-SC
3C0-St
30-50
30-SC,
30-1030-SO30-S0
30-50
30-S030-S0
2-10
2-lC2-IC
2-10
S-155-155-IS
10-205-10
10-2!2-10
10-2'2-1C
10-25
15-3c2-10
20-40
15-3C
2-102-1C
2-10
2-1(.C
5 -1Qc
*2
5-1 9C
S-Ise
2-1Cc2-1cv
'Sl
S'C
10-2!c2-Itr
2-1ce
2-10C 2s
5,15C
4Sc.
f-
* If~d>1C,b6 class
C &Sol niteC Chloritt
hematit
19
APPENDIX A (cont)
Cart Coit)
Depth smec- l n. Anl. Crist- Tridy. AlgaliSample e1 t1t1 Pice P11elits ciue Oatf ball ite ste Feldspar Calcite Class tOter
_ - _ - - - _ - - - - _
USb Gt.3
31.0 9.S 2-4 1-3 . - - s-1S * 70-0 It-i -
41.0 13.7 . . . . . 1-20 4.6 70-60 .79.0 24.1 - - 1-3 4-E 20-30 *5-75 . -
103.1 31.4 . . 1-3 11-25 1-10 6s7s 1.3 -Fracture 1 -'-3 1.3 6-12 s-9
191.3 19.5 - - . - 20-30 . 70-so . -___ _ 2.4 . . . - 2-S .s S--91 -0
245.7 74.3 1.3 1 - * -3 20-30 2-4 *5-75303.e 9.s I - - . - 20-30 * 70.t0 - - -
316.6 96.6 - - - . - 20-21 - 70460 . -
34:.1 104.2 2-1 - - - * 25-31 - i5-is3MA 206.7 1-10 - - - - 10-20 3 3-45 . 30-.0 -
376.1 124.6 3-6 - - . 2- 2-. 45-55 . 30-SC -
410.0 125.0 16-24 #I 1 - 1-3 20-30 - 45.15 - -
414.3 126.3 2-5 -P I * 2-5 1S-21 - 7040 - - -
417. 127.3 10-1S -I * - 4.6 11-20 * 60-70 -
424.4 129.4 - - . 1-3 15-20 4.6 70-O --
42S.0 13C. - 1.3 - . 2-6 11.25 2.6 61.75 . - -Von 1 . . . .- 3 - 4-. 9-95 - -
43C.S 131.2 - 2-4 - - 10-15 2-6 75-eI - -
4*1.S 14. * . . . . 6-12 -1S 7s-es -
42.0 146.9 - S1 - - 1-10 15-25 65-75 2 -
62C.3 1S1.6 . - - . 2-8 11-25 61-71 2.4 -Ctt * . - . . * 10-20 10-Is 7S-3-525.3 160.1 * . - 4. S-21 61-7 - *17s.o 176.1 .1 - - . - 20-25 10-11 60.70 * -
633.4 193.1 -l - - . 1-3 20-2S S-10 65.75 - '674.7 205.7 -I - - 1-3 20-21 2-8 6-75 - -
Fro.ture . . 10-l - 60-S0 11-20 -
702 . 214.1 - A - - 4.6 11-2D . 65.75 - - -
79.S 234.1 -1 I - - l 20-25 2-0 60-70 - -
s.4 25F.9 I If - - Z-F 15-2C - 70-C0 - - -Fracture 7 # - 7SO ' 2-S 10-2c - * -
91C.S 277.5 - - * - 2-1 21-30 - 60-7 --Fracure A _ _ _ l-2G 1-3 30-10 31-4
924.3 261.7 I . - - 1C.I2 10-is 1-I1 60-70 - -fretur. - . . - 7s.1s 1 10-11 S-1c - -
9;.1 2e9.9 1 . . . 6-10 1-20 2- 65-71 -
954.f 291.0 ,1 i - 15-20 10-11 - 6-75 * -
102 .0 313.0 - - - - 2-10 11-20 - 70-8c.fronure, 1-3 . . . 5.9 '1 - 44 3S-5 - 3s-^t1041.0 323.4 - . . . 16-22 1-10 - 6-7S .1130.3 344.5 - *1 - . 11-20 6-32 - 65-75 -
1171.0 316.1 -I 1 - 30-40 2-4 S15-E - '
lS.7 364.1 4-6 . . 2-4 21-30 - 30-40 20-4c -vei_ - *1 - 6-10 20-25 - 65-71 . * -
122.0 374.0 1.3 . . . 6-10 15-20 - 30-4G - 30-S01302.4 397.0 1-3 2-6 lob .2 35.45 30-G -
1322.0 403.0 2 . . . 2so -o - 25.35 - 10-O -1344.6 409.9 . . . . 5-10 1.10 - 2S-3 - 40-7C136$.6 417.s . . . . 2-6 210 - 20-30 S-Ft -
1399.1 425.0 - . . - 2-6 2-10 - 2S-35 - so-o -13s4.6 425.1 - . . . 2-6 210 - 25-.5 - 5-St
20
APPENDIX A (cont)Core (cont)
Depth Smec. Clao. £nfl. Cristo. Iri@o. Alta1ISemilt (.? tite "ka FtIite clo, Quatz 6lW1 te Feldspar Calc'te Glss Ott
US w Ct-31411.5 431.4 - - . - 2-U 2-10 - 30-40 . 40.70
1439.2 43E.7 - * * * -25 2-10 * 15-2S 40-70
1439.5 43E.t -1 1-3 * * 2-3 2-10 30-40 - 4.7C346.5 447.6 . 1-3 '. 2-C 2-10 * 3040 ' 40-701493.7 455.3 1 * 1-3 - 2C 2-10 - 20-30 - 56-so
1496.3 415.7 . 24 - 4-10 2-10 - 20-30 . 50.s-t1510.7 *6C.S 2-4 '1 * - 2-S 2-10 - 20-30 . So-Bo1537.S 468.6 2-4 2-4 1.3 . 15-20 26 . *5.55 2-4 10.30 1 . 3b1571.6 *7S.0 1.3 1-3 . . 2.6 2-F . 40.0 . 30-6c159I.1 487.2 3-6 e1 . . 2-8 1- . s0-S 30-6t16Q'.0 488.6 * P1 - - 1-3 21-35 - 60.70
1624.2 495.1 - - - - 15.21 1-3 S.10 65.751653.2 S04.0 -1 '1 . - 10-20 1. 10-20 61.75 -
170S.0 121.0 1 - - 10-1I 1.1 61.75 1.31744.0 531.6 . - . . 4-e 20-30 - 65-751827.2 517.0 * - 1-25 - 2-6 2-6 . 65-751874.v 671.2 - * £5.%5 - 1-10 2-8 * 3-4-1931.8 S90.0 2-5 - SS-65 - 2-6 2-6 - 25-35 -
19L,6.0 605.3 . . 65-76 . 2-6 4-8 - 1-25 -
1993.1 607.S . . SS-tS - 2-6 E-12 - 20-302G13.2 613.6 1-3 1-3 45-SS - 2-4 2-6 - 35-4.Fracture 21.31 2-4 10-20 - S-IS . - 35.4-
207C.2 t31.0 1-3 - - - 15-21 2-4 1-10 61-75 -
213f.2 651.7 1-3 1-3 * - 15-20 0-IS - 65-75 - - Trb2177.3 683.8 1.3 1-3 . * 16-24 6-14 - 60-70 * r
fle9.3 667.3 1-3 1-3 - - 10-1 12-15 - 65-75 -
219t.C 67C.Q 1-3 1-3 - . 10-IS 11-20 - 61-75222t.0 676.1 9E-100 - - - * * - . . -
236Z.C 71S.2 . 1-3 - . 17-23 1011 - 6-71 . - 12ac-uer 1.3 1-3 - 35-4C . . 3.41 . - C-2
236S.4 722.2 1-3 1-3 - * 15-20 10-15 * 65-'S - -
2467.4 752.1 - 1-3 . - 18-22 6-12 - 65.75 . -
254*.a 776.6 25-35 1-3 10-1 - 6-IC - . 45.152577.4 7e8.* 24 4-t 45-55 1 1-3 2- 3.40 - - 1-2t2615.3 79'.1 1-3 2-6 35-45 * 3-7 $410 - 40-S.2623.4 799.6 2-4 1-3 2S-35 - 3.7 1-4 * SS-IS - -
2618.f "5 .7 2- 3-7 21.35 * 3-7 6-lt a *5-S5 s2895.7 621.7 ' 2.4 25-31 . S- .11 . 3S.41 .-Fr:tute . 1 5-15 . 75.CS S.1s . . . .2727.4 *31.3 1-2 2.4 1 - 1-20 10-20 . 60-702914.1 t8E.3 - 2-4 . - 16-24 S-10 - 60-70
2971.0 901.6 1-2 2-S . . 12-11 10-15 . 5-S-3004.5 911.8 - 2-S - . 2S-35 2-6 . 60-70 -Fracture 34 - - 11.20 1-3 - 70-CO - -
304.3 921.2 1-2 2-4 * - 8-24 S-IC . 60.70 - -
3113.1 948.9 1-2 36 . - 10-t 1S-20 60.70 - -
3164.1 964.4 1.3 3-6 1-1S 6-12 10-20 . 1S-6* - -
3207.4 977.6 1-3 2-4 S-15 6-12 11-20 . 55-65Fracture 3-5 5-7 10-20 . 14-13 10-20 . 40.50
3226.0 983.3 4-6 24 2-10 . 10-iS 10-20 S 15.65 .323S.0 9E7.3 . . 1-3 . . 14-18 10-20 - 60-70
21
APPENDIX A (cont)
Cart (cant)
US% G.3frectuot
3311.03475.3
3589.43672.0
376.1
3Mi4.e
3e69.33936.3400b.3
4117.0
424t.64263.t42S7.1Fractur*4410.0
4423.0
1503.7Feacture4066.446C0C.?
470f.6475t..
478t.44603.2
4etS.4
495t.S
5034.C
Deth Sme'.(WI tite
Cl Ino- Aba1.Pica. ptilolite clor
Cristo- Trtid. ltalQuartz bolit, site Folspo Calcite Glass 0 her
1009.2
0SS.3
1094.1
1119.21145.6
1174.9
117e.3119S.81221.71254.91292.5
1299.61309.8
134 .0
1318.13372.7
1392.S1402.2
3435.21449.1
345.9
3464.0
1404.2149!.5
352E.3
2J2.4
S-104-e
6-12S-10
2-J1-22-4
2-10-15
2-6
2-62-6
4-1?15-266.30
IS-204-0
6-124-e
1-10
1-224
1-32-f
1-32-4
3-6
2-12.62.4
1-3
1-36-1
1-8
4.1
2-4
1-3
3-21-2
1-33-31-22.4
1-3
1-3
1-3
1-31-3
1-21-3
3-3
10-20
1S-25
It
3t
2(
0-40
0-2C0-20O-4t.
'-3C5 151
_ I- I
21
* 30-35
- 12-36
- 12-1.
- 30-15
_ 34-.1- 26-3t0
- 20-30
- 25.3C
2-9 28-32D-20 30-35
6-12 32-3e* 25-30
D-30 30-3S
-11
5-S5.15
4-10
4-12
0-400-60
4 630-40
40 .6040.50
2 3 6
35 .454 540-10
45-SI4 5
30-40
2- 1Ce
- 5-10
- 5-10
10-15 S-102-t 2-62-11-3 10-1
1-3 -
- 15-20
- 10-is
- 15-20
- 15-20IS-4c
- 30-4C
- 10-20
35.4035-40
30-3535-4060-6S25-30
48-5432-3631-40
30-35
32-3832-3f
32-3635-d0
- - 1~~-10* - ~~6-12- - ~~30-40- - ~30-40- - ~21-35- - ~30-40- - ~36-45- - ~~30-40- - ~~3S-45- - ~~35-15- - ~35.45* - ~~20-30
- - 26-3C
* - ~~35-4!
1.6
5-10
1-2
35-45
31-4!
1-3
1-2
1-3
_ .
e hornbleect
C qefte1te
e "ryeewite
* ryptotel rme
22
APPENDIX A (cont)
Care cont)
Dept" S*c. tClIto. "rden. Cristo- Alkali Trso.Simple (in) t te Pics pt.I ite It. Oweart btito Felespor site class Ct
47 14.3 t I - 2 I 28S 70 10 .
72 21.9 -I - .21 2ii 70:10 - -
107 32.6 - - - 2%1 32*1 67210 -
123 37.1 30110 - - 2121 49*10
14 4b.1 35-11S . - . 1510 *0!2c
170 1.1 28:1C S22 . . 8:2 5:2 40:20 * 20s10
22u 67.1 10*1 3*2 - 4: 2 122 6*2C * 2010 -
231 70.4 6:4 101- . -32 6020 - 20:1C
236 71.9 ot. s 101 l01 tO - *0l 2f
26t 41.7 . .1 . . . 6:2 73:1O 20:1C .
26G 41.3 * *1 . *- 12 eC2o 1C-! .
332 101.2 - 2*1 . . . 11St 76:20 76 .
383 116.7 32 Z * - - - 111 70±10 1S-11 .
410 125.0 3W2 1i . * I 12:5 64110 1721C -
416 126.8 3:2 PI - - 1 14:1 73110 0*1 *
447 136.2 2:1 el . 3:1 205 48:1C 61S .
Sl 116.7 21 - - 2:1 22:5 69:10 624
556 169.5 2:1 - * 6:2 9sS W1810 ISS11
62 "'-5 2:1 -*1724 622 63te1Q Ills
676 206.0 31 * * * 41 23:5 66:10 4:2
69' 211.5 3-2 * - - 4:1 13:2 62:10 It6 - -
746 227.' A 3:1 28:S 68:10
tl7 249.0 2*: - - - 251 3 7:3 65110
934 264.7 e1 - . . 16:2 11:4 63±1C 401
1021 312.7 1 - 9.2 201S 661C St2 -
10NS 331.9 *I - 12:2 10t 61:10 16i .t
108S. 331.9 661 1 32IQ *Fta:tuee111 34C.. I 5 * 62 14*4 69:1 I C
1163 354.1 * - - 16*2 1:4 69:1t - - -
1163 34.1 : - 35 5 3±2 6121.tnclusi3 1
119c 362.7 I - . 25 3 13 * 1W it -
124 37S.2 *i *1 .173 Isid 6*:1 .
12E2 39.6 *; *1 * 16:3 l9*4 *1C 1
12E3- 391.11293E 394.1 t e - 6-2 23 4 9 691 * - -
1299 395.95 21 2 2 23±4 62:1C
1301 396.1 el I 12 9-2 20*4 61:10 *
1310 399.3 I3 *1 3!2 12 29'S 65210 *
3314 400.1 4*:IC . 28*6 - 2-1 14*4 112.
133C 401.4 . . . 10- - 20:10 - 70:2C
1341 406.7 . . . lO:S . 30:10 - 6k2t
1372 418.2 6:-2 21 121 * *22 I25 36:10 * 4020
361 420.9 7:3 * 16:1c S t 2 42 2*10 I
13el. 420.9 42 10S . 10*S * - - . 71:20Ifcluslet1392 424.3 2 1 75:11 - 2-1 4:2 21:10 * -
1392. 424.3 . 221 - S: * . 9:2C
23
APPENDIX A (cont)
Care (co"t)
)epth StC- pic tito- H te b Cristo- Alklig mIte-5empl1 (") tt Pic t ila! te It* otttt balite Folospar ste Cl ss t tite
USh 6.4Inic Ws 1o.
1411. 432.5
143? 43t.5
143t 43e.3
d7(. 44F.1
)S 47t.F
160? 482.3
1*t5 113.6
17C7 120.3
173* s2b.5
17e3 137.4
1775 542.2
178 14.O
176. 145.0F1?ctu 0.
1 794 S46.t
1641 661. 1
1e7; s7C.3
193t 59C.7
1952 59t.0
19E 599.
1989. 606.2
2039 621.5
20es O3C.6
209s 637.0
21C 64C.1
2100. 64C.1Fva:turt
220? 671.2
222t 67t.!
* 2:1l
3±2 4:?
3:2 el
322
A .A A
P1 -.
2'1
3:1
- 'I
21 'I
rl
3:2 -
- '1
2:1
30: IC75s11
7621577210
1W. IC
40:10101025±10
3021C
451 IC
28±10
15:
"!It
3C:I t35 IC
10:'
30-: 1;
St.
* 712 6±3 S3:I0- Is 7:4
* 412 412 13±S* 6*2 1424
20±11 - *22 121412S5 1:2 6!4 30:10
1:10 4!2 723 19:101225 3:2 14±4 3810
1tt 5 12s2 11±4 29:10* - 321 13:5
- - 10-4 440ICA12 512 61210
9 o10 712
202:10
15:10
20-±1
35:10
3C I C
35:1t
20: ICIC-:'
IS:1C
2:1C
321 29:5 672102725 312 67:IC
235 1:2 69:1C1:2 29:4 65:IC5:2 18:4 7f:IC
*:2 10' 45t:IC
713 IS:4 33It
1:2 6±3 42:
321 4:2 35:10
522 1014 40:10
2:1 - 3S:15204 Q 4:l
* el 30:!1
- 4A 10
I . 35:ICw]
2231 6e.. I '1 -
22et 6M.6 . 132215 696.1 el 1±323*3 714.1 el 3±22343. 714.1 9:s 322rractuPe I2343. 714.1 6:3 2s1Fr,tue* 2
235S 717.2 - W:1
23el 725.7 P1 2:1
2423 73F.S el 2 1251* 766.9 t 3212533 772.1 -l 221
2551 777.5 * 2W1260* 762.1 - 2s1
2592 791.9 l 2:12*el el7.2 221S :1
10:1.
221 46±:142 713 3?:1C
6:2 2:1 38:1C
6:2 - lMI:019 -l 75:It325 2±1 60:1C
3121 - It: X
41:1 * 39S!C
- 32±S
* 315S
3cr5
* 261S
291* 31S
* 25S.31:5
25sS9:4
S4%IC
Ge: Io
6711C
7021;
68: I
66:1t
73:10
6*L0C
71s10
67:1C
24
a
APPENDIX A (cont)
Core (coan3
Depth c nlo- eon- Cristo- Al kt1 Tridy-Sawmle (i) tte Pice ptiloltte Itt Djartz balito feldspar site lass Otei
us. ;.'2716 U2.@ .O±10 tist - .M -
2731 £32.' . . 13-5 6020 75 . . . .
27se 839.4 1225 221 23:10 - 29:5 - 331C - -
21t 640.0 - 5:2 3:2 19s± 24:5 - 310 - - -
27t2 841.9 #1 6±2 3:2 IS: 232 - 52:10 -
2792 611.0 92 4:2 70-15 ItS
2623 160.9 2±1 6±2 16±10 S1 26± M . 9:1 -
28 3.
2Wt2Vb5
294?29'.
3000.
86C.S 7:s 2a1
66.6 6±287.3 - 42
398.2 - 3:2
898.2 -
914.4 . 42?
1±3 60:20 27:5
- * 39±1 S 12O0* - 315t . 61:10
- @ 31:1 e 66:10
P ots- 12 a - 60:20'
42: . 14!10
a Cryptomeldae
Sidewal "e Cuttings*
Deth Smoc- "eelandite. tcrdef- Tria). Cristoa. Altual horn.Sample (m1 tMe Pica Clifloptilellte Itt alto Oart litc Feldspr glass bltnoe
US--TTf:T.; 472.4 trace 0-1 O-S S-10 1-1S 1-10 60-tC .1ett'Swh S0.S trace 0-1 O-S - S-10 5-10 S-10 6S-CS . -
I W:S&) SIE.2 trace 0-1 0-S - - 5-15 10-20 -.70 -10-20 -l1o8x*S! 54F.6 0-5 0.1 So-70 - - S-10 * 20-IC *I9:S 179.1 S-10 0-1 70-O - o-s 0-S 0-s 10-20 -24? I Sh 73I.S * 0-I 70-30 - - - 0-S 10-2t - 0-1244:. S 743.7 - 01 X-40 204sC * O- s O-S 4C - -24.9 S: 759.C C-5 0-2 40.1S 20-30 . 0-S . IC.3: -
US-"'=775 395.S 0-6 0-1 0-10 - - 1.IS S-10 20-1c St-7C42:'S. 432.E 0-S 0-1 60-0 - - 0- 0- 2tY - -
14ttlS' 4.3.5 : 0-1 40-90 20-30 . O-S 0-S 10-3t -I5SL:S. 472.4 O-S . cs-8 - - 0-2 a-S IO-2t -16EWSaK; 104. - . - - - 0-S 20-C 5O-9 - -
i 1I.? - - - - 10-25 . G-S 7C.9c . -IS,. 57.9 - . - 0-5 . 2; 3C 7C9: - -42;:DC: 12E.0 10-20 - - - - 0.2 IC-IS 3C-4e 4-SC C-i4 'ODC' 137.2 - - - - - 0-2 * C. 95-9F70t Di 1 213.4 trace -I - - 15-2S - It-2C 55.7' -
Ift'*C") 32C.0 trace C-I - - 0 0.5 30-0 41-4 - -MCrO!C' 49.7 . . _ - - 0-2 a-S S1-1 It -9 -
166sbI sc'.e 40-U . 1-1 - - 0-2 10-IS 2C-3; - -1750i. 33.4 - - trace? - 0-S 0-10 O-IC £C-9U1762!U' 537.1 . - - - - 0-2 0-2 0.10 9Q-10t I1800S.' 5 .0 - 0-1 - - - 0-5 0-9 5-1' 10-90 -
I1M52: 164.9 - 0-i _ _ _ 0-9 _ 5-IC 10.100 -
I1 75Sb; S7I.S - - trace? - - 0-5 ttac? C-IC 90-9 -19!7'S: S11.3 - a-i 20-30 - - 25131 10-20 2S-41 - -1930(D~l 1U.3 0-5 0-2 *0-60 - - 10-20 - 25.31 - -IWI S S 19.2 a-10 . _ - - 0-5 . 10-PC 6S-et -22?'0DC) 67C.6 trace - 10-70 - - -' 0-5 30-40 '
*Sawm I numbers represent deptp of Saum1e In est. * seull core sample. C * rill (tlt cutting %a;1e.0e:%t is rly appromimate for K samples.
VI data fror Levy (1984a).
25
APPENDIX A (cont)
Cuttins
Depto Smec- triaj. Cristo .£11a11S-tmrlc () Site Rics site OWerts talite Feldspa- class "eatite
US1, 14-
470-4C 143.3-146.3 - 2l 6 . ft3 77:10 - ltls20-s3t 118.S-161.5 * * Tr. - 2465 76:10 - -
40C-SbC 164.6.167.6 . r. 214 A 13 73110 * l
610-62C 181.9-169.0 . . Tr. * 29:5 7121( - 1274(-76C 225.6-22b.6 l PI 4 2 261 s 6:&
O0.I 243.6-246.9 21 l Tr. 221 27±1 69:1 -IC
e7t.e80 26S.2-26t.? . r. - 29±4 2 Gb:1 -
930.94r 263.s-286.5 I ii - 14±3 16:4 6910 IC
92(-1COC 301.8304.8 el - 4-2 Tr. 23 S 7210
1003-1040 313.9-317.0 A l 1e. 31 24: 7210 1±
IIO-IIIC 335.3.338.3 PI Tr. 2-1 231 74 10 -
316c-1170 353.6.316.6 .1 . - 2:1 29:1 672±10
1270-12K- 37.1.39Ci.1 2:I - 2±1 7:4 19_1C 7Ci20 -
132C-133C 402.3-401.4 . 2±1 S 3 23.1G 70.20 -
Cuttings
Dept' Urtc. Clio 1raen- 7ri y- Cristo- Alkali sn i he-Sample t( w Sic, ilolite it. pite tuartz talite Folospar ble Glass tte
USh h-I7-Tu-o 94.1.9* * ' - 114 10-4 71± - 1±1390-400 lle.9-121.9 222 1 - 14i4 221 13!4 65:IC - -440.S4S 134.1-137.2 222 - - - 19s 221 I3: 64:1C - - 1:49C-S00 149.4-1S2.4 2:2 - - 1124 e1 lets 67:I - 1:!64,.ScC 19.1-19e.1 222 - - 4:2 2t 6b0 iM34-L'4r 253.0-Ml.0 3:2 A - 12± 4 14!4 6EIt - -
91t.-92t 2'7.4-2F:.4 A - - - - 1122 20-. 67:IC -940-95C 28t.5- A. 1 . . .. 7±2 21±1 71±1C -
104C.-lo 3!.Q-32:. el . . *- 232t 70:: .ISC1-IIec 3SC.1-S . *. 22 A1 - - IS2 I:! 64:1C -190-120C 3 .f7-3t7.F . - St - 112 l tSt* 2:
123C.1240 37i.9-37 .C 20:10 2:1 - - 4s2 2C±5 2t:10 - 3C:2(.22:-13;; £:;.3-sci.' . - * 31:4 9±4 1S±0 -
1SC-136C0 41.1-4.1 . - 78-10 3:2 9:4 IC:! - -lih-14C2 C ?f.F-43.F . . 1220 -- 7:2 9:4 31%±t-11f4-SSt 4LS.4-42.a 3±2 29±.1 16:5 , 11:3 10: 31:1 -- -16.-161C 4V.7-49:.7 * 9:3 31± C 17±4 e ±c 35::.164:-161C 495.9-512.9 - - 101 - - 6±2 ;&:b 6C:1 -Il7172C 62I.2-24.3 A A - . . 33±1 3:2 EWE±1 . .179C-1OQ %46.6-14*.6 hi - - 152C 17:5 64:%.s0-191 s79.1-SE21.2 . l 22:7 - - 2 16:10 1: 2 2L- 198-1s90 603.5-604.6 3:2 HIS 23te - 2:1 6±3 11:10 2:1.
26
;
APPENDIX A (cont)
Cuttigs
Depth bec. CMoo. Tric. CiSto- Al kal$zaplt (.) tMte Nice Pti ilo)ite ite cl'tt -al Ste Feldspar eatite
_~ -_ - - - -
USk -720-730 219.S-222.S 3±2 Tr.800.910 243.8-246.9 2830.640 253.0-256.0
S2t-930 280.4-2E3.5 2±2 #1
170-980 295.7-298.7 2:2
1150-1160 350.5-353.6 2±2 Tr.
1230-1240 374.9-379.0 222 Tr.
1290-1300 393.2-396.2 2 1
1380-1390 420.1-'23.7 2±2 eI
1450-160 "2.0-445.0 Tr. el1490-lSOO 454.2-457.2 2±2 -I
1590-1600 464.6-487.7 35:10
1710-1720 521.2-524.3 3±2
23 10Tr. 2±1
lrt. --
lr. 3:1
yr. 2:1
26±5* 72
IC 25102
* 20:5
L. 3- S 3
9:s 6510
24:5 72±1
274! 7t:IC
24: 71:10
26±5 71:30
lotS 62-.10
23±5 1K18±s 71l
20-S 645SCe:5 71±10
21:5 6fIC
17±5 40:30
5:3 2M.1C
11III
3121
121
1:1
1:11:1
1:1
7Q:20
10:5
Core
Depth Isec- C1ino- Anatl. tCrsto. AltolSample Is t tite Nica ptIl ite cime Ouartz aIIte Felcso Class Ott%,
USk M.4
I0CM.
1126.6
1149.2
116t.3
136t.41371.2
13Pc.f1421.6
1511.7
1671.4
1679.2
1829.
2011.0
2354.6
2861.0
3003.2
318E.4
3605.2
3806.0
333.0 trace trace
34.1 trace '1
35C.3 trace trace
355.5 3±2 -1
417.1 10_5 tract£19.5 trace 2:1
420.9 Ite5d3;e - #1
46C.A 10 5 2-1
S09.4 trace trace
531.19 tra:e
557.6 * 2:1625.1 trace 4±2
717.7 - 2:1
873.3 trace 3:2
915.4 I 5±5971.8 3 2 12:5
IQSe.9 trace 1025
1100.1 32 U±S
- - 2015 9:5 7 10- - 2125 12ts 6ti0 c- - 16±1 Is5s 69±1 -
21: 13:5 62:10
- - 20:5 2I5 6.IC 6Q:25* . 10:6 11:5 60 SC 60± 2
- - 7:! 1O-S 2t-IC 6:256:3 - 7±S 105 2!IC 0:2!
36±5 - 75 * 4V91t tS* - S:3 23S 72:1 -- - 4±2 2Mt 721C -- - 212 6-1 71±3C -
- - 2tr tS 68:IC- - 37:S 13:1 67:1C
ItS * 29- - S W-I -
2t:5 - - 5:3 Sl1l103 ISi 19:5 63±10C
3±2 - 5:3 725 WIN1 15:10
9±5 12±S 22:5 221 I6±C -
3± 2
2- 1a2s1'1
Potes: ( orfibleAdo.. (-) not etected.
27
APPENDIX A (cont)
Cutting5
Dept?, Smec- ClIno. Obrdef- erid- Crtsto. Alka1Iamole 1) tte f1ca ptiloilt. Ite site Ojert: blte Felaspa Clcite glass Iea lte
USh r-IUll:;T~ 134.1-137.2 St3 8:4 - 412 12 *4 70:2CSOO-SIO 152.4-155.4 - 4±2 * * 11:5 - 2!t 72i10 2:1 1:1550-56Q 167.6-170.7 * 121 . . 19:4 * 103 71f10 - 11640-650 195.1-S9L 121 . . 1324 * 1613 6210 - 121690-700 210.3-213.4 Ir1 . - - 19±2 19-3 61:10 - - 1:17?0.79r 237.7-240.8 12 . . _ 3±2 25:3 9±2 61:10 12 - -
640-9s 256.0-259.1 1-1 1 1 - - 6:3 20±2 16±3 56:10 - '930-940 283.5-28t.5 1I _ , Sf2 26:3 7i2 57210 . . I
1000-1010 30.P-307.8 1:1 - - - 22:2 16:3 60:!0 1:1 1109-O 332.2-335.3 1:1 - - - . 24±3 15:3 58e10 - - 'I1160-1170 353.6-356.6 11 Isl . _ 10±2 18:3 U:10 1:1 - '11220.1230 371.9-374.9 - 1±1 - - - 27:3 8:2 S9:10 - - I1300-1310 396.2-399.3 11 2:1 - . 35±4 4±2 59:10 . . <11320-1330 402.3-405.4 2±l 121 1424 - * 202 1324 5Q 10 - - -
1340-1350 40.4-411.5 - 11 29 e * - 1C-.2 9-.3 51:10 - -
1380-1390 42C.6-423.7 - 11 40_10 12±4 - 8:2 7±3 31:6 - - -
1410-1420 426.8-432.8 - - 4010 8 3 - 3±2 e 3 40-2 - - -
1470.1480 46.1-451.1 - 1±1 252± 1:5 - 10-3 7si 39:e - - -
1510-152C 460.2-463.3 - 121 43±10 10e4 _ 8f3 512 33:? _ _ISS-1560 472.4-475.5 - 11 40±10 12±4 _ 1<:3 723 26±5 - - -
1570.1580 47e.5-481.6 - 121 5±3 3±2 _ 26:3 9:3 17210 _
28
APPENDIX (cont)
Cutt tegs
Depto Spec- ClIno- Karoen- Tridy. Cristo. AlkliSmple (a) tite Nice ptilolite It# ,1t, ua'tz ballte Feldspa Calcite Glass hene-te
_ ~ ~ - - -_ _-
USw h1-2
250-26E,
260-27C29'-30C
420-4Se910-520
S7&-SBC,
650-66C
720-730
7F-79K
650I-860930-94C
99D-1OCt1060-107C-
1130-114C1190-1200
1200-12101250-121C
130. -131C
136C-137Q
1420-143C
1450-14b0
1470-3482l
152to-353C
1970-1980
164.-.165C
1710.-172C
1 750t.1 760
I2-16t3t191 0-1920
200-2CI2CPC.2
20W53.77CSS.3
76.2-79.2
79.2-82.3
SE.4-91.4
12.0-131.0
11s.4-196.s
173.7-176.F
198.2-201.2
219.5-222.5
237.7-240.6
259.1.262.12e3.s.-2e.s
301.F-304.F
323.1-3it.1
344.4.347.5
362.7-365.0
365.F-368.f
3E1.0-304.0
396.2-399.3
414.5-417.6
432.8-435.9
442.0-445.0
4£8.1-451.1
463.3-466.3
478.5-4£1.6
49S.S-5C2.9521.2-524.3
533.4-536.4
554.7-567.p
682.2-et5.2
609.6-612.1
624.9
62f.C627.7
4±2 -
723 3±.2
III 41
121 -e1
221 *121 41
121 *1
121 *1
1± 1 .1
221 1
3±1 *1
1I 41
121 -
2Al 121
*1 *1
1:1 *1
*1 <I
3±2 121
- 2±3
121 *1
1t1 121
*22 -
* 121
- 121
221 3±1<1 3±1
121
1±2
2 1 114
- III 73
10±1 - 9:3
12±4 21 1123
13±4 321 2123
13±4 St2 2123
10±4 622 22:3
3024 622 19:3
623 2123 10:3
1324 1423 16:3
13-4 1122 17:3
- 14s2 21:3
- 1612 19!3
* 1322 19±3423 9±3
- 724 1M4924 1214
- 10-4 1224
114 84
- 1124 422
- 1423 8±4
- 83 C:4
- 3123 124
- 16:2 723
- 2223 723
- 2223 7:3
- 14:2 1723
_ St2 14:3
_ 5!2 623
_ 3±2 32P
- - 18:2- 19:2 10:2
- 2122 9:2
34 IC
1120
76- IC
73 10
6221C
59! IC
61:1C.
S9: It
96210
70:10
26:1t.
36±IC
36±1C
4021 i
44±10
49:1t
48: It
53:1C
671C
69:1C
66: 1C
59±1C
47:1C
SSWlt
9:2
67±h1
6t:1:
211
3:1
1:1
90± 20
3C'±20.
*1
C 1
'1
1
_ .1
* !
41:
121
.1
*1±
121
-I412*2
'1
5t324±5
19±4
21
121
19±4
42210
3±1
1024
<I
- 302C- 90±20.
- 40:2C40:22
- 40:2Cl 30:2C
ci 3 0±2 0
- 30:2t
M. 1 -
,
(1
1
41I
A I
29
APPENDIX B (cont)
i
II
I
III
Fig. B-i.Plan view of the Yucca Mountain area based on the map by Scott and Bonk(1984). Locations of drill holes described in this report are indicated,along with the orieritttions of cross-sections used in Figs. B-2 through B-8.Drill hole J-12 Is located outside of this figure but can be found in thelocation map published by Bish et al. (1984). Figures B-2 through B-8 showmineralogy overlain on the geologic cross-sections drawn by Scott and Bonk.Several drill holes (USW H-6, WT-I, WT-2, and UE-25b$l) are projected onto theScott and Bonk cross sections as shown.
31
APPENDIX B (cont)
"A I I 4pro0
MEM~~~~~~~IO
S 5CtIOWIw oECt-ON ICtIO - -
TVR Tr" '5 i- -
u#. I
In
.
g ot O 6004 ,*.~~~~~~~~O owo
gsol ~~~~Glass
*=vitrophyre
- 1vitr nonwelded
Fg.a X gse Of
ved tlass an iticdonwdtdsgain olwte h n
nsely weld Fig.cca. .presered wit i trav fo ws.r nth A in the following figures, unit es Ogf th i ya. folw h asso
Dsotr tind BOf (18) pws Ipnw ts a nd 1ptiv represent the welded edzones fia tucca Prt, tpeserve t Oener of98the Tpaitbus Tut cW cbw, and TCtw represent the welde zoe f rw brci ; a sCllot and rai tb r usf he Crater Flat uff Tfh represents lavas and flowd treffa nd Therepeofts he e at fode ifS Tu fy~~ n s used o l nonweldpdtf ~oS h
sboisnthe werred lin SndCates the St atic water level
APPENDIX B (cont)
1 . a
0(EW
US"
tam
5II
,c
eoo
U'"0.? km "I
ofND
PiEC TIN US
I wrtl
4 2.1 b "
a~~ No
lowMETERSe
GlassU = vitrophyre
= vitric nonwelded
Fig. B-2 (cont)
wA
APPENDIX B (coht)
0V"
*,6J'uIN I.mWI0
IgI"
I
SW
SECTIOW
I
Pi-d0. km mS
I4
TVRW
.A
'It
4U0It
U
U
gm iRI.
O -, -0
t--4 STEP5
TrdYm~t
Fig. -3.Distribution of tridYmite Symbols are defined in Fig. B-2.U,
,
as'
APPENDIX B (cont)
E3
'isvm.". 0wwt.2
0. k NO
SEND
SECTIONI
wOTp w IL4
wwunt4f -
2.1 Skm m
twoO
Iao+.m
4Is'A
'it
II
0-4-
. 0 Om t * IIwo@ ; I 4 @ I M ETE Mff res
Trldymite
Fig. B-3 (cont)
APPENDIX B (cont)
l
I
IJso
U'
4
Xo
* 0
.60
*, . . , .. 4 1 -me
and abundant occurrence)Quartz (zone of common
Fig..6 4
Distibltiol ofquatZ ccurencs Qart ay also occur above the level shol'f , bt nya nioaeDif r b liin o r qun rt ifl ccurym b s a re de fined in FigS 6 2
a
1ppEttDIX (t)
0
0
tIt
VaW.
0.
I
abunldant occurrence)Q Uft (oneO of common and
rig. B (COnt)
WJto0
a
.
APPENDIX B (cont)
O SL,
.--v
gm e.
I 0I 1
a- P ---.-- - - 1 w
am~=:~_
r - - -..- - -- - 1
i
AII
M.0-
Quartz (zone of common and abundant occurrence)
Fig. 0-4 (cont)
. I
APPENDIX B (cont)
PEND"4
SECTION
IU4"
0USW.4
MROACTEO2.1 k Ml
I
SECTION
SENDIN
SECTION
I
W1-45#tI
I.
15W ip
10"t
-C
0
iSoom
o gm lo*-4- 4 ., , * 4- 4 *-4__
METERS
Smectite C>5%)
Distribution of smectite,appreciable interstratifled
Fig. B-5.shown as percentage ranges of abundance.lilite. Symbols are defined in Fig. -2.
Deeper occurrences may include
-a
APPENDIX (ont)
0
. I .1
(Eti,l
lh _
Us~~W
IB
I0I t2
:10
UtS.T-?
0.7 kam Ns1
I"PO
SECTIONIUS"
,H-4
UwI -I
2. to "Im
0 000 ' I 0000 g m t ,t~
ME TER
Smectite (5%)
Fig. 3-5 (cont)
APPENDIX B (cont)II
I
.8usrf0
WOJACTED2.? h yN)
INSeCD
SECTI"IN
SECTION
tUf.25ab01 hewS)
O I bonff
towt-aU0
.40
0
0
I-U
W+
n
I0.
0 6we Iwo0*-. 4 - 0 0 4- 4-*- _
MITEMS
Major Clinoptilolite / Mordenite Intervals
H-5 below 760 m from Bentley, et al.(1983)central part of H-6 from Craig, et aI.(1983)
Fig. B-6.Major intervals containing the sorptive minerals clinoptilolite or mordenite. The interval within thelower Tptw (above the basal vitrophyre--see Fig. B-2) consists mostly of heulandite (isostructural withclinoptilolite). Mordenute may he completely absent in some parts of some of these mapped intervals (e.g.,in USW G-3 and GU-3). Symbols are defined in Fig. B-2.
APPENDIX B (ont)
E3 US" use I WT4se~P
* o
InaIt ,
WIN,
Ma lot CllnoptItoflt/Modentte Intervals
Fig. B-6 (cont)
D
B
APPENDIX (cont)
w.a
HZ w%"
KAIDIN
S6CTION
IU"
SI
CISC
E'N
SECTION
MD 259
01t hmSI
I
.1
4
i
20*
amo tlw#9---4 -f 4- * 4- .-4a..t-4
METE5
Analcime
Fi g. B-7.Distribution of analcine. Symbols are defined In Fig. 8-2.
-I
fu
APPENDIX B (cOnt)
. a
IAEH)
BEND
I
, Ft 2.1t
tIOO
-a
0
IMOO,
0-
?P
L * 1 1 A I . I i lMETERS
Anatcime
Fig. B-7 (cont)
.
C' APPENDIX B (cont)
USWH4
WROJCTED2.1 m Nl
SENDIN
SECTIONIXt
INSECTION
UE - tUS .256e1"teed
1"W,
1000.
4
I.
2
A
00+ IA
9
^ I
? _ l~~~~~~~~a-
0 Om Io1-I-4 - * 4- *-4--44
METERS4 0 0
Authigenic Albite
Fig. B-8.Distribution of authigenic albite (approximately pure albite with only minor potassium feldspar component).This distribution is determined by optical and electron microprobe studies (Dish et al. 1982; Caporuscio etal. 1982) rather than by x-ray diffraction. Symbols are defined in Fig. B-2.
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53
*S
Carroll, P. I., F. A. Caporuscio, and D. L. Bish, Further Description of thePetrology of. the Topopah Spring Member of the Paintbrush Tuff in DrillHoles UE25A-1 and USW-G1, and of the Lithic Rich Tuff in USW-G1, YuccaMountain, Nevada," Los Alamos National Laboratory report LA-9000-MS(November 1981).
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Heiken, G. H. and M. L. Bevier, Petrology of Tuff Units from the J-13 DrillSite, Jackass Flats, Nevada," Los Alamos National Laboratory reportLA-7563-MS (February 1979).
Hoover, D. L., Genesis of Zeolites, Nevada Test Site," in Nevada Test Site,Geological Society of America, Memoir 110, 275-284 (1968).
Jones, B. F., "Mineralogy of Fine Grained Alluvium from Borehole Ulig, Expl.1, Northern Frenchman Flat Area, Nevada Test Site," U.S. GeologicalSurvey Open-File report 82-765 (1982).
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54
Levy, S. S., "Petrology of Samples from Drill Holes USW H-3, H-4, and H-5,Yucca Mountain, Nevada," Los Alamos National Laboratory report LA-9706-MS(June 1984a).
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Scott, R. and J. Bonk, Geological Map of Yucca Mountain with Cross Sections,"U.S. Geological Survey Open File report 84-494 (1984).
Smyth, J. R., Zeolite Stability Constraints on Radioactive Waste Isolation inZeolite-Bearing Volcanic Rocks," Journal of Geology 90, 195-201 (1982).
Suquet, H., C. De La Calle, and H. Pezerat, Swelling and StructuralOrganization of Saponite," Clays and Clay Minerals, 23, 1-9 (1975).
Sykes, M. L., G. H. Heiken, and J. R. Smyth, Mineralogy and Petrology of TuffUnits from the UE25a-1 Drill Site, Yucca Mountain, Nevada," Los AlamosNational Laboratory report LA-8139-MS (November 1979).
Vaniman, D., D. Bish, D. Broxton, F. Byers, G. Heiken, B. Carlos, E. Semarge,F. Caporuscio, and R. Gooley, Variations in Authigenic Mineralogy andSorptive Zeolite Abundance at Yucca Mountain, Nevada, Based on Studies ofDrill Cores USW GU-3 and G-3," Los Alamos National Laboratory reportLA-9707-MS (June 1984).
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55