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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

MINERALOGIC CROSS SECTIONS OF YUCCA MOUNTAIN

30

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

w'

APPENDIX B (cont)

A.,

I.0I.

Glass

- vitrophyre

= vitric nonwelded

Fig. B-2 (cont)

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)

'''

II-.

£1

IS.

A m-.

Trldymite

Fig. B-3 (cont)

w

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)

'Ij

APPENDIX (ont)

0

I

II

H '*

1._

oft"

I..

* " ft

Smectite c5>%)

Fig. B-5 (cont)

* Z.

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

-IJ .

APPENDIX B (cont)

i

or

.

I-,rI.-

Major Cnoptilotite/Mordenlte Intervals

Fig. -6 (cont)

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)

b.

APPENDIX B (cont)

0Osl.-.

"a"

'4.

I

I .., , , .

~~~tt r 4 ~ 1 ..

Analckov

Fig. B4 (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.

.

APPENDIX B (cont)

0

4I

0 01010

MI

I

40

0 we0 lo0wVMRfS

Authigenic Albite

Fig. B-8 (cOnt)

-(

S

APPENDIX B (ont)

0. .scfa

us

vit

"NoNoI-or

(Dr-

...

I

I5-

- Jr

Authigenic Albite

Fig. B-8 (cont)

REFERENCES

Barth, T. F. W., Theoretical Petrology, John Wiley Sons, Inc., New York(1952).

Bentley, C. B., J. H. Robison, and R. W. Spengler, Geohydrologic Data forTest Well USW -5 Yucca Mountain Area, Nye County, Nevada," U.S.Geological Survey Open File report 83-853 (1983).

Bish, D. L., F. A. Caporuscio, J. F. Copp, B. M. Crowe, J. D. Purson, J. R.Smyth, and R. G. Warren, Preliminary Stratigraphic and PetrologicCharacterization of Core Samples from USW-G1, Yucca Mountain, Nevada,"Los Alamos National Laboratory report LA-8840-MS (November 1981).

Bish, D. L. and E. Semarge, "Mineralogic Variations in a Silicic TuffSequence: Evidence for Diagenetic and Hydrothermal Reactions," 19thAnnual Clay Minerals Society Meeting, Hilo, Hawaii, August 8-14, 1982(Abstract).

Bish, D. L., D. T. Vaniman, F. M. Byers, Jr., and D. E. Broxton, Summary ofthe Mineralogy-Petrology of Tuffs of Yucca Mountain and the Secondary-Phase Thermal Stability in Tuffs," Los Alamos National Laboratory reportLA-9321-MS (November 1982).

Bish, D. L., A. E. gard, D. T. Vaniman, and L. Benson, Mineralogy-Petrologyand Groundwater Geochemistry of Yucca Mountain Tuffs," in ScientificBasis for Nuclear Waste Management VII, Materials Research SocietySymposia Proceedings, Boston (G. L. McVay Ed.), 283-391 (1984a).

Bish, D. L., D. . Vaniman, R. S. Rundberg, K. Wolfsberg, W. R. Daniels, andD. E. Broxton, "Natural Sorptive Barriers in Yucca Mountain, Nevada, forLong-Term Isolation of High-Level Waste," Radioactive Waste Management,Vol. 3, 415-432 (984b).

Borg, I. Y. and D. K. Smith, Calculated X-ray Powder Patterns for SilicateMinerals, Geological Society of America, Memoir 122, 896 pp (1969).

Byers, F. M., "Petrochemical Variation of Topopah Spring Tuff Matrix withDepth (Stratigraphic Level), Drill Hole USW G-4, Yucca Mountain, Nevada,"Los Alamos National Laboratory report LA-10561-MS (December 1985).

Caporuscio, F., D. Vaniman, D. Bish, D. Broxton, B. Arney, G. Heiken, F.Byers, R. Gooley, and E. Semarge, Petrologic Studies of Drill CoresUSW-G2 and UE25b-IH, Yucca Mountain, Nevada," Los Alamos NationalLaboratory report LA-9255-MS (July 1982).

Caporuscio, F. A. and D. T. Vaniman, Iron and Manganese in Oxide Minerals andin Glasses: Preliminary Consideration of Eh Buffering Potential at YuccaMountain, Nevada," Los Alamos National Laboratory report LA-10369-MS,(April 1985).

Carlos, B. A., Minerals in Fractures of the Unsaturated Zone from Drill CoreUSW G-4, Yucca Mountain, Nye County, Nevada," Los Alamos NationalLaboratory report LA-10415-MS (April 1985).

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).

Chung, F. H., "Quantitative Interpretation of X-ray Diffraction Patterns ofMixtures. I. Matrix-Flushing Method for Ouantitative MulticomponentAnalysis," Journal of Applied Crystallography, 7, 519-525 (1974a).

Chung, F. H., "Quantitative Interpretation of X-ray Diffraction Patterns ofMixtures. 1I. Adiabatic Principle of X-ray Diffraction Analysis ofMixtures," Journal of Applied Crystallography, 7, 526-531 (1974b).

Craig, R. W., R. L. Reed, and R. W. Spengler, Geohydrologic Data for TestWell USW H-6 Yucca Mountain Area, Nye County, Nevada," U.S. GeologicalSurvey Open File report 83-856 (1983).

Gillery, F. H., "Adsorption-Desorption Characteristics of SyntheticMontmorillonoids in Humid Atmospheres," American Mineralogist, 44,806-818 (1959).

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).

Klug, H. P. and L. -E. Alexander, X-ray Diffraction Procedures for Poly-crystalline and Amorphous Materials, John Wiley & Sons, Inc., New York(1974).

Knauss, K. G., V. M. Oversby, and T. J. Wolery, Post Emplacement Environmentof Waste Packages," in Scientific Basis for Nuclear Waste Management VII,Materials Research Riciety Symposia Proceedings, Boston (G. L. McVayEd.), 301-308 (1984).

Lappin, A. R., Bulk and Thermal Properties of the Functional Tuffaceous Bedsin Holes USW-G1, UE25A#1, and USW-G2, Yucca Mountain, Nevada," SandiaNational Laboratories report SAND82-1434 (1982).

Lappin, A. R., R. G. VanBuskirk, D. 0. Enniss, S. W. Butters, F. M. Prater, C.B. Muller, and J. L. Bergosh, Thermal Conductivity, Bulk Properties, andThermal Stratigraphy of Silicic Tuffs from the Upper Portion of HoleUSw-G1, Yucca Mountain, Nye County, Nevada," Sandia National Laboratoriesreport SAND81-1873 (March 1982).

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).

Levy, S. S., Studies of Altered Vitrophyre for the Prediction of NuclearWaste Repository-Induced Thermal Alteration at Yucca Mountain, Nevada,"in Scientific Basis for Nuclear Waste Management VII, Materials ResearchSociety Symposia Proceedings, Boston (G. L. McVay, Ed.), 959-966 (1984b).

Moncure, G. K., R. C. Surdam, and H. L. McKague, Zeolite Diagenesis BelowPahute Mesa, Nevada Test Site," Clays and Clay Minerals, 29, 385-396(1981).

Price, R. H., S. J. Spence, and A. K. Jones, Uniaxial Compression Test Serieson Topopah Spring Tuff from USW GU-3, Yucca Mountain, Southern Nevada,"Sandia National Laboratories report SAND83-1646 (February 1984).

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).

Zielinsky, R. -A., "Evaluation of Ash-Flow Tuffs as Hosts for RadioactiveWaste: Criteria Based on Selective Leaching of Manganese Oxides," U.S.Geological Survey Open File report 83-480 (1983).

55