AECL-6439

ATOMIC ENERGY A A L'ÉNERGIE ATOMIQUEOF CANADA LIMITED f S j P DU CANADA LIMITÉE

A GEOLOGICAL RECONNAISSANCE STUDY OF M LAC DU BONNET BATHOLITH

LEVE DE RECONNAISSANCE GEOLOGIQUE DU BATHOLITE DU LAC DU BONNET

H. Y. Tammemagi, P. S. Kerford, J. C. Requeima and C. A. Temple

Whiteshell Nuclear Research Etablissement de RecherchesEstablishment Nucléaire? de Whiteshefl

Pinawa, Manitoba ROE 1LOFebruary 1980 février

ATOMIC ENERGY OF CANADA LIMITED

A GEOLOGICAL RECONNAISSANCE STUDY OF THE LAC DU BONNET BATHOLITH

* * *H.Y. Tammeraagi, P.S. Kerford , J.C. «iequeima and C.A. Temple

Summer Student

Whiteshell Nuclear Research EstablishmentP'.nawa, Manitoba ROE 1LO

1980 February

AECL-6439

LEVE DE RECONNAISSANCE GEOLOGIQUE DJ BATHOLITE DU LAC DU BONNET

de

H.Y. Tamnemagi, P.S. Xerford*, J.C. Requelma* et C.A. Temple*

RESUME

On a effectué un levé de reconnaissance géologique du batho-

11 te du Lac du Bonnet, dans le sud-est du Manitoba, dans le cadre de la

phase de vérification dr concept du programme canadien de stockage des

déchets de combustible njclôaire.

Ce rapport résume les données géologiques obtenues, présente

les résultats de la cartographie du terrain et examine les analyses

géochimiques des échantillons de roches. It décrit les aspects géolo-

giques et structuraux du batholite ainsi que sa disposition régionale et

sa genèse possible.

* Etudiant d'été

L'Energie Atomique du Canada LimitéeEtablissement de Recherches Nucléaires de Whiteshell

Pinawa, Manitoba ROE 1L01980 février

AECL-64.39

A GEOLOGICAL RECONNAISSANCE STUDY OF THE LAC OU BONNET BATHOLITH

by

* * A

H.Y. Tammemagi, P,S. Kerford , J.C. Requelma and C.A. Temple

ABSTRACT

A geological reconnaissance survey was carried out of the Lac

du Bonnet batholith, southeastern Manitoba, a6 part of the concept veri-

fication phase of the nuclear fuel waste disposal program for Canada.

This report summarizes available geological information, presents the

results of field mapping and discusses the geochemical analyses of reck

samples. The geological and structural aspects of the batholith are

described as well as its regional setting and possible genesis.

Summer student

Atomic Energy of Canada LimitedWhiteshell Nuclear Research Establishment

Pinawa, Manitoba ROE 1L01980 February

AECL-6439

CONTENTS

1. INTRODUCTION

2. REGION/IL GEOLOGY

S. METHOD

4. GEOLOGY

Page

4.1 THE LAC DU BONNET BATHOLITH 64.2 THE COUNTRY ROCKS 94.3 MICROSCOPIC DEFORMATIONAL FEATURES 11

5. STRUCTURE 13

5.1 FOLIATION 135.2 JOINT FRACTURE SETS 14

5.2.1 General 145.2.2 Old Pinawa Dam Site 165.2.3 Discussion 17

5.3 LINEAMENT STUDY 18

6. GEOCHEMISTRY 20

6.1 CHEMICAL ANALYSES 206.2 COMPARISON TO OTHER GRANITES 216.3 DISCUSSION 21

6-j.l Ternary Plots 216.3.2 Alkalinity and Differentiation

Indices 226.3.3 Areal Distribution 236.3.4 Magma Source 246.3.5 Other Rock Types 26

7. CONCLUSIONS 27

8. ACKNOWLEDGEMENTS 29

REFERENCES 30

TABLES 33

FIGURES 39

APPENDIX A - GEOCHEMICAL RESULTS 61

1. INTRODUCTION

A program to demonstrate the viability and safety of under-

ground disposal of nuclear wastes has been initiated by Atomic Energy of

Canada Limited. The general outline and objectives of the program have

been described previously '""' . The rock formations which are receiv-

ing the main focus of attention are large igneous intrusive masses with-

in the Canadian Shield These plutons and batholiths are particularly

attractive since they occur in the Canadian Shield, which forms over 50%

of the Canadian landmass and is centrally located within the country.

Furthermore, the Canadian Shield is one of the most stable landforms in

the world, most of it having been essentially quiescent for the past

1000 million years or longer. Thousands of plutons exist in the shield;

they are large, relatively uniform and any economic mineralization, if

i.t occurs at all, is generally restricted to their margins. Approxi-

mately 1500 plutons exist in Ontario, the province where the disposal

vault will ultimately be located.

Research to demonstrate the suitability of crystalline rocks

such as plutons for nuclear waste disposal has only commenced in the

last few years and much still needs to be learned. For example, frac-

tures occur in plutons, as they do in all geological media, and tech-

niques to predict and understand them are needed. In particular, the

groundwater flow regime, which in this medium occurs primarily through

fractures, must be thoroughly investigated. The petrological, geochem-

ical and structural aspects of several types of plutons must be thor-

oughly investigated to develop the data necessary to demonstrate that

this disposal concept is safe.

The Canadian development program consists of three phases, the

first of which is entitled Concept Verification . The object of the

concept verification phase is to carry out a broad range of research

topics including the investigations mentioned in the previous paragraph

- 2 -

In order to verify that effective isolation of nuclear wastes can be

achieved by disposal some 500 to 10C0 m deep into plutons in the Cana-

dian Shield. It must be stressed that this phase of the program is a

research phase and only on its completion will the site selection phase

commence. The research is generic in nature and will investigate forma-

tions which represent different categories of available rock types US

shown below:

Less Fractured

More Fractured

Granite Syenite Anorthosite Gabbro

The reconnaissance geological study described in this report

forms only a small part of the investigation which is being performed on

the Lac du Bonnet batholith as part of the concept verification program.

The other studies will be reported independently, however, an overview

is presented in reference 4.

The object of this study was to gather together the available

geological information concerning the Lac du Bonnet batholith and to

supplement that data with some reconnaissance mapping and sampling over

the body. During the field mapping, emphasis was placed on defining

structural features. This report is designed to serve as a handbook of

available geological data for other investigators, such as hydrogeolo-

gists and geophysicists, who are studying the batholith. It can also

form the basis for more thorough geological investigations.

2. REGIONAL GEOLOGY

The Lac du Bonnet batholith is located in southeastern Mani-

toba about 16 km vest of the Manitoba-Ontario border and about 50 km

- 3 -

north of the Trans-Canada highway. Its location is shown in Figure 1.

The batholith Is elongated in shape with its major axis striking ENE.

It extends from near Pointe du Bois for 80 Jan to the WSW. as far as

Tyndall, where its presence is inferred by its magnetic expression .

The maximum width is clone to 25 km and the areal extent is over 1000 km .

The Whiteshell Nuclear Research Establishment (WNRE) occupies approxl-2

mately 45 km on the southern edge of the batholith.

In general the Plutonic rocks within the Canadian Shield have

received far less attention than the economically more interesting

greenstone belts. This is particularly the case for the Lac du Bonnet

batholith and the following summary contains virtually all the published

references dealing with this body. The rock is a pink, massive homoge-

neous quartz monzonite cut by numerous pegmatite and aplite dikes .

Field evidence suggests that the Lac du Bonnet batholith postdated the

last major orogenic activity and it is considered to be intrusive Into

both the adjacent Bird River greenstone belt and the Great Falls quartz

diorite bodies . Dikes believed to be related to the batholith cut

t'.ie quartz diorites and the metavolcanic and sedimentary rocks. Xeno-

liths of the latter two units have been observed in the batholith. Itsf f\\ ft 7 Rft

age, as found by Penner and Clark using Rb/ Sr age determinationmethods, Is 2495 + 130 Ma. This age supports the interpretation that

this is the youngest of the granitic rocks in the region and that it is

post-tectonic.

Penner and Clark^ interpret the high initial 87Sr/86Sr

ratio to suggest that the batholith originated from either pre-existing

crustal material or that the isotopic composition has been altered by

assimilation of rubidium-rich rocks during emplacement. This agrees

with the interpretation that the mqgma was generated by anatexis of(7 8 9̂

earlier igneous and metamorphic suites ' .

Farquharson revised the Rb-Sr age of the batholith to

2680 + 91 Ma. This would mean that the major periods of plutonism and

accompanying periods of regional metamorphism were concluded by about

this time. Further work is necessary in this area.

A number of pegmatites containing rare elements occur in the

country rock near the northeast end of the batholith . One of chesi

the Tanco deposit, is currently being mined for tantalum, lithium and

cesium. It is believed that these pegmatites a:

du Bonnet batholith by magmatic differentiation

cesium. It is believed that these pegmatites are derived from the Lac

.(7)

Regionally the Lac du Bonnet batholith is located in the

English River subprovince which is one in a series of large east-west

trending Archaean subprovinces within the Superior province of the

Canadian Shield . The English River subprovince consists of two

parts: the northern part in which sedimentary gneiss is dominant and

the southern part in which felsic plutonic rocks are the most abundant.

The terms Ear Falls-Manlgotagan gneiss belt and the Winnipeg River

batholithic belt have been introduced for the northern and southern( 12)

parts, respectivelyv '. The Lac du Bonnet batholith is located in the

latter belt. Figure 2 shows the regional geology.

The batholith is located in the centre of a large block which

is bounded by major faults. The faults, which formed in the last phase

of the Kenoran orogeny, probably represent sutures with an original( 8}

vertical scale of crustal proportions .

Outcrop is extensive to the east of the town of Lac du Bonnet

but to the west there is virtually no outcrop at all, with only the very

occasional rounded hillock of granite protruding through the glacial

cover. Exposure on the WNRE site is limited to three outcrops, of which

the largest has an area of 17 000 m while the other two are substan-

tially smaller. The sedimentary cover in the site area originated from

Wisconsin glaciations of the Pleistocene epoch and associated phases of

glacial Lake Agassiz. The major superficial deposits in the study area

are lacustrine clay and silty clay, lacustrine sand and gravel, sandy

- 5 -

till and associated poorly sorted sandy deposits . The total se-

quence of glacial deposits on the WNRE site does not exceed 25 m and is

generally between 10 and 15 in. Figure 3 shows a typical cross section

of these deposits.

3. METHOD

Field work was carried out in the summers of 1977 and 1978 and

uost of the laboratory a-alysis was done in the fall and winter 1978/79.

The field work was focussed primarily on the central part of the batho-

lith with only a few observations made in the eastern- or western-most

ends of the formation (Figure 4). Studies of the eastern part of the(14)

batholith are being undertaken as part of another project

A total of approximately 140 outcrops were visited during the

course of the study. At the 73 sites shown in Figure 4, observations

were made, samples taken and fractures measured. Table 1 is a checklist

of the observations made and recorded for each of these sites. At the

remaining sites the rock type, grain size, dikes, inclusions and usually

a summary of the main fracture sets were recorded.

Satellite images (Landsat, 1:1 000 000 band 7) were inspected

to delineate any major fractures. No major lineaments were observed,

although the parallel trends of the Winnipeg River and the Pinawa

Channel as they cross the batholith may be more than a coincidence.

Aerial photographs were used to perform a lineament analysis similar to

that employed by the Geological Survey for categorizing plutons

The analysis was done by selecting wo areas of the batholith, each of2

about 56 km . similar in size to the intrusive masses beinj: considered'15)

by Brown and Thiviergev . By measuring any natural feature which had

some sort of a linear attitude, a "lineament density" could be calcu-

lated. In addition, percentage outcrop and "major lineament density"

- 6 -

were calculated, with major lineaments defined as having a length great-

er than or equal to half the length of the smallest dimension of the

body (In this case the diameter of the chosen area). Consequently,

any lineament longer than three kilometres was arbitrarily considered a

major lineament.

The following laboratory analyses were performed:

a) Analysis "f 28 thin sections, using a petrological microscope

to detenu le mineral content, relationships between grains,

crack-filling materials, strain in the rock and mineral re-

plaçaient.

b) Standard whole rock analysis of 45 samples for SiO.,, A^O.,

FeO, Fe2O3, CaO, MgO, Na2<>, K2<J, C02> TiO2> MnO and P ^ .

Analyses for a number of trace elements were also carried out.

The structural data obtained from field mapping were reduced

using a computer program which displayed the dp.ta as equal area

polar density projections and which also separated the bearings of the

fractures into 10" sectors for use in Rose diagrams.

4. GEOLOGY

4.1 THE LAC DU BONNET BATHOLITH

Figure 5 is a geol' 'leal map of the Lac du Bonnet (LDB* batho-

lith. The batholith is predominantly a pink, medium- to coarse-grained,

slightly porphyritic granlte-granodiorite. The porphyrltic texture of

the granite Is most developed in the centre of the batholith, tending to

be more equigranular towards the boundaries.

- 7 -

The edges of the batholith show a very distict foliation and

banding of the type which Balk attributes to the magma being dragged

along the contact, forcing alignaient of some minerals parallel to the

contact. The boundaries have many darker inclusions of the country

rock, which show varying degrees of assimilation.

Field mapping has resulted in the redrawing of the southern

contact of the batholith (Figure 5).

Mineralogically the rocks consist almost wholly of potassium

feldspar (orthoclase), plagioclase and quartz with minor amounts of

biotite. Microcline phenocrysts iorm about 5% of the granite and vary(18)

in size, but usually range from 1-3 cm. Ziehlke termed this type "£

phenocryst, or late stage megacryst, a deuteroblast. Tte6e deutero-

blasts developed early enough that late-stage movement" of the magma

oriented them, allowing the general preferred direction to be measured

in the field. Kleeman1 ' and Beakhouse^ have suggested that the

development of these potassium feldspar deuteroblasts is best considered

as a fractional crystallization process. Figure 6 shows modal abundances

of the minerals. It is seen that the Lac du Bonnet batholith is a gran-

ite to granodiorite, according to the IUGS classification system.

An equigranular coarse-grained groundmass makes up approxi-

mately 95% of the total rock and consists of roughly a 2:1 ratio of

plagioclase (402) to potassium feldspar (25%), along with quartz (30%)

and minor amounts of biotite (5%). The plagioclase is oligoclase in

composition and often crystals are zoned with a more sodic rim. The

potassium feldspars show perthitic and cross-hatching character. Acces-

sory primary minerals include apatite, zircon, muscovite, epidote and

some opaques.

Alteration products of the early formed igneous minerals are

chlorite and magnetite replacing biotite, and sericite along with

International Union of Geological ̂ Sciences

- 8 -

muscovita and epidote replacing plagioclase. Weathering on the granite

has produced iron oxides (goethite and/or hematite). Numerous cracks

are present.

Even though more than 99 percent nf the batholith was mapped

as pink equlgranular-to-slightly-porphyritic grtiite, two separate minor

phases of the batholith were observed. One was located at the Old

Pinawa dam site and the other was intersected at the WNRE Geotechnical

Activity Site by diamond drill holes, WN1, WN2 and WN3.

The Old Pinawa phase can be best described as a leucocratic,

light grey, medium-grained, equigranular tonalité, with approximate

mineral concentrations of 60-702 plagioclase, 15-252 quartz, 2-107.

bxotitt. and 0-10% potassium feldspar. No foliation was observed.

The phase observed at a depth of 46.5 to 96.9 m in the drill

holes also shows very little potassium feldspar (0-5S), but unlike the

Old Pinawa tonalité, this plutonlc rock is composed of 10-15Z biotite,

with locally higher concentrations. Quartz makes up 257. of the rock

while plagioclase makes up the remaining 45-50%. This phase shows a

slight foliation of the biotite minerals.

Pegmatites are consistently found through the batholith in two

forms:

1. As long straight dikes with discrete boundaries. These pro-

bably formed as the result of pegmatitic fluids filling in

primary fractures.

2. As patches and blobs of pegmatite without discrete boundaries.

These probably tormed from products of volatile-rich residual

melts or fluids which were not tapped by fractures.

The pegmatites consist of microcline-perthite and quartz whose

concentrations vary greatly with location. Crystal sizes usually range

- 9 -

from a few centimetres to 10 cm, but potassium feldspar orvstals with

diameters as large as 20 cm have been observed. Accessory minerals of

the dikes are a red garnet, probably almandine, and allanite. Aplites

occasionally occur as dikes but are far Ies6 common than the pegmatites.

Zenollths in the granite appear to be derived from the nearby

country rock. In addition, amphibolite inclusions are sparsely scct-

tered throughout the batholith.

A single green to black ultramafic (dunite) inclusion, found

in the centre of the pluton (site 43), is not representative of any of

the other xenollths. It is an equigranular, medium-grained rock con-

sisting of olivlne (about 802), pyroxene (about 15X) and alteration pro-

ducts (about 57.) with trace amounts of calcite and opaques. This ultra-

mafic inclusion may be indicative of a larger buried mass since its lo-

pronc,(21)

cation coincides with a pronounced magnetic high and an unexplained

positive gravity anomaly

The pluton contain* numerous zones of darker material with the

appearance of schlieren. These are generally wavy in form (probably

indicative of a flow structure), of dimension 30-100 cm, and are richer

in biotite than the granite.

4.2 THE COUNTRY SOCKS

The country rocks and their relationships to the gran te body

were observed at four locations. These locations are shown as A, B-B1,

C-C and D-D' in Figure 5.

From thià reconnaissance study three geological units were

differentiated. In chronological order from oldest to youngest they

are:

- 10 -

1. Metaeedlmentary Unit

A foliated metasedimentary unit was observed at the northeast

contact along the Bird River road. (Figure 5, site A). The

fine-grained sediment in composed of biotite, hornblende and

plagioclase along with larger mediua-grained crystals of gar-

nets. The hornblende and plaglo^lase are metamorphic contact

derivatives of the sediments. The original sediment was prob-

ably a calcium- and iron-rich siltstone1 .

2. Quartz Piorite-Granodiorlte Gneissic Unit

A large gueiusic unit, extending tens of kilometres in length

and width, borders the batholith to the south.

The gneissic unit consists primarily of a medium-coarse

grained, bluey grey-black quartz diorite, which 1B strongly

foliated, end its partially banded, white-black anatectlc

derivative. The layers are made up of two major groups of

minerals: a light-colored layer composed of quartz and pla-

gioclase and a dark-colored layer composed of biotite, plagio-

clase and some hornblende.

Inclusions of fine- to medium-grained amphibolite are scat-

tered through the gneissic unit. These inclusions vary in

size from a few centimetres to tens of metres in length and

are blocky or lenticular in shape. Hornblende, plagioclase

and biotite comprise the major minerals of the amphibolite.

Biotite is an alteration product of hornblende

The gneissic unit has been intruded by dikes of varying age

and composition. Pink pegmatites and lesser numbers of ap-

lites are the most abundant and latest in the sequence of

dikes. The color, textures and mineralogy of these dikes are

such that they are interpreted as being oxfshoots from the

main body.

- 11 -

Earlier lighter colored, biotite-poor grandiorite-quartz dio-

rite dikes also cut the gneissic belt.

As the contact of the batholitli is approached, the <?rey gneiss

becomes more heavily Intruded by pegmatitles and grades into

a more felsic rock, showing bands of orangy-red feldspar and

black biotltes, which giva it a migmatitic appearance. It is

our belief that this gradation from grey gneiss to migmatite

along the contact of the batholith was due to metasoznatic

fluids derived from the batholith.

3. Great Falls Quarts Diorite

The Great Falls quartz diorite Is a large, medium-grained,

black and white speckled pluton found to the north of the Lac

du Bonnet batholith. From field relations, the Great Falls

intrusive Is considered earlier than the batholith since the

LUC du Bonnet batholith contains inclusions of the quarcz-rich

diorite rock.

Plagioclase is the major feldspar forming up to 60% of the

rock while quartz (25%) and biotite (15%) are the lesser com-

ponents. In outcrop only a slight foliation exists.

4.3 MICROSCOPIC DEFORMATIONAL FEATURES

A study of the microscopic deformational features of the Lac

du Bonnet batholith and some of the country rocks showed that the batho-

lith has undergone the least amount of deformation of the units in the

area. The metasediments and the gneissic units have been subjected to

metamorphism, as recrystallization and crushing were evident in all thin

sections.

Fifteen thin sections of LDB granite were inspected and their

cataclastic features recorded- They were divided into three groups,

based upon the amount of deformation, on the following basis:

- 12 -

1. Deformed

a. Quartz grains exhibiting undulose extinction and deforma-

tion bands

b. Finer crushed grains or microbieccia

c. Quartz grains showing a mosaic textu/e with interfacial

angles of about 120°

d. Kinking in the biotlte crystals

e. Small biotlte crystals, and finely crushed material

occasionally wrapped around larger crystals - giving an

augen-type texture

f. Plagioclase crystals fractured across their lamellae and

often bent.

2. Moderately Deformed

a. Quartz exhibiting undulose extinction

b. Quartz forming defcrmational bands

c. Quartz grains showing a mosaic texture with interfacial

angles of about 120° and some crushing.

3. Minor Deformation

a. Quartz exhibiting undulose extinction

b. Quartz forming deformational bands.

The locations of the three groups of deformation are shown in

Figure 7. The parts of the batholith that are deformed most are local-

ized at the borders. This type of localization, according to Moor-(22)house , is often indicative of a protoclastic origin whereby the

intrusive is still in movement after the granite has partially or wholly

solidified causing a crushing of the finer crystals. In the central

part of the batholith a slight decrease in the amount of deformation is

- 13 -

observed from south to north, with samples at the north showing virtu-

ally no deformation. The significance of this trend is not known.

5. STRUCTURE

5.1 FOLIATION

Rocks generally display a foliated character of two main

types: primary foliation caused by flow in the liquid or partially

liquid state and secondary foliation caused by shearing of the solidi-

fied rock.

From field and pétrographie studies of the Lac du Bonnet

batholith and surrounding regions, the following conclusions have been

derived:

1. The foliation in the batholith is of prir .— origin. This

conclusion is based on the following observations: the folia-

tion is generally parallel to the wall rock; the phenocrysts

generally show no signs of deformation or of rotation into

their preferred direction after magma solidification; and the

granite displays a normal interlocking texture of the minerals.

2. The foliation in the couuLry rock is of secondary origin.

This is displayed by an abundant amount of cataclastic deform-

ation in crushing, by the reorientation of crystals and by the

recrystallization of minerals.

The orientation o£ foliations measured in at;d around the bath-

olith is displayed in Figure 8. The near vertical and steeply dipping

foliation in the granite indicate that the batholith probably has near

vertical or slightly outward dipping boundaries and is not a shallow

dipping sheet to the north as postulated by McRltchie .

- 14 -

5.2 JOINT FRACTURE SETS

5.2.1 General

Measurements and observations of the fracture or joint systems

were made at 73 slues, as described in section 3, by laying two perpen-

dicular measuring tapes across the outcrop. All fractures which inter-

sected the measuring line were recorded.

The object of these observations was to record quantitative

descriptive data on fractures which could assist in developing an under-

standing of groundwater flow in fractured crystalline rock. Some of the

parameters which need to be determined are: orientation, length, frac-

fre termination, connectivity (i.e., how is one fracture connected to

another and how continuous is the fracture itself), spacing and sheeting.

The major difficulty in obtaining the required data is that,

aside fiom orientation measurements, very little work has been done pre-

viously in this area. Thus, there is no commonly accepted terminology

nor standard field technique. In addition exposures of bedrock are gen-

erally not sufficient in areal extent to obtain data on fracture lengths.

It is difficult to classify joints because of their great variability in

shape and character, which is further complicated by near-surface weath-

ering effects such as exfoliation.

Large areas of outcrop are very scarce and thus it was diffi-

cult to assess quantitatively the length of the fractures. In general

they are a metre to several tens of metres in length and are vertical to

subvertical in dip.

Fractures in the batholith terminate in a variety of ways.

Many of them end in other fractures while others die out in bare rock.

Some fractures bifurcate into two separate fractures which usually end

in bare rock while others splay off into several small cracks.

- 15 -

Sheeting is evident throughout the batholith as irregular wavy

fractures. Many large, flat outcrops appear to be sheet fracture sur-

faces.

When analyzing the ler.gths of fractures, two groups were used:

1. Fractures with known lengths

2. Fractures with unknown lengths, where one or both ends of a ,•

fracture are covered by overburden, yielding only a minimum /

length.

Average length of fractures with known lengths is 6.2 metres

while the average length for fractures with unknown length- is greater

than 15.2 metres. A histogram (Figure 9) of the length of fractures

versus the number of fractures clearly shows that as the length of frac-

tures increases the number of fractures recorded decreases. Since out-

crops %rere seldom larger than a few tens of metres in dimension, a large

proportion of the fractures had unknown lengths due to their termination

under overburden.

The strikes of fractures were recorded and displayed on indi-

vidual Rose diagrams for each site. The orientations of the fracture

sets do not show any major trends related to the shape of the pluton.

The strikes of all fractures in the batholith were then combined on a

single Rose diagram (Figure 10). Two main sets of fractures exist in

the batholith: a NE.-SW. striking set and another which strikes NW.-SE.

These main fracture sets were compared with a Rose diagram for the frac-

tures of the country rocks (Figure 10) and regional fracture maps by

McRitchie^ ' and Grisak et al.' K The orientations of the fractures

in the country rock, although exhibiting more variation and an additional

N.-S. set, are similar to those recorded in the batholith. The main

fracture set orientations were compared to the foliation orientations

recorded at several sites throughout the batholith. The data clearly

- 16 -

Indicated that the major fracture sets do not parallel the foliation

directions at any ot the sites. Therefore it is concluded that the

fracture patterns in the pluton probably reflect the action of regional

stresses and are not related to the foliation formed by the emplacement

of magma.

The SW.-NE. trending fracture set has an average spacing of

3.2 metres/fracture while the NW.-SE. striking fracture set has an

average spacing of 2.8 metres/fracture. Average spacing at specific

sites ranges from 1 to 10 metres/fracture.

The orientation of pegmatite dikes in the pluton is shown su-

perimposed on the Rose diagram of Figure 10. A definite NE.-SW. trend

is apparent. This coincides with the orientation of one of the fracture

sets. It is concluded that the NE.-SU. striking fractures were the ear-

liest fractures to have formed In the batholith.

The results of this section (and the next one) are preliminary

in nature and more work needs to be done in this area. In addition to

standardizing field techniques and terminology, the observations need to

be described in a more rigorous quantitative fashion. Because of the

inherent variability in fracture data, a statistical approach to frac-

ture description seems warranted.

5.2.2 Old Pinawa Dam Site

At Old Pinawa, an abandoned dam site (site 15 on Figure 4),

the exposure of outcrop is far superior to that found elsewhere in the

batholith. For this reason a more detailed fracture study was carried

out at this site. Figure 8 shows the position of Old Pinawa with re-

spect to the batholith. Two study sites were chosen: study site A

which exhibited a greater fracture density than average and site B which

showed only very light fracturing. A and B are located about 150 m from

each other.

- 17 -

For this phase of the study, a more detailed fracture mapping

method was devised which allowed large fractures to be described in

terms of their component fractures (Figure 11). It was felt that the

new mapping procedure would record the maximum joint information. The

component fractures, which show offsets of a few centimetres up ci> a

quarter of a metre, often are not connected to each other at the sur-

face. To what degree the fracture components are connected to each

other at depth is unknown. Long joints that are composed of a number of

offBet components are ubiquitous throughout the batholith. This obser-

vation is important fcr hydrogeological studies since potential ground-

water flow along such fractures could be seriously restricted by the

offsets.

The strikes of all fractures recorded at Old Pinawa are dis-

played on a Rot.o diagram in Figure 10c. The diagram shows three main

sets: a NE.-SW. set (Set 1), a NW.-SE. set (Set 2), and a NNW.-SSE.

set (Set 3). The first two sets are typical of the batholith, but the

third set is not.

Table 2 represents the fracture data collected from study

sites A and B. It is evident that the fracture density varies consid-

erably over very short distances within the pluton.

Figure 12 again illustrates a decrease in the number of frac-

tures as the fracture length Increases. A Rose diagram of the pegmatite

dikes at the Old Finawa dan site shows a definite NE.-SW. trend, which

is similar to the trend of the Set 1 fractures, as seen In Figure 10c.

5.2.3 Discussion

Although there is some inherent variability in the fractures

observed in outcrop on the bathclith, it appears th: - Fractures occur in

sets which can be characterized by orientation and spacing. Individual

joints appear often to be composed of components which are slightly off-

- 18 -

set from each other. Long fractures are less frequent than short ones.

There can be great variability in fracture density even over distances

as small as a few hundred metres. It is concluded that far more re-

search is required In this area of structural geology.

5.3 LINEAMENT STUDIES

Field study of major fracture zones or faults is intrinsically

difficult since such features are generally more eroded than the sur-

roundings, yielding vegetated valleys or forming depressions for rivers

and lakes. However, two large lineaments, visible on an aerial photo-

graph, were visited and inspected. In the field the lineaments are de-

pressions or valleys between two elongated hills. The edges of the

hills are straight and usually sub-vertical and their orientations are

the same as the major joint sets of the hill. No shearing or major

fracture zones are observed on either Hide of the depression. Therefore

the lineaments probably formed as the result of weathering on joint

sets, which may have been locally more closely spaced than average.

An area about 6.5 km by 6.5 km, termed LDB-1, (see Figure 8)

was chosen for analysis of lineament orientations. Figure 13 shews the

lineaments of the study area as well as some north-south and east-west

sampling lines. Wherever a sampling line crossed a lineament, its ori-

entation was recorded. A total of 119 lineament orientations were re-

corded and plotted on a Rose Diagram in Figure lOd where three sets are

seen: NE., N.-S. and SE. When this diagram is compared to Rose dia-

grams of fractures (Figures 10a and c) a definite correlation can be

seen. The NE.-SW. and the NW.-SE. liniment sets are similar in orien-

tation to the major joint sets in the batholith. Although the north-

south set of lineaments does not correlate with any major fracture set

in the batholith (Figure 10a), it does correlate with the third set

found at Old Pinawa as well as with fracture sets recorded at various

individual sites around the batholith. Therefore it is possible that

these lineaments are large-scale erosion features of joint sets which

- 19 -

may locally be quite closely spaced. An interesting feature is thai the

NE.-SW. lineament set is parallel to the trend of the Winnipeg River and

Pinawa Channel.

Two areas, LDB-1 and LDB-2, o-ich about 6.5 x 6.5 km f.soe Fig-

ure 8 ) , were chosen for lineament analysis similar to that performed by

Brown and Thivietge , so that the LDB batholith could be compared to

plutons in Ontario being categorized by the Geological Survey of Canada.

They tabulated data for 317 plutons on the basis of size, outcrop, major

lineament density and total lineament density, and selected the 22 which

had the most optimal structural conditions of the last three parameters,

as well as being greater than three kilometres in diameter. Measure-

ments on the LDB batholith yielded the following data:

Site % Outcrop Major lineament density Total lineament density

(mile/mile2)* (mile/mile2)*

LDB-1 35 0.53 4.43

LDB-2 12 0.60 2.73

Figure 14 shows a summary from reference 15, with the LDB-1

and LDB-2 data superimposed. LDB-1 and LDB-2 rank in the part of the

group which has better structural integrity, that is, fewer fractures.

Therefore the LCB batholith belongs to the less fractured, granitic

group of rocks as defined in the matrix of rock types to be assessed

during the concept verification phase (see section 1 ) .

British units are used so that comparison can be made to reference 15.1 mile = 1.61 km; 1 mile2 = 2.59 km 2

- 20 -

6. GEOCHEMISTRY

6.1 CHEMICAL ANALYSES

Forty-five samples were selected for chemical analyses. 1:ie

sample locations, which occur predominantly In the central portion of

the batholith, are shown in Figure 4. Although most of the samples were

of typical LDB granite, a few sampIts of pegmatites, hypabyssal phases

and country rock were included for comparative purposes.

The samples were analyzed for: SiO-, A1.0-, Fe.O , FeO, MgO,

CaO, Ua-O, K_0, TiO_, MnO, Be, Ga, Y, Pb, Sn, C, P, Ba, Rb, Sr, Cs, Li,

Tl, Th, U, Zr and Hf. The selection of those elements was based on

studies by Taylor' ' and Ewers and Scott .

The Department of Earth Sciences, University of Manitoba, the

Analytical Science Branch, WNRE, and a commercial laboratory performed

the analyses, as listed in Table 3. In most instances elemental analyses

were performed both at the University of Manitoba and at WNRE and cross-

checks were carried out by other laboratories. For the sake of consis-

tency, University of Manitoba resu'.ts have been used as far as possible

in this study. WNRE results and interlaboratory cross-checks are des-

cribed in references 26 and 27.

Abundances of the 10 major and 17 trace elements are tabulated

in Appendix A for the 45 rock samples which were analyzed. In addition,

mesonorms were determined, based on the Niggli norm calculation with

alterations by Barth for granite rocks. A computer program was

written to perform the mesonorm calculations, based on procedures out-

lined in reference 29. Average values for LDB granite were determined

from those samples considered representative of the main phase of the

batholith; see Table 4 and Appendix A.

- 21 -

6.2 COMPARISON TO OTHER GRAMITES

The average elemental abundances in LDB granite are compared

to the compositions of the standard granite and granodiorite of Taylor

in Table 4. The elemental abundances were plotted versus the differen-

tiation index of Thorton and Tuttle in Figures 15a and b. These

plots consistently show that the Lac du Bonnet camples follow the gen-

eral trend expected of a rock more differentiated than a standard grano-

diorite or granite.

The concentrations of thorium and uranium in the LDB samples

are high (Table 4 ) . This enrichment was observed by Farquharson to

be characteristic of the English River gneiss belt of which the Lac du

Bonnet btthollth is a member. The Th/ll ratio of 2.8 is lower than that

(33)of standard granite or granodiorite, or than the average value of 4.2

for the Canadian Shield -

The major elemental abundances in the LDB granite are quite

similar to those of a single phase leucogranite of Kolbe and Taylor

In summary, the major and trace element analyses indicate that

the central portion of the LDB batholith is relatively homogeneous and

forms a single phase granite which suffered more differentiation than

the standard granite of Taylor^ .

6.3 DISCUSSION

6.3.1 Ternary Plots

A ternary plot, Figure 16, of QTZ:OR:PLAG (quartz:orthoclase:

plagioclase) calculated from mesonormative mineral abundances shows that

the Lac du Bonnet samples cluster within the granite field of the IUGS

igneous classification system. The average value for QTZ:OR:PLAG is

32:29s39 and comparison to the modal analyses obtained in section 3

- 22 -

shows this same general distribution (Figure 6). Thus the Lac du

Bonnet batholith can be classified as a granite, but with a composition

lying close to the granodiorite boundary.

A Lernary plot, Figure 17, of QTZ:OR:AB (quartz:orthoclase:al-

bite) shows a close cluster of points near the centre of the ternary

triangle. Figure 17 shows that the average LDP, sample falls on the

3000-bar contour of confining pressure. This isobaric minimum is based

upon a water-saturated composition , which is compatible with the

presence of late-stage pegmatites. The uniform chemical composition,

the 3000-bar confining pressure and the presence of pegmatites suggest

that the pluton formed from a magma which solidified at a relatively

shallow depth of 10 km or less.

6.3.2 Alkalinity and Differentiation Indices

The Alkalinity Ratio of Wright(

A1.0 + CaO + Total Alkali

A12O3 + CaO - Total Alkali

is commonly used to distinguish rocks from a common source and to sepa-

rate those phases which are present.

The Lac du Bonnet rocks plot within the alkaline field as seen

in Figure 18. The various fields of the alkalinity ratio versus SiO_

diagram are representative of observed rock associations, but no trends

are observed in the LDB samples suggesting there is only one phase pre-

sent.

Another index of magmatic evolution is the Differentiation(31)

Index of Thorton and Tuttle , which is based upon the sum of the

salic mineral constituents. For the Lac du Bonnet rocks this is the sum

of normative quartz, orthoclase and albite. The index is a guide in de-

- 23 -

termining how far a magma has evolved toward its ultimate composition

and is also a useful means by which to observe variations in chemistry.

The plot of the differentiation index versus SiO, composition,

shown in Figure 19, indicates that the Lac du Bonnet rocks are over-

saturated in SiO, and that they are located within the contour interval

of the most commonly found igneous rocks.

Teng and Strong found a variation of + 8% SiO, for the

single phase Swift Current granite in Newfoundland over a change in dif-

ferentiation index of 25%. The Lac du Bonnet samples have a variation

of + 6% SiO, over 12% change in differentiation index. A similar com-

parison for barium gave a range of + 1000 ug/g for the LDB samples while(25)

the Cullen granite in a study by Ewers and Scott gave ranges from

+ 5000 to + 1000 pg/g for a single phase. This chemical evidence sup-

ports the field evidence which suggests the central portion of the

batholith is essentially single phase.

6.3.3 Areal Distribution

Areal distribution of the elements shows no distinct trends

and often wide variations are observed within a small area. Because of

pegmatitic mineralization in the Bernic Lake area just outside the

northeast boundary of the batholith, particular attention was given to

lithium, beryllium, cesium, rubidium and thallium. However, the concen-

trations of these elements are no higher than would be expected and no

trends in areal distribution can be detected. This lack of persistent

trends for even trace elements reflects the homogeneous nature of the

batholith. It must be stressed that far more sampling is required,

particularly in the eastern portion of the batholith, before definite

conclusions can be drawn.

- 24 -

6.3.4 Magma Source

The volume of magma necessary to produce a body the size jf

the Lac du Bonnet batholith suggests that genesis by differentiation

from a basic magma 1B improbable. Even if the magma had been contami-

nated by silica-containing material, the volume of basic magma would

have had to be enormous to form a batholith of this size. If it had

formed from a basic magma it would seem likely that closely associated

rock bodies or various phases would be present, which is not the case.

Therefore the granite probably originated by partial melting of pre-

existing crustal material.

(38)The peraluminous index of Chappell and White

(Na.O + K-0 + CaO)

was one of the factors they presented to distinguish between igneous or

sedimentary origin of granites. A high value of the index indicates

sedimentary origin. The average value for the LDB standard samples is

1.5, with all samples except one pegmatite having values well above 1.1,

the limit which delineates igneous and sedimentary origins. The two

pegmatite samples both show lower values because of late-stage chemical

changes, which rapidly increase K,0 while reducing Al 0 . The Lac du

Bonnet rocks are therefore considered, by this index, to have probably

formed from a magma derived from a sedimentary rock type.

The presence of more than 1% mesonomative corundum is also

considered to reflect a sedimentary origin . The average corundum

content for the LDB rocks is 2.1%, although it should be noted that* (14)

Chappell and White used a CIFW norm not a mesonorm. Other studiesindicate that the CIPW norm for LDB granite will be significantly lower

(38)than 2.1%. Chappell and White ' felt that granites of sedimentary

origin normally have x Na_O content of less than 3.2%; however the

Cross, Iddings, Firrson and Washington.

- 25 -

average Ha 0 content for the Lac du Bonnet rocks is 3.6Z. These fac-

tors, taken as a whole, are inconclusive, but suggest that a sedimentary

origin is more probable than an Igneous origin.

H 7 Sift ( f\\

The initial Sr/ Sr ratios determined by Penner and Clark

yielded a value of 0.7086 which they interpreted as indicating that the

LDB bathollth originated from pre-existing crustal material or that the

ieotopic composition was altered by assimilation of rubidium-rich rocks

during emplacement. This figure was later revised to 0.6998 by Farquhar-

son which may indicate an upper mantle source. It is considered

that there is insufficient data at the moment to reach a definite con-

clusion.

A ternary plot of Na.CkJCChCaO in Figure 20 shows the Lac du

Bonnet rocks clustering In the same region as the leucogranite of Kolbe( 34)and Taylor . These Snowy Mountains leucogranltej are hypothesized to

have formed from sedimentary rocks. Comparison of elemental abundances

of the Snowy Mountains leucogranites to the Lac du Bonnet samples shows

that major elemental abundances are similar although the trace elements

show a wide variation.

The ternary diagram, Sr:Ba:Rb (strontium:barium:rubidium),

shown in Figure 21, classifies the Lac du Bonnet rock as an anomolous(39)granite according to El Bouselly and El Sokkary . The anomolous gr a-

nite field is considered to include those granites which have either

formed by or been subjected to metasomatism, have undergone chemical

changes or were not formed by a simple mechanism. An impoverishment of

rubidium is considered to be related to metamorphic or metasomatic pro-(39)cesses , however the LDB batholith rocks do not show low rubidium

content.

Comparison of the LDB granite with the standard values of El(39)Bouseily and El Sokkary , as shown in Table 5, indicates rubidium,

strontium and barium concentrations between those of normal granites and

granodiorite.

- 26 -

6.3.5 Other Rock Types

Schlieren

Samples 0816IB and 38155C consistently plot separately from

the other main phase samples. On the QTZ:OR:PLAG ternary plot (Figure

16), according to IUGS nomenclature they are termed as tonalité. Their

differentiation index indicates a less differentiated rock. Comparison

of these two samples with average Lac du Bonnet granite (Table 6) indi-

cates that the elemental abundance of most major elements is similar;

however the CaO content is greater and K_O content is definitely less in

the two samples compared to the LDB granite.

From field notes, 08164B is described as schlieren and 38155C

has the appearance of typical granite. These rocks can represent either

an earlier phase not totally reassimilated into the melt or an inclusion

from earlier rocks Into which magma Intruded. Comparison of the

Na-O.-ICOrCaO ternary plot, seen in Figure 20, with those by Nockolds and

Allen indicates that none of the differentiation trends which they

present are comparable to that joining the pegmatites, main phase and

schlieren samples of the Lac du Bonnet rocks. Samples 08164B and 38155C

probably represent country rock which was intruded by Lac du Bonnet

magma. Sample 38155C has probably been more assimilated and for that

reason was not recognized as schlieren. The original composition of the

samples cannot be determined because of the wide variation in abundances

between the samples, as seen in Table 6, and their probable contamina-

tion by the intruded magma.

Pegmatites

Two samples of pegmatites were collected from the southern

edge of the batholith. The observed field relationships between the

pegmatites and granite suggest that they formed from the same magma.

- 27 -

Extreme potassium and rubidium enrichment and a drop in barium

concentration, all indicators of progressive fractionation, are observed

in the pegmatite samples {Table 6). The pegmatites, therefore, represent

an end-product of crystal fractionation and were not formed by remelting

of rock material. The lack of metamorphism in the batholith and the

fact that some of the pegmatites appear to fill an early fracture set

(see section 5.2) support this conclusion.

Hypabyssal Phase

Sample 35157C was from an outcrop referred to by McRitchie as

a hypabyssal phase (see Figure 5) because of its similar rock properties

and close association to the Lac du Bonnet batholith . The chemical

composition of sample 35157C compared with average plutonic values indi-

cates the hypabyssal phase is a more differentiated rock, although sev-

eral samples of the LDB granite, listed in Appendix A, are chemically

quite similar to sample 35157C. No definite conclusions can be drawn on

the basis of a single sample.

7. CONCLUSIONS

The following conclusions concerning the geology and geochem-

istry of the Lac du Sonnet batholith have been reached:

1. The pluton is a pink, medium- to coarse-grained, equigranular-

to-slightly-porphyritic granite to granodiorite rock showing

a mild concentration of microcline phenocrysts In the centre

of the batholith.

2. The edges of the batholith show a distinct foliation and

banding with numerous inclusions.

- 28 -

3. Field mapping led to significant redrawing of the southern

contact.

i. The central portion of the batholith appears to be predomi-

nantly a single phase; two minor phases were observed.

5. Microscopic deformatlonal ieatures of the batholith show it to

have undergone the least amount of deformation in the region,

confirming earlier hypotheses of its late emplacement.

6. The slight foliation in the batholith is of primary origin

while the foliation in the country rocks is of secondary

origin.

7. Foliations near the batholith boundaries indicate that the

pluton probably has vertical to slightly outward dipping con-

tacts.

8. Two main sets of fractures, a NF.-SW. set and a NW.-SE. set,

were found to exist in the batholith.

9. The orientations of the fracture sets in the batholith appear

to be caused by regional forces and not related to the intru-

sion or cooling of the batholith.

10. The NE.-SW. set of fractures, containing pegmatite veins, was

considered to be the earliest set of joints to develop in the

pluton.

11. Long linear joints were observed to be the combination of sev-

eral smaller component fractures.

12. Lineaments, observed on aerial photographs of the batholith,

may be the result of weathering of closely spaced joint sets.

- 29 -

13. The main phase exhibits a uniform composition and no elemental

nor mineralogical trends were observed.

14. The pluton shows characteristics of having been emplaced rela-

tively near the surface flO km).

15. The geochemical data is Inconclusive, but favors the hypothe-

sis that the probable source ct the parental magma is from a

partial melt of earlier crustal material.

8. ACKNOWLEDGEMENTS

We are indebted to many people who, during the course of this

study, provided valuable assistance and discussion concerning geological

methods, regional geology and interpretation of our observations. Spe-

cial thanks are extended to W.C. Brisbin, P. Cerny, M.E. Durocher and

C.W. Bird. D. Beauchamp and G. Thorne assisted in computing and D.R.

Greig assiôted with calculations and drafting of figures. He thank K.

Ramlal and P. Cerny of the Department of Earth Sciences, University of

Manitoba and A. Wikjord, N. Pearson and the Analytical Science Branch of

WNRE for providing the geochemical analyses. C. Kamineni of the Earth

Physics Branch, Energy, Mines and Resources, Ottawa kindly performed a

number of pétrographie analyses.

- 30 -

REFERENCES

1. J. Boulton (éd.), "Management of Radioactive Fuel Wastes: TheCanadian Disposal Program", Atomic Energy of Canada LimitedReport, AECL-6314 (1978).

2. H.Y. Tammemagi, "Geological Disposai of Radioactive Wastes -The Canadian Development Program", Atomic Energy of CanadaLimited Report, AECL-5392 (1976).

3. S.R. Hatcher, S.A. Mayman and M. Tomlinson, "Development ofDeep Underground Disposal for Canadian Nuclear Fuel Wastes",in proceedings: International Symposium on the UndergroundDisposal of Radioactive Wastes, Otanieml, July 2-6, 1979.

4. H.Y. Tammemagi, "Developing the Data for Nuclear Waste Dispo-sal - Investigations of the Lac du Bonnet Batholith", Geosci-ence Canada, in press.

5. W.D. McRitchie, "Petrology and Environment of the Acidic PlutonicRocks of the Wanipigow-Winnipeg Rivers Region, South-EasternManitoba", in Manitoba Mines Branch Publication 71-1. 57 (1971).

6. A.P. Penner and G.S. Clark, "Rb-Si Age Determinations from theBird River Area, Southeastern Manitoba", Geolog. Assoc. Canada,Special Paper £, 105 (1971).

7. P. Cerny and D.L. Trueman, "Distribution and Petrogenesis ofLithium Pegmatites in the Western Superior Province of theCanadian Shield", Energy, in press.

8. H.D.B. Wilson, "The Superior Province in the Precambrian ofManitoba", Geolog. Assoc. of Canada, Special Paper ±, 41 (1971).

9. B.W. Harris, "Significance of Garnet and Cordierite from theSioux Lookout Region of the English River Gneiss Belt, North-ern Ontario", Contrib. Mineral. Petrol. 5tf, 91 (1976).

10. R.B. Farquharson, "Revised Rb-Sr Age of the Lac du Bonnet QuartzMonzonite, Southeastern Manitoba", Can. J. Earth Sci. 1£, 115(1975).

11. P. Cerny and A.C. Turnock, "Pegmitites of Southeastern Mani-toba", Geolog. Assoc. Canada, Special Paper 9_, 119 (1971).

12. G.P. Beakhouse, "A Subdivision of the Western English RiverSubprovince", Can. J. Earth Sci. 14, 1481 (1977).

13- P. Chagarlamundi, "Resistivity and Seismic Refraction Surveysover Pleistocene Deposits in Southern Manitoba", M.Sc. Thesis,University of Manitoba, 1971.

14. P. Cerny, D.L. Trueman, D.V. Ziehlke, B.E. Goad and B.J. Paul,"Pegmatite Mineral Evaluation Project, 1975-1979", in preparation.

15. P.A. Brown and R. Thivierge, "Pluton Categorization", AtomicEnergy of Canada Limited Technical Record, TR-36, in preparation.

16. P.W. Jeran and J.R. Mashey, "A Computer Program for the Ster-eographic Analysis of Coal Fractures and Cleats", U.S. Bureauof Mines, Inf. Circ. 8454 (1970).

17. R. Balk, "Structural Behaviour of Igneous Rocks", Geol. Soc.An>., Man. 5 (1937).

18. D.U. Ziehlke, "Aulneau Batholith Project", Progress Report,Centre for Precambrian Studies, Part 2, 6 (1975).

19. A.W. Kleeman, "The Origin of Granitic Magmas", Jour. Geol.Soc. Aust. 1£, 35 (1965).

20. Geological Survey of Canada, "High Resolution Aeromagnetic To-tal Field and Vertical Gradient Survey", Open File report, 1979.

21. U.C. Brisbin, "A Gravity Profile across the Lac du Bonnet Bath-olith in Southeastern Manitoba", Atonic Energy of Canada Lim-ited, Technical Record, TR-17, in preparation.

22. W.H. Moorhouse, "The Study of Rocks in Thin Section", Harperand Row, New York, 1959.

23. G.E. Grisak, J.A. Cherry, J.A. Vanbof and J.P. Blumele, "Hy-drogeologic and Hydrochemical Properties of Fractured Till inthe Interior Plains Region", Royal. Soc. Canada Special Paper12 (1976).

24. S.R. Taylor, "Applications of Trace Element Data to Problemsin Petrology", Physics and Chemistry of the Earth 6_, 133 (1965).

25. G.R. Ewers and P.A. Scott, "Geochemistry of the Cullen Gran-ite, Northern Territory", BMR Journal of Australian Geologyand Geophysics 2_, 165 (1977).

26. "Analysis ?i Surface Outcrop Rocks in the Lac du Bonnet Batho-lith, Field Samples 1977", Atomic Energy of Canada LimitedTechnical Record, TR-23 (1979).

27. "Analysis of Surface Outcrop Rocks in the Lac du Bonnet Batho-lith, Field Samples 1978", Atomic Energy of Canada. Limited,Technical Record, TR-22 (1979).

- 32 -

28. T.F.W. Barth, Theoretical Petrology, 2nd ed. John Wiley andSons, New York, 1962.

29. C.S. Hutchinson, Laboratory Handbook of Pétrographie Techniques,John Wiley and Sons, New York, 1971.

30. S.R. Taylor, Geochemistry of Andésites, Origin and Distributionof Elements. Symposium held in 1967, published 1968, p. 559.

31. C.P. Thorton and O.F. Tuttle, "Chemistry of Igneous Rocks I.Differentiation Index", Am. J. Sci. Zb%, 664 (1960).

32. R.B. Farquharson, "Radioélément Content and Variation in someGranodiorites of Southeastern Manitoba and Adjacent Ontario",Can. J. Earth Sci. K3, 993 (1976).

33. D.M. Shaw, "Uranium, Thorium and Potassium in the CanadianPrecambrian Shield and Possible Mantle Compositions", Ceochim.Cosmochim. Acta 31» 1111 (1967).

34. P. Kolbe and S.R. Taylor, "Major and Trace Element Relation-ships in Granodiorites and Granites from Australia and SouthAfrica", Contrib. Mineral. Petrol. 12_, 2 0 2 (1966).

35. O.F. Tuttle and N.L. Bowen, "Origin of Granite in the Light ofExperimental Studies in the System NaAlSi,OH-KAlSi.Oa-SiO?-H,O",Ceol. Soc. Am. Mem. ]±, 1 (1958). J

36. J.B. Wright, "A Simple Alkalinity Ratio and Its Application toQuestions of Non-Orogenic Granite Gneiss", Geological Magazine106, 370 (1969).

37. H.C. Teng and D.F. Strong, "Geology and Geochemistry of the St.Lawrence Peralkaline Granite and Associated Fluorite Deposits,Southeast Newfoundland", Can. J. Earth Sci. 13_, 1374 (1976).

38. B.W. Chappell and A.J.R. White, "Two Contrasting Granite Types",Pacific Geology ji, 173 (1974).

39. A.M. El Bouseily and A.A. El Sokkary, "Relation Between Rubidium,Barium and Strontium in Granitic Rocks", Chem. Geol. 16, 207(1975). ~

40. S.R. Nockolds and R. Allen, "The Geochemistry of Some IgneousRock Series", Geochim. Cosmochim. Acta k_, 105 (1953).

41. J.A. Cherry, G.E. Grisak and W.E. Clister, "HydrogeologicStudies at a Subsurface Radioactive Waste Management Site inWest-Central Canada", Underground Waste Management and Arti-ficial Recharge, Vol. 1, 1973, pp. 436-467.

- 33 -

TABLE 1

DATA RECORDED AT EACH SITE (OUTCROP)

A. General Description

1. location of outcrop2. size of outcrop3. type of rock and its homogeneity4. grain size5. mineral components and their percentage6. dikes7. inclusions8. main fracture sets9. horizontal sheeting

B. Sample

A representative sample of approximately 1 kg taken and labelled.

C. Fracture Analysis

1. measuring tape placed and bearing recorded.

2. rock type, dikes, inclusions recorded.3. fractures recorded:

a. location on tapeb. stride and dip (where possible)c. attitude, i.e., linear, irregular or curvedd. compound or singlee. lengthf. open or tightg. vegetation

It. repeated with tape perpendicular to original bearing.

- 34 -

TABLE 2

OLD PINAWA - FRACTURE PARAMETERS AT 2 LOCATIONS

Site A

Joint

Set

Set

Set

Sets

1

2

3

Azimuth

031°

135°

166°

Spacing(Metres)

4.7

7.0

5.5

Frequency(Fracturesper Metre)

0.21

0.14

0.18

FractureLength*(Metres)

18.4

24.6

15.2

ComponentLength(Metres)

8.3

10.3

6.69

Site B

Set

Set

Set

1

2

3

033°

-

-

22.

-

-

9 0.

-

-

04 14.0

-

-

4.2 3.0

-

-

2.5

* includes all fractures.

- 35 -

TABLE 3

CHEMICAL ANALYSIS METHODS

Element Laboratory Method

FeO

TiO,

MgO

CaO

MnO

Trace

Ba

Sr

Zr

P

C

Sn

Cs

Rb

Y

Li

Th

Be

Ga

Hf

Pb

U

University of Manitoba

University of Manitoba

University of Manitoba

University of Manitoba

University of Manitoba

University of Manitoba

University of Manitoba

University of Manitoba

University of Manitoba

University of Manitoba

Bondar-Clegg & Co.

University of Manitoba

Bondar-Clegg & Co.

University of Manitoba

University of Manitoba

Bondar-Clegg & Co.

University of Manitoba

University of Manitoba

W?T"S

Bondar-Clegg & Co.

University of Manitoba

Bondar-Clegg & Co.

University of Manitoba

Bondar-Clegg & Co.

WNRE

University of Manitoba

Bondar-Clegg & Co.

X-Ray Fluorescence Spectrometry (XRF)

XRF

Tota

Fe 0, by calculation

XRF

If high by XRF; if low by AA

XRF

Atomic Absorption Spectrophotometry (AA)

XRF

XRF

XRF

Flame Emission Spectrophotometry (FE)

XRF

Coloriraetry

Combustion/Gravimetry

XRF

Flameless hi*:=sion Spectrophotometry (FLE)

FE

Optical Emission Spectrography (OES)

XRF

FE

XRF

FE

XRF

OES

FLE

XRF

- 36 -

TABLE 4

AVERAGE ROCK ANALYSES

MajorElements

sio2

A12O3

Fe2°3FeO

TiO2

MgO

CaO

Na2O

K2O

MnO

TraceElements

Cs

Rb

Tl

Ba

Sr

Y

Th

U

Zr

Hf

Li

Bet>

C

Sn

Ga

Pb

Lac

%

72.83

14.53

0.92

0.66

0.20

0.42

1.17

3.59

4.83

0.03

PS/B

9.6

185

1.7

750

194

5.6

25

9

201

3.8

37

1.7

301

329

6.7

29

20

du Bonnet

Range

76.9-68.1

16.5-12.6

1.40-0.45

1.60-0.22

0.27-0.04

0.71-0.11

1.81-0.57

4.55-2.98

5.84-3.78

0.09-0.012

13.3-0.2

327-85

< 1.0-2.4

1718-391

782-28

14-1

36-5

26-1

300-118

7-1.5

110-17

2.9-0.8

742-2

710-115

13-2

34-23

27-11

Standard

Granite<30)

71.20

14.70

1.28

1.80

0.40

0.55

2.00

3.54

4.18

0.05

5

145

1.0

600

285

40

17

4.8

180

4

30

5

700

-

3

20

30

Standard

Granodiorite^30^

66.90

15.70

1.06

2.59

0.57

1.57

3.56

3.84

3.07

0.06

4

110

0.9

500

440

30

10

2.7

140

3

25

-

920

-

2

18

15

* Major elements based on 29 representative samples, trace elements often

on less than 29

- 37 -

TABLE 5

Rb:Ba:Sr RELATIONSHIPS

Granodiorite

Normal Granite

Strongly DifferentiatedGranites

AnomolouE Granites

Lac du Bonnet Granite

1

Kb

140

190

260

210

185

Ba(fg/g)

1170

550

140

1030

750

Sr

810

70

20

280

194

Rb/•

7

23

62

14

16

: BaX

55

69

33

66

66

: Sr

38

8

5

18

17

- 38 -

TABLE 6

CHEMICAL COMPOSITION OF OTHER ROCK TYPES

Element

Sample

(Z)sio2

A12O3

Fe2°3FeO

TiO2

MgO

CaO

Na2O

K2O

MnO2

(Wg/g)

BaSrZrCsRbTlyLiThUBeHfPCSnGaPb

D.I.

Pegmatites

04734B

72

14

0

0

0

0

0

2

9

0

4165692.

491

1475400.-

8738292424

97.

.8

.8

.25

.10

.06

.10

.20

.30

29

02

7

8

8

10106A

73.1

14.2

0.22

0.12

0.08

0.07

0.04

0.75

11.08

0.01

28939-8.3

6491.8-

22-50.51.5

1313927176

98.4

Schiieren

08164B

68.3

15.10

1.5

2.32

0.42

1.84

2.84

4.85

1.66

0.09

942081344.2

1792.121148625.04.0

87332810385

74.0

38155C

72.3

15.0

0.68

0.54

0.21

0.52

2.77

5.78

1.14

0.02

_286

-2.9441.7-

23--2.3-

480491

--6

84.3

Hypabyssal

35157C

75.3

13.2

0.76

0.42

0.14

0.20

0.87

3.55

4.88

0.02

3891151241.2

2242.22312232.13.0

131328123113

93.4

Average

Granite

72

14

0

0

0

0

1

3

4

0

7501942019.

1851.5.372591.3.

3013296.2920

89.

.8

.5

.92

.66

.20

.42

.17

.59

.83

03

6

76

78

7

7

FIGURE 1: The Location of the Lac du Bonnet Batholithin Southeastern Manitoba

IONTARIO-MANITOBABORDER

I

Red LakeSubprovince

Ear FallsManigotoganGneiss Belt

THE LACDUBATHOLITH

j£§§ metosedirnentary gneiss'=Ip early gnetssic suiteJs52 trondh'jemite - granodlorlte suite^ 1 granodiorite - granite suit*WZ mefavolcanic rocksililii metasedimentary rocks

FIGURE 2: The Lac du Bonnet Batholith and i t s Regional Geolcgy.After Beakhouse (12), McRitchie (5) and Wilson (8).

600 900 METRES EAST

tà5n

LACUSTRINE SILTY UNIT

LACUSTRINE CLAY UNIT

CLAY-LOAM TILL UNIT

BASAL SANDY DRIFT UNIT

LACUSTRINE SAND AND GRAVEL UNIT

PRECAMBRIAN BEDROCK

FIGURE 3: Stratigraphy of the Surficial Deposits along a Profile Nearthe Waste Management Site, WNRE (from Reference 41)

5 (0 Km

FIGURE 4: Sites Where Samples Were Obtained and Fracture Measurements Recorded. Chemical AnalysesWere Done on Samples from Sites Whose Numbers are Underlined.

f Contacts : de f i nod,—.,SN, undefined

* « • > . « noundary of strongfoliation

fOkm

FIGURE 5: Geological Map of the Lac du Bonnet Batholith

QUARTZ

• TYPICAL GRAHITE

© INCLUSIONS AND COUNTRY ROCK

FIGURE 6: Modal Analysis, IUGS Classification

Déformée1.

Moderately Deformed

Minor Deformation

10 km

Deformation Group Boundaries• Sites where thin sections were taken

FIGURE 7: The Lac du Bonnet Batholith Showing Degree of Deformation

0 5 10 ttmFOT.T.Vïnv - d i p unl.rov-

V r t i c . i l .i ncl i ne1'?

FIGURE 8: Foliation of the Lac du Bonnet Batholith and Surrounding Region

180 r

170 -

160 -

150

140

130

120

110

100

90

60

70

60

50

40

30

20

10

! 1

•"•"^••— Knovn lonqths

Unknown lengths(represents .1 =Inimra length)

i

IIII , r-

i10 15 20 30 35 40 45

:.12CRTH .'F FRACTURES (mrtri'3)

FIGURE 9 : Length of Fractures in the Lac du Bonnet Batholith

- 48 -

peçmatites

a) Fractures and pegmatite dikesin La-: du Bonnet hatholith

b) Fractures in countrv rock

020

c) Fractures and pegmatitesat Old Pinawa Dam Site

d) Lineaments in Lac du Bonnetbatholith

FIGURE 10: Rose Diagrams of Fractures, Pegmatite Dikes and Lineaments

AC = F r a c t u r eAB = Component of

f r a c t u r e AC

FIGURE 11: Showing TVo Fracture Sets and How a Linear Fracture is Composed of Components.

o

7

6s

« 5jtu

o 4

3 3

2

1

n

i

-

1

—

1

— Known lengths

-"""• Unknown lengths

1

1

1J1

10 15 20 25 30LENGTH OF FRACTURES (metres)

35 40

FIGURE 12: A Frequency Histogram of Fracture Lengths Measured at the Old PinawaDam Site.

- 51 -

I km

FIGURE 13: Aerial Photograph of Lineaments in Area LDB-1.(See FIGURE 8 for Location of LDB-1)

1.5H

Hood L.

a Viola L.

> Maple Cr. . ' *

,F

orthbrook / ' ^

St . Ignace • , » M a n i t o W a b l n E , ' 'Ht. S t . Patr ick , " » ' Tlchborne-Buck Bay

Badgerew

LPB 2 ffSy '-<=ggat i..

• Spawn tnlct'

** Vhitostone

.' «Entwine L. -̂***

T\'R1 op-Shakespeare

. ' C o s b y . , -' II.DB 1

Eagle L.

** Knbcnunp L.

Drybcrrv Done

Skoot3n.it ta

4 S 6

FRACTURE DENSITY ( n i . ' s q . n i . )

—I10

FIGURE 14: LDB-1 and LDB-2 Plotted on a Practure Density - Major Lineament DensityPlot of Brown and US)

- 53 -

90 80 70 60 SO 40 30 20DIFFERENTIATION INDEX

10

90 80 TO 60 50 40 30 20DIFFERENTIATION INDEX

10

JOO 90 BO 70 60 50 40 30 20 10 0DIFFERENTIATION INDEX

• Standard GraniteD Standard GranodioriteO Lac du Bonnet Granite

FIGURE 15a: Elemental Abundances Plotted Against Differentiat ionIndex, (from Reirrence 31).

80 60 40 20DIFFERENTIATION INDEX

60 60 40 20DIFFERENTIATION INDEX

A Standard GraniteO Standard GranodioriteO Lac du Bonnet Granite

600

400

200

CS

90 80 70DIFFERENTIATION INDEX

2.0

6»

O -« Rb

\ .T l

90 80 70DIFFERENTIATION INDEX

90 80 70DIFFERENTIATION INDEX

FIGURE 15b: Elemental Abundances Plotted Against DifferentiationIndex, (from Reference 31).

QUARTZ

BO/t

ALKALI-ÎXUÎSPAPGRANITE

ALKALI-FELDSPAR/-QUARTZSYENITE/

» '. • \cRANODIORITf. \

TONALITE

—A so

QUARTZSYENITE

OfARTzHONZON'ITE

OUARTZ 'Ct 'ARTZ:tioNzonroRrri: DIORITE

ORTIIOCLASr. 60OCLAr.E

FISURE 16: QTZ:PIAG:OR Mesotvom Plot with IUGS Igneous Rock Classification

- 56 -

(3U

- 57 -

70

Z 60

o

50

40

PERALKALINE

2 3 4 5 6 7 8 9 10 12

ALKALINITY RATIO

FIGURE 18: Alkalinity Ratio (from Reference 36)

- 58 -

100 80 60 40 20DIFFERENTIATION INDEX

Ml,II

FIGURE 19: Silica-Differentiation Index Diagram,(from Reference 31)

Solid and dashed linesrepresent differentiationtrends of the SouthernCalifornia batholith andScottish CaledonianrocksdO)

20

FIGURE 20: Na 0:K 0:Ca0 Ternary Plot

FIGURE 21: Sr:Ba:Rb: Ternary Plot from Reference 39

- 61 -

APPENDIX A

GEOCHEMfCAL RESULTS

The following notations are used in this section:

na = not analyzed

0.0 = analyzed, but below detection limits

- 62 -

FIELD DESCRIPTION OF SAMPLES

Sample

No.

O1131B

0210'iB

022O7B

042.»3B

04633B

P7159B

14130A

15134C

16135C

17136C

18136C

19113A

20245C

21119A

22124A

23132A

24133A

25136A

26139A

29147A

33153A

39158C

401D

Rock

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

Lac

du

du

du

du

du

du

du

du

du

du

du

du

du

du

du

du

du

du

du

du

du

du

du

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

Bonnet

granite

granite

granite

granite

granite

granite

granite

granite

granite

granite

granite

granite

granite

granite

granite

granite

granite

granite

granite

granite

granite

granite

granite

Sample

No.

4 <ilD

461D

511D

521D

561D

581D

04534B

04734B

06158B

O7259B

08164B

10106A

35157A

38155C

151D

341D

371D

531D

61AD

0P87D

OP331D

OP132D

Rock

Lac du Bonnet granite

Lac du Bonnet granite

Lac du Bonnet granite

Lac du Bonnet granite

Lac du Bonnet granite

Lac du Bonnet granite

amphibolite

pegmatite

Marijane Lake pluton granite

darker granite

schlieren

pegmatite

hypabyssal phase

granite (schlleren)

quartz diorite phase

pegmatite?

hypabyssal phase

quartz diorite zenolith

pegmatite

quartz diorite gneiss

banded gneiss

banded gneiss

- 63 -

STANDARD GRANITE

ElementorOxide

wt.ZElementorOxide

wt.X

sio2

A12°3Fe2O3

FeO

MgO

CaO

K2°MnO

BaSrZrPCSnCsRbTlYLiThUBeGaHfPb

72.83

14.53

0.92

0.66

0.20

0.42

1.17

3.59

4.83

0.03

TOTAL

750194201301328

69

184.1.5.

36.25.

9.1.

29.3.

20.

99.

.0

.0

.0

. t

. 6

. 7

.6

.7

.7

.6

.8

.0

.07

.080

42

QuartzCorunduraZ ire oilOrth.idnseAlbiteAnorthositeNephelineHaliteMagnetiteHematiteApatiteCalciteCassiteriteOlivineBiotitt?KdeniteSphene

TOTAL

D.I.Ab:An

29.562.120.02

27.5432.604.090.000.000.940.020.150.310.000.002.170.000.43

99.96

89.7189:11

- 64 -

Elemen

Oxide

Al-»°j

I'eO

TJO,

HBO

CttO

"•2°

MnO

tin

5r

2 r

P

C

Sn

Cs

Kb

TJ

Y

U

u

C«

l l f

l*b

TOTA1

QtE

Cor

Z i r

Orth

Ab

Neph

H a l

Ma 8

Hen

ApaC

Calc

Case

Oliv

Eden

Sph

TOIAL

D.r.

Ab:An

06613

1L.0

1 Ï.9

0, 71.

0,0b

O.?!>

: . < • ! >

3.26

0.03

no

joe.o

no

266.0

156.0

•IB

O.t

327.0

0 . 0

na

27.0

„.ua

0 . 0

23.0

99.70

28.86

0.1?

0.00

32.66

29.59

0.00

0.00

0.6b

0.11

0.12

0.15

0.00

0.00

0.00

0.08

99.93

91.33

82:18

01131

72. i

14.7

J .O

O.ft

0 . 7

CJ.l

1. )

Ï . 6

0 . 0

7 ?6.0

200.0

210.0

262.0

519.0

9 . 0

i . 6

?19.O

0 . 0

16.0

16.0

3J.00 . 0

2?.O

99.65

29.07

2.18

0.03

25.98

33.07

0.00

0.00

1.07

0.00

0.13

0.49

0.00

O.OO

0.00

0.51

99.91

88,12

88:12

O21O8P

7;'. vo

K.JO

0. ÏB

0.80

O.J1)

a, en

i.to

O.OJ

860. &

208.0

198.0

306.0

519.0

2 . 0

1.6

20?.0

1.1

9 . 0

J1.0

9 . 0

0 . 0

98.98

31.07

2.10

0.02

27.18

3 J.OB

0.00

0.00

0.83

0.00

0.25

0.49

0.00

0.00

0.00

0.49

99.93

89. 3 i

89:11

SfiKPLf

0220U

Ml .

Ti.m

li.W

O.fci

o.wy

0. Ï4

!).(.«

1.1V

3. !i«

o .n ;

79t.. 0

223.0

2JÎ.0

JiV.O

409.0

b.O

3.0

18b. 0

0 . 0

H . O

3Ï.U

7 ,0

J1.0

i . t

99. ÎÎ.

wt . t

30.7 3

2.5t

0.03

25.33

32.56

0.00

0.00

0.90

0.00

0.17

0.38

0.00

0.00

0.00

0.51

99.95

86.63

69:11

KUKBOt

• 42Ï3

/5,0

! 3 »

0,<i

o . i

0 . 1

0 . 2

0. 7

Î . 1

0 . 0

115.0

:,a

.'62.0

ÏB2.0

t\a

1.6

ïbZ.O

i.:

no

C O

tia

tia

0 . 0

99.3(>

3t.7&

2.85

0.00

28.95

28.56

0.00

0-00

0.67

0.00

0.13

0.36

0.1*0

0.00

0.00

0.30

99.92

92.27

94:6

HH59

72.70

14.80

U.V4

U.'lï

0.21

7.ÎH

l.OB

J . t

0.0]

6J6.0

219.0

185.0

Î0&.0

218.0

6 . 0

J3.Ï

Ï65.O

1.2

1.0

110.U

17.0

M>.0

1.5

99.72

28.19

2.06

0.02

31.17

31.05

0.0D

0.00

0.99

0.00

0.J5

0.20

O.OO

0.00

0.00

0.44

99.89

90.41

89:11

U110A

74.60

1 J.VD

0.M1

o, j ;

O . K

0.20

0.57

;.9B

0.02

na

120.0

na

J31.0

164.0

na

1.6

24i.O

2 . 0

« a

}«.O

l i a

ua

0 . 0

9V.55

31.99

2.23

0.00

3d. 40

27.15

0.00

0.00

0.8O

0.04

0.06

0.15

0.00

0.00

0.00

0.30

99.94

93.55

94:6

IMiiC

Ti.HQ

K.20

o.;<i

0.17

0. Î0

0.9ti

J.V8

0.03

ti.6.0

43.0

156.0

218.O

246.0

7.0

J.O

2ZH.0

0 . 0

i.O

ÏV.0

2V.0

15.0

31.0

6 . 0

99.57

29.91

1.72

0.02

25.31

36.04

0.00

0.00

0.6 i .

0.00

O.JJ

0.23

0,00

0.00

0.00

0.36

99.93

91.26

91:9

161JSC

*?. 70

K.S0

0. fb

0. ?(,

0.17

0.40

1.01

Î .65

O.0Î

675.0

150.0

217.0

J93.D

246.0

i . O

2.b

.•21.. 0

1.6

9 . 0

49.0

24.0

•ib.O

31.0

6 . 0

99.27

28.73

1.99

0.03

28.51

33.18

0.00

0.00

0.60

O.OO

0.19

0.23

0.00

0.00

0.00

0.36

99.93

90.41

90:10

- 65 -

Ueacni

SlOj,

A1,O,

rM

no.MKO

MnO

Bû

5r

Zr

P

C

Cs

Kb

T ;

y

LI

I'll

U

tie

Git

If*

Pb

TOTAl

Qti

Cor

Z i r

Orrh

Ab

An

Neph

HaJ

" • K

Hen

Apit

Calc

(Use

01 l v

Blot

Eden

Sph

TOTAl

D.I.

'

74.21

14.2t

0 . 6

O.B

0.1

0. 1

3.6

4 . 1

0 . 0

606.0

150.0

9 . 0

1 . '

m.oi.i

55.0

20.0

]!,0

I . »

21.0

2.0

19.0

99.65

2.79

0.02

23.1»

32.92

3.36

0.00

0.00

0.12

0.00

0.13

0.66

0.00

0.00

2.42

0.00

0.54

99.92

89.49

73.9

14.0

' .3

0.1»

0 . 2

0.3

) . "

4 . 7

0 . 0

716.0

203.0

196.0

5 .0

1.1

146.0

i.a

19.0

20.0

0 . 0

1.5

24.0

2 . 0

15.0

99.56

32.S3

2.72

0.02

27.27

30.96

2.39

0.00

0.00

1.37

0.04

0.11

0.41

0.00

0.00

1.42

0.00

0.44

99.97

91.06

69.70

1 1 . UO

1. u

1.60

0.46

0. 71

3.83

1.80

0.09

no

173.0

n»

na

5 .6

316.0

I.»

77.0

1U,

U d

3.1

» B

6 . 0

11.0

«9.22

25.24

2.19

0.00

25.62

14.80

4.19

0.00

0.00

1.42

0.00

0.36

0.1(1

0.00

0.00

4.92

O.OO

0.97

99.89

85.66

SAMPLE

VI •

70. eo

15.20

1.3U

o.m

o . »

g.6)

J.7O

5.1»

0.02

758.0

235.0

257.0

t . O

1.5

125.0

2.3

25.0

10.0

0 . 0

l . l

27.0

7.0

14.0

99.70

25.20

1.78

0.03

28.92

33.43

j .17

0.00

0.00

1.37

0.00

0.19

0.37

0.00

f '0

2.£9

0.00

0.50

99.95

87.55

11. W

I t .400.07

0.VO

O./J

O.',B

3.70

5-10

O.Oi

635.0

149.0

IL2.1.

13.0

2 . 3

2SC.0

S2.0

IV.U

6 . 0

1.4

» . O

4 . 0

l ft.0

99.51

1.46

0.03

26.36

33.55

3.23

O.OO

O.CO

0.92

0.00

O.\9

0.31

0.00

0.00

3.30

0.00

0.57

99.93

89.93

71.6

K.ti

1.0

0 . 8

U.2

Q.b

3.8

b.5

0 . 0

666.0

170.0

2U.0

b.O

J .6

i6.0

26.0

ÏU.0

r.o1.5

ÎV.0

1.0

11.0

99.3?

3.6?

0.03

25.52

34.96

5.27

O.OD

0.00

1.12

0.00

0.15

0.26

0.00

0.00

2.56

0.00

0.57

99.95

SB.IB

7t.7O

13.HU

o.eo

0.54

0.1*

0. 3<<

3.68

4.62

0.02

685.0

183.0

181.0

6 . 0

2 . 5

116.0

2Ï.0

S4.U

i .o

1.0

27.0

2 . 0

11.0

9 9 . «

1.36

0.02

27.77

33.44

3.60

0.00

0.00

0.85

0.00

0.06

0.20

0.00

0.00

1.69

0.00

0.34

99.97

91.85

71.50

U.OO

0.96

0.60

0.20

0.40

3.6B

4.80

0.03

t u

163.0

" *

os

1.1

256.0

2.1

3«"o

tta

na

2 . 1

I I S

7 .0

19.0

»9.2Z

30.42

1.93

0.00

27.56

13.51

2.80

0.00

0.00

1.02

0.00

0.13

0.23

0.00

O.OO

1.91

O.OO

0.42

99.93

91.50

69.40

15.30

1.40

1.04

0.30

o . n

4.55

3.78

0.02

772.0

230.0

202.0

6 . 0

2 . 1

85.0

1.7

12.0

24.0

12.0

1.0

1.7

28.0

3.5

13.0

98.69

2Î.65

l . M

O.OZ

20.24

41.3Î

7.01

0.00

0.00

1.48

0.00

0.21

0.28

0.00

0.00

3.77

0.00

0.63

99.95

85.22

- 66 -

El erne

S .o ,

FeO

H 80

CaO

KnO

Ba

Sr

P

C

Sn

Cs

Kb

T l

M

n i

u

Ga

tir

Pb

TOTA1

Qtz

Cor

21 r

Ortn

Ab

An

Neph

H a l

Mag

Hen

Apat

Cale

Cass

01 l v

Blot

Eden

Sph

TOTAI

D.I.

Ab:An

72.4

0 . 8

0 .6

1.1

3.5

0 . 0

879.0

215.0

175.0

218.0

6 . 0

1.9

206.0

1.6

35.0

36.0

7.0

29.0

2 . 0

23.0

99.25

2B.50

1.60

0.03

28.30

32.32

4.61

0.00

0.00

0.86

0.00

O.09

0.20

0.00

0.00

2.94

0.00

0.51

99.96

69.12

88:12

73.9

0. 2

0 . 2

O.V

3.1

0 . 0

616.0

169.0

476.0

519.0

13.0

0 .6

117.0

na

J7.U

60,0

o.>

21.0

l u

19.0

99.92

31.19

3.06

0.02

31.90

28.49

2. SO

0.00

0.00

0.54

0.16

0.23

0.48

0.00

0.00

1.04

0.00

0.36

99.97

91.58

92:8

, , ,

U.6

0. 1

1.6

3.6

0 . 0

na

199.0

109.0

273.0

0 . 6

208.0

na

;fv.o

l i a

na

IU1

na

25.0

99.45

28.32

1.37

O.OO

28.45

33.12

5.89

O.OO

0.00

0.78

0.00

0.05

0.26

0.00

0.00

1.37

0.00

0.30

9.92

9.90

5:15

SAMPLE

VI •

tH. 10

O.titt

0 . 7

1 .«

6 . 0

0 . 0

3716.0

782.0

666.0

437.0

5 . 0

0 .2

105.0

na

.»O.U

i . O

0 . 0

ÏO.O

•ta

12.0

99.1C,

22.29

2.63

0.O6

25.83

36.46

6.82

0.00

0.00

1.66

0.29

0.31

1.41

0.00

0.00

2.71

0.00

0.51

99:97

84.60

84:16

NUMBER

7 3.9C

0 . IE.

U. 36

1. )b

î.bts

0 . 0

na

225.0

166.0

382.0

na

0. 3

113.0

i i -

22.0

i,a

na

l i a

27.0

99.63

31.01

2.03

O.OO

25.45

33.32

5.24

0.00

O.OO

0.65

0.00

0.08

0.36

0.00

0.00

1.52

0.00

0.30

9.96

9.78

6:14

n. 6

0. 7

l.!t

î.J

0 . 0

696.0

225.0

506.0

194.0

2 . 0

0 . 9

154.0

na

Ï9.0

23.0

0 . 0

Ï / .O

22.0

99.72

27.17

2.53

0,03

25.56

36.14

5.79

0.00

0,00

1.04

0.00

0.24

0.18

0.00

O.OO

2.74

0.00

0.50

99.94

86.87

85:15

72.6

0 . 4

0 . 6

O.B

3.0

0 . 0

707.0

169.0

197.0

573.0

9 . 0

0 . 9

180.0

na

4 Ï .0

2U.0

5 . 0

H.U

na

22.0

99.19

30.02

3.25

0.02

33.59

27.31

2.11

0,00

0.00

0.83

0.00

0.19

0.56

0.00

0.00

1.75

0.00

0.34

9.95

0.92

3 :7

72. 7

16.7

O . t

0 .6

1.0

S. 30

5. 3.0.0

no

153.0

Ï93.O

266.0

na

0 .7

176.0

na

22.0

na

na

26.0

99.21

T9.66

2.59

0.00

30.82

30.05

3.26

0.00

0.00

0.96

0.00

0.19

0.23

O.OO

0.00

1.69

0.00

0.51

99.97

90.53

90 • i.O

2O265C

71.10

16.00

0.9b

0.62

0.51

1.5H

6.03

3. B90.03

no

2Î6.0

201.0

392.0

no

2. 3

178.0

na

S2.0

na

ua

na

15.fi

99.13

27.60

3.20

0.00

21 .71

36.96

5.99

0.00

0.00

1.01

0.00

0.10

0.37

0.00

0.00

2.35

0.00

0.66

99.95

86.67

6:14

- 67 -

Flemeut

orOxide

sto2

A l 2 ° 3

' V lJVO

Ti t ) ,

MB0

CaO

Na 0

KO

MnO

Bo

SrZr

r

c

S f i

Ce

Kb

Tl

Y

LI

Th

V

B«

1'Li

TOTAL

Cor

Zlr

Ore h

*b

An

Neph

Hal

ag

en

Apsn

Calc

j s a

l i v

l o t

Eden

p h

TOIAL

- I .

Ah: An

75.20

1 î . VU

0.45

0. JO

0.11

0.71

0.90

3.554 . 1 - ,

0.02

391.0

133.011B.0

35.0

115.0

b.O

1.0

223.0

O S

2 . 0

Ï 4 . Q

21.0

2.0

1.4

i.'.o

25.0

99.43

32.91

1.840.01

27.14

32.30

3.80

0.00

O.OO •

0.48

0.00 ;

0.02

0.11 '

0.00

0.00

1.03

O.OO

0.32

99.95

92.35

39:11

7fc.9D

12.60

0.92

0.00

O.K

0. 11

0. IK

3.25

4. 38

0.0Ï

28.0

tu

2.0

227 0

«a

0.6

127.0

us

its

25.0

iia

( Id

; ' . : >

« »

IV.0

99.58

38-OB;.O3

o.oo

25.84

29-75

1.91

O.OO

o.oc

0.9S

o.oo

o.oo

0.21

0.00

0.00

0.B7

0.0Q

0.3D

99.96

93.66

94:6

47,50

14.00

(..20

¥.04

0 . VO

J. VO

10.40

1 .9»

1.54

0. tZ

54.0

42.0

562.0

43Ï.O

6 . 0

2 . 7

123.0

J. 3

n. ol n . o

0.0

2.0

1.2

20.0

3.0

98.11

O.OO

0.01

0.00

0.00

25.46

A.26

0.00

(. -

o.oo •

0.28

0.42

O.OO

0.56

K.97

35.7 3

2.06

84.27

0.19

0:100

SAW LE

7Î.80

14.«U

0.21

0.10

0.0b

0. 10

0.20

2 . 3 0

V.2V

o.o:

56.0

9.0

B7.0

382,0

9.0

2. 7

491.0

0 . 0

0 . 0

u . o

71.ti

tiU.O

O.li

2 t , 0

00.0»

1.11

o.oo

54.66

20.7 3

0.00

0.00

0.60

0.26

0.00

0.04

0.36

0.00

0.00

0.3»

0.00

0.13

93.95

97.80

100:0

KUKBtK

T SB

7fc. >0

11 . %0

0. 1 Ï

0 .16

0.0',

0.07

CJ.H

J. '

!..<.*

0.01

w.ona

3J.9.0

2Î8.O

na

1.6

15J.0

u.o

t . o

0. )

Toj e . o

VV.5 3

2.17

0.00

26.43

33.87

1.51

0.00

0.00

0.Ï4

0.00

0.17

0.20

0.00

0.00

0.54

0.00

0,11

99.97

95.13

96:4

0

71 , 70

15.00

1 -11

0 . VO

0 .1?

0.04

4.5B

4.10

4.0b

0.04

20S.O

29b. 0

480.0

191.0

2.0

5.6

220 .0

l.K

21.0

1 39.0

42,0

10.U

l.n

».o

20.0

99.69

1.92

O.Oi

22.06

37,00

5.7B

0.0D

0.00

1.17

o.oo

0.23

0.18

0.00

0.00

3.28

y.oo

O.fc7

99.86

86.59

86:14

68. Î

15.1

1.5

2.3

0 . 4

l . t i

2.B

4.H

l . W

0 . 0

2U8.O

114.0

B73.O

328.0

10.0

4 . 2

179.0

2 . 1

21 .0

Uti.O

0 , 0

7.0

5 0

$H.O

5.0

VV.15

1.56

O.Oi

3.35

43.78

10.70

O.OO

o.oa

1.58

0.00

0.42

0.31

0.00

0.00

10.42

0,00

0.H8

99.85

73.97

80:20,

I0106A

?i. JO

14.20

(1.22

0.1?

0.08

0,07

O.Oi.

0. '5

11 .08

O.OI

39.0

O.O

131.0

39.'. 0

1.0

8.3

649.0

l.ti

0.0

32.0

o.u

5.0

0.5

17.0

0.0

99. ë7

1.53

0.00

65.32

6.64

0.00

o.oo

0.00

0.23

0.00

0.06

0.37

0.00

0.00

0.33

0.00

0.17

99.93

98.36

100:0

J51S7A

75. JO

11.20

0. Jt

O.4.'

0.14

0.70

(J.H7

3.55

i . BB

o.o;

115.0

124.0

131 .0

12». 0

12.0

1.2

22*. V

2.2

2 .0

II ,0

ii.o

i .o

2.1

31.0

11.U

99.6B

32.46

1.09

0.02

28.63

32.31

3.03

0.00

0.00

0.81

0.00

0.06

0.31

0.00

o.oo

0.95

0.00

0.30

99.96

93.40

91:9

- 68 -

Element

OxU'e

sio2

TiO,

CaO

N«2O

K2D

MnO

B.

Sr

Zr

¥

C

Sn

Ab

T l

y

L l

Tl i

U

i t )

Ga

IK

Pb

TOTAL

Qte

Cor

Z i r

Orth

Ab

AnNeph

H a l

Mag

Hen

Apat

Calc

Cast

Oliv

Bloc

Eden

Sph

TOTAL

D.I.

Ab;An

38155C

72.30

li.00

0.<JB

0.56

0.21

0.1?

; , 7 ;

5.7B

1 . 1 *

O.OZ

na

286.0

n«

480.0

491.0

n .

44.0

1.7

na

21.0

ua

na

2. 3

na

0 . 0

t>.0

99.09

27.14

0.15

0.00

5.21

51.93

1 1 . ~5

COO

o.eo

0.71

cooC.23

0.46

0.00

0.00

2.64

0.00

0.46

99.98

86.30

82:16

1510

73. 50

14,70

1.04

O.ïb

O.Ï0

0.2fc

1.06

J.fafl

6.7t

0.03

na

166.0

na

140.0

1200.0

na

196.0

M

na

Î7.0

na

im

1.5

n t

na

32.0

99.82

30.72

3.16

O.OO

27.66

33.16

O.OC

0.00

0.91

0.12

0.07

1.12

0.00

0.00

0.96

0.00

O.<2

99.95

91.54

95:5

361!)

71.10

16.60

0.15

0.10

0.11

0.09

0.71

3.157.12

0.01

5BB.0

176.0

105.0

61.0

666.0

0 . 0

256.0

na

0 . 0

8 . 0

6 . 0

17,0

0 . 9

25.0

na

26.0

99.31

24.80

0.60

0.01

62.27

28.56

0.00

0.00

0.26

0,07

0.03

0.63

0.00

0.00

0.33

0.00

0.23

99.97

95.63

93:7

SAXPLZ

3710

70.70

15.00

1 .97

1.12

0.66

0.66

1.3«

3.636.62

0.06

na

153.0

na

B03.0

300.0

„.186.0

na

ua

«5.0

na

na

2 . )

na

na

12.0

99.01

26.57

3.30

0.00

26.61

33.13

0.00

O.OO

2.09

O.OO

0.39

0.26

0.00

0.00

3.09

0.00

0.93

99.92

86.30

90:10

NUMBER

531

69.6

IS.2

7 .0

1,0

0,66

0. 70

1.60

6.00

4.50

0.04

na

214.0

na

327.0

491.0

n .

171.0

na

na

45.0

na

na

1 . )

na

na

16.0

99.12

24.83

2.16

O.OO

25.11

36.36

0.00

0.00

2.17

0.00

0.16

0.66

0.00

0.00

2 .

0.00

0.93

99.93

86.28

88:12

616D

76.30

14.20

0.67

0.44

0.12

0.27

0.91

1.80

6.86

0.02

620.0

139.0

138.C

SSC.O

27.0

13.0

237.0

na

1.0

36.0

6 . 0

1.0

2 . 0

29.0

na

21.0

99.78

29.80

1.69

0.02

28.10

36.38

0.00

0.00

0.71

0.00

0.19

0.03

0.00

0.00

1.33

0.00

0.25

9.95

2.26

0:10

OP87D

69.60

16.60

1.62

7.20

0.18

1 81

3.60

3.58

1.68

0.06

260.0

174.0

141.0

515.0

328.0

3.0

97.0

. . .

8 , 0

96.0

u.u1.0

0 . 9

71.0

na

S.O

98.92

36.71

2.15

0.02

2.61

32.60

0.00

0.00

1.73

0.00

0.25

0.31

0.00

0.00

10.11

0.00

0.81

99.91

70.12

69:31

0P131D

73.50

16.60

0.95

0.60

0.17

0.61

1.66

1.08

1.86

O.Q2

na

Î9D.0

na

231.0

664.0

n .

«7.0

na

ua

11.0

na

na

0 . 7

na

na

7 .0

98.97

36.06

3.47

O.OO

21.96

28.26

0.00

0.00

1.01

0.00

0.11

0.64

0.00

0.00

1.95

0.00

0.36

99.95

86.28

82:18

0P112D

67. 3C

16.20

1.6»

1.7?

0. Id

1.20

1.90

6. SO

1.60

0.04

591.0

473.0

198.0

901.0

273.0

10.0

68.0

na

3.0

90.0

11.0

0 . 0

1.1

27.0

n .

7.0

98.78

25.95

1.2}

0.02

5.66

60.92

0.00

0.00

1.7B

0.00

0.66

0.26

0.00

O.OO

6.56

O.OO

O.SO

99.92

72.33

71:29

ISSN 0067-0367 ISSN 0067-0367

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