P O S I V A O Y

FI -27160 OLKILUOTO, F INLAND

Tel +358-2-8372 31

Fax +358-2-8372 3709

Seppo Pau lamäk i , Markku PaananenSeppo Gehör , Au l i s Kärk i

Ka i F rontI smo Aa l tonen , Tu ro Ahokas

K immo Kemppa inen , Juss i Mat t i l a

L i i sa Wiks t röm

May 2006

Work ing Repor t 2006 -37

Geological Model of the Olkiluoto SiteVersion 0

May 2006

Base maps: ©National Land Survey, permission 41/MYY/06

Working Reports contain information on work in progress

or pending completion.

Seppo Pau lamäk i , Markku Paananen

Geo log ica l Su rvey o f F in l and

Seppo Gehör , Au l i s Kärk i

K iv i t i e to Oy

Ka i F ront

VTT

I smo Aa l tonen , Turo Ahokas

K immo Kemppa inen , Juss i Matt i l a

L i i sa Wikst röm

Pos iva Oy

Work ing Report 2006 -37

Geological Model of the Olkiluoto SiteVersion O

ABSTRACT

The geological model of the Olkiluoto site consists of four submodels: the lithological model, the ductile deformation model, the brittle deformation model and the alteration model. The lithological model gives properties of definite rock units that can be defined on the basis the migmatite structures, textures and modal compositions. The ductile deformation model describes and models the products of polyphase ductile deformation, which enables to define the dimensions and geometrical properties of individual lithological units determined in the lithological model. The brittle deformation model describes the products of multiple phases of brittle deformation. The alteration model describes the types, occurrence and the effects of the hydrothermal alteration.

The rocks of Olkiluoto can be divided into two major classes: 1) supracrustal high-grade metamorphic rocks including various migmatitic gneisses, tonalitic-granodioritic-granitic gneisses, mica gneisses, quartz gneisses and mafic gneisses, and 2) igneous rocks including pegmatitic granites and diabase dykes. The migmatitic gneisses can further be divided into three subgroups in terms of the type of migmatite structure: veined gneisses, stromatic gneisses and diatexitic gneisses. On the basis of refolding and crosscutting relationships, the metamorphic supracrustal rocks have been subject to polyphased ductile deformation, including five stages.

In 3D modelling of the lithological units, an assumption has been made, on the basis of measurements in outcrops, investigation trenches and drill cores, that the pervasive, composite foliation produced as a result a polyphase ductile deformation has a rather constant attitude in the ONKALO area. Consequently, the strike and dip of the foliation has been used as a tool, through which the lithologies have been correlated between the drillholes and from the surface to the drillholes.

The bedrock in the Olkiluoto site has been subject to extensive hydrothermal alteration, which has taken place at reasonably low temperature conditions, the estimated temperature interval being from slightly over 300oC to less than 100oC. Two types of alteration can be observed: 1) pervasive (disseminated) alteration and 2) fracture-controlled (veinlet) alteration. Kaolinisation and sulphidisation are the most prominent alteration events in the site area. Sulphides are located in the uppermost part of the model volume following roughly the lithological trend (slightly dipping to the SE). Kaolinite is located also in the uppermost part, but the orientation is opposite to the main lithological trend (slightly dipping to the N). The third main alteration event, illitisation, appears to form a wedge- or dome-like body located outside and north of the ONKALO access tunnel but penetrating the planned eastern repository panel.

1700 fault planes and fault striation orientations, and sense-of-shear of the faults were measured from drillholes OL-KR1 – OL-KR33. On the basis of the statistical analysis of the orientation data, faults have tentatively been divided in five main fault groups: A, B, C, D and E. Fault-slip vector directions are subhorizontal, N-S trending for group A, gently NE or SW plunging for group B, gently SSE plunging for group C, gently ENE plunging for group D and gently SE plunging for group E. On the basis of drillhole data, 98 fault zones were determined from the drillholes and modelled in 3D. In addition, the model includes 3 fault or fracture zones observed both at the surface and in the

ONKALO access tunnel, and two zones interpreted on the basis of charge potential survey.

Key words: lithology, ductile deformation, brittle deformation, hydrothermal alteration, 3D modelling, nuclear waste disposal, Olkiluoto, Eurajoki, Finland.

TIIVISTELMÄ

Olkiluodon alueen geologinen malli koostuu neljästä osamallista: litologinen malli, duktiilin deformaation malli, hauraan deformaation malli ja muuttuneisuuden malli. Litologinen malli kuvaa kivilajiyksiköt, jotka voidaan määrittää migmatiitirakenteen, kiven asun ja mineraalikoostumuksen perusteella. Duktiilin deformaation malli kuvaa ja mallintaa monivaiheisen duktiilin deformaation rakenteet, mikä mahdollistaa litologisten yksiköiden koon ja geometristen ominaisuuksien määrittämisen. Hauraan deformaation malli kuvaa monivaiheisen hauraan deformaation tulokset. Muuttuneisuuden mallissa kuvataan hydrotermisen muuttumisen tyypit, esiintyminen ja sen vaikutukset.

Olkiluodon kivilajit voidaan jakaa kahteen pääluokkaan: 1) suprakrustiset, korkean metamorfoosiasteen kivet, jotka ovat erilaisia migmatiittisia gneissejä, tonaliitti-granodioriitti-graniittigneissejä, kiillegneissejä, kvartsigneissejä ja mafisia gneissejä, 2) magmakivet, jotka ovat pegmatiittisia graniitteja ja metadiabaaseja. Migmattiittiset gneissit voidaan edelleen jakaa kolmeen alaryhmään migmaattirakenteen perusteella: suonigneissit, raitaiset gneissit ja diateksiittiset gneissit. Uudelleenpoimutus- ja leikkaussuhteiden perusteella metamorfiset kivet ovat käyneet läpi viisivaiheisen duktiilin deformaation.

Litologisten yksiköiden 3D-mallinnuksessa on maanpinta- ja kairanreikähavaintojen perusteella oletettu, että monivaiheisessa duktiilideformaatiossa syntyneellä läpikotaisella liuskeisuudella melko pysyvä suuntautuneisuus tutkimusalueella. Tämän perusteella liuskeisuuden suuntaa ja kaltevuutta on voitu käyttää työkaluna, jolla litologisia yksiköitä on korreloitu kairanreikien välillä ja maanpinnalta kairanreikään.

Olkiluodon kallioperässä on vaikuttanut laajamittainen hydroterminen muuttuminen, mikä on tapahtunut melko alhaisessa lämpötilassa (300 - 100oC). Muuttuminen jakaantuu kahteen päätyyppiin: 1) läpikotainen muuttuminen ja 2) suoniverkostotyyppinen tai rakoilun kontrolloima muuttuminen. Kaoliniittiutuminen ja kiisuuntuminen ovat merkittävimmät muuttumiset. Muuttumisen kolmas päätyyppi, illiittiytyminen, on satunnaista ONKALOn alueella, mutta se näyttää muodostavan laajan, kiila- tai doomimaisen muodostuman ONKALOn pohjoispuolisella alueella lävistäen suunnitellun itäisen loppusijoitustilan

Kairanrei'istä OL-KR1 – OL-KR33 mitattiin 1700 siirrostason ja siirrosvektorin suuntaukset. Mittaustulosten tilastollisen käsittelyn perusteella siirrokset voidaan jakaa viiteen ryhmään: A) loiva-asentoiset siirrokset, joiden siirrosvektorit ovat etelälounaaseen tai pohjoiskoilliseen, B) pystyistä loiva-asentoisiin vaihtelevat siirrokset, joiden siirrosvektorit ovat koilliseen tai lounaaseen ja C) loiva-asentoiset siirrokset, joiden siirrosvektorit ovat itäkaakkoon, D) loiva-asentoiset siirrokset, joiden siirrosvektorit ovat itäkoilliseen ja E) loiva-asentoiset siirrokset, joiden siirrosvektorit ovat kaakkoon. Siirroksia yhdistettiin kairanreiästä toiseen siirrosvektorien suuntien perusteella. Mallissa on 98 tällä tavalla kairanrei’istä tulkittua ja mallinnettua siirrosvyöhykettä. Lisäksi malli sisältää kolme maanpinnalta ja tunnelista havaittua siirros- tai rikkonaisuusvyöhykettä sekä kaksi latauspotentiaalimittausten perusteella tulkittua vyöhykettä.

Asiasanat: litologia, duktiili deformaatio, hauras deformaatio, hydroterminen muuttuminen, 3D-mallinnus, ydinjätteiden loppusijoitus, Olkiluoto, Eurajoki.

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TABLE OF CONTENTS

ABSTRACT

TIIVISTELMÄ

TABLE OF CONTENTS.................................................................................................. 1 PREFACE....................................................................................................................... 3

1 INTRODUCTION .................................................................................................... 5 1.1 Background..................................................................................................... 5 1.2 Objectives and scope...................................................................................... 5

2 APPLIED INVESTIGATION DATA ......................................................................... 9 2.1 Geological data ............................................................................................... 9

2.1.1 Surface data (outcrops, trenches)........................................................... 9 2.1.2 Drill core investigations ......................................................................... 10 2.1.3 The VLJ repository ................................................................................ 14 2.1.4 ONKALO underground rock characterisation facility............................. 14

2.2 Geophysical data .......................................................................................... 16 2.2.1 Airborne and ground geophysics .......................................................... 16 2.2.2 Drillhole geophysics .............................................................................. 21

3 METHODOLOGY OF DETERMINISTIC MODELLING ........................................ 27 3.1 Lithological model ......................................................................................... 28 3.2 Ductile deformation model ............................................................................ 30 3.3 Brittle deformation structures ........................................................................ 30 3.4 Retrogressive metamorphism and alteration ................................................ 31 3.5 Modelling and visualisation in 3D.................................................................. 32

3.5.1 Modelling of ductile deformation and lithology ...................................... 32 3.5.2 Modelling of hydrothermal alteration ..................................................... 36 3.5.3 Modelling of brittle deformation ............................................................. 38

4 LITHOLOGICAL MODEL...................................................................................... 43 4.1 Description of the lithologies ......................................................................... 43

4.1.1 Migmatitic gneisses............................................................................... 44 4.1.2 Gneisses ............................................................................................... 45 4.1.3 Pegmatitic granites................................................................................ 46 4.1.4 Diabases ............................................................................................... 46

4.2 Whole rock chemistry and petrography ........................................................ 47 4.2.1 The T series .......................................................................................... 48 4.2.2 The S series .......................................................................................... 49 4.2.3 The P series .......................................................................................... 49 4.2.4 Mafic and ultramafic metavolcanics ...................................................... 50 4.2.5 Pegmatitic granites................................................................................ 50

4.3 Metamorphic mineral assemblages and secondary alteration products ....... 51 4.4 Two-dimensional lithological model .............................................................. 52 4.5 Three-dimensional lithological model............................................................ 54

4.5.1 Diatexitic gneiss/veined gneiss contact zone........................................ 54 4.5.2 Tonalitic-granodioritic-granitic gneiss units (TGG1 – TGG17) .............. 55 4.5.3 Pegmatitic granite units (PGR1-PGR36)............................................... 59

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4.5.4 Diabase dykes (DB1-DB6) .................................................................... 64 4.6 Correlation to lithology in southern Satakunta .............................................. 65 4.7 Correlation to previous bedrock model ......................................................... 67 4.8 Correlation to ONKALO area model version 0.............................................. 68 4.9 Evaluation of implications for construction.................................................... 68

5 DUCTILE DEFORMATION MODEL ..................................................................... 69 5.1 Description of the ductile deformation........................................................... 69 5.2 Two-dimensional Model ................................................................................ 73 5.3 Three-dimensional Model ............................................................................. 74 5.4 Correlation to ductile deformation of the Svecofennian Domain................... 75 5.5 Correlation to previous bedrock model ......................................................... 76 5.6 Correlation to ONKALO area model version 0.............................................. 76 5.7 Evaluation of implications for construction.................................................... 76

6 ALTERATION MODEL WITH SPECIAL EMPHASIS ON HYDROTHERMAL ALTERATION ....................................................................................................... 79

6.1 Description of hydrothermal alteration .......................................................... 81 6.2 Kaolinisation.................................................................................................. 87 6.3 Sulphidisation................................................................................................ 89 6.4 Illitisation ....................................................................................................... 91 6.5 Carbonatisation............................................................................................. 93 6.6 Evaluation of implications to construction ..................................................... 95 6.7 Correlation to the bedrock in Finland in general ........................................... 97

7 BRITTLE DEFORMATION MODEL...................................................................... 99 7.1 Description of brittle deformation .................................................................. 99 7.2 3D model..................................................................................................... 103

7.2.1 Interpreted brittle fault zones............................................................... 103 7.2.2 Observed brittle fault or joint zones..................................................... 125 7.2.3 Possible brittle fault zones .................................................................. 133

7.3 Correlation to previous bedrock model ....................................................... 134 7.4 Correlation to ONKALO area model version 0............................................ 136 7.5 Intersections with ONKALO underground rock characterisation facility...... 136 7.6 Evaluation of implications for construction.................................................. 137 7.7 Lineament map ........................................................................................... 138

8 SELECTED FRACTURE STATISTICS............................................................... 141 8.1 Surface fractures (outcrops and trenches).................................................. 141 8.2 Fractures in the ONKALO access tunnel .................................................... 145 8.2 Fractures in drillholes.................................................................................. 146 8.3 Statistical modelling of fractures ................................................................. 148

9 EVALUATION OF UNCERTAINTIES ................................................................. 151

10 SUMMARY...................................................................................................... 155

11 FUTURE ACTIVITIES..................................................................................... 159

REFERENCES ........................................................................................................... 161

APPENDICES............................................................................................................. 173

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PREFACE

The geological model of the Olkiluoto site area has been produced by the Geological Modelling Task Force (GeoMTF), a team of experts of geology and geophysics established by Posiva to carry out geological modelling of Olkiluoto. The following members of the GeoMTF have contributed to the modelling work: Kai Front of the Technical Research Centre of Finland (VTT), Aulis Kärki and Seppo Gehör of Kivitieto Oy, Markku Paananen and Seppo Paulamäki of the Geological Survey of Finland (GTK), and Ismo Aaltonen, Turo Ahokas, Kimmo Kemppainen, Jussi Mattila and Liisa Wikström of Posiva Oy. Markku Paananen and Seppo Paulamäki have constructed the 3D models with Surpac® Vision 3D software.

The report has been reviewed by Johan Andersson of JA Streamflow AB, Sweden, Pirjo Hellä of Pöyry Environment Oy, Nuria Marcos of Saanio & Riekkola Oy, Alan Geoffrey Milnes of GEA Consulting, Switzerland, Raymond Munier of the SKB, Sweden and Petteri Pitkänen of the VTT. The authors wish to thank them for their valuable comments and suggestions. Mr. Christopher Cunliffe is thanked for corrections to the English of the text.

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1 INTRODUCTION

1.1 Background

In Finland, two companies, Teollisuuden Voima Oy (TVO) and Fortum Power and Heat Oy (formerly Imatran Voima Oy), utilise nuclear energy to generate electric power. The companies are preparing for the final disposal of the spent nuclear fuel waste deep in the bedrock. In 1996, they established a joint company, Posiva Oy, to run the programme of site suitability investigations and other research and development for spent fuel disposal. Posiva will ultimately construct and operate the future disposal facility. After an extensive investigation programme had been carried out at several sites since 1987, Posiva submitted an application to the Government in May 1999 for a Decision-in-Principle to build a final disposal facility for spent fuel at Olkiluoto, in the municipality of Eurajoki. The Decision-in-Principle was approved by the Finnish parliament in 2001, allowing Posiva to continue the development of a repository in the bedrock of Olkiluoto. Construction of the repository should start after 2015, and the final disposal facility will commence operations in 2020 (Tanskanen & Palmu 2003). As a part of the site investigations, an underground rock characterisation facility, ONKALO, is being constructed at Olkiluoto during 2004-2010. The aim of ONKALO is to study the bedrock of the site for the planning of the repository and for the safety assessment, and to test the disposal techniques in real deep-seated conditions. At a later date, it may become part of the repository. ONKALO will be composed of characterisation facilities, connected to the surface by an access tunnel and a ventilation shaft. Its construction will begin with excavation of approximately 5.5 km of tunnelling to the depth of 520 m. The main characterisation level of ONKALO will be at the depth of 420 m and the lower level at 520 m. Excavation of the ONKALO access tunnel started in autumn 2004 and has now reached a chainage of about 1020 m (depth ca. 90 m).

1.2 Objectives and scope

The objective of the work leading to the present report was to develop a “start version” (version 0) of the geological model of the Olkiluoto site area, based on the state of geological knowledge at the beginning of underground investigations at the Olkiluoto site, in a format that could be later used to create updated and revised versions as excavations and investigations proceed. The purpose of the site model is to evaluate the geological properties and conditions of the rock mass in the modelled area and as such, the model acts as an important background reference for construction, layout design, safety assessment and hydrological and geomechanical models. In contrast to the published ONKALO area model (Paananen et al. 2006), which mainly focused on the needs of the ONKALO tunnel construction, in the site model report more effort has been focused on the description of the applied modelling methodology and the estimation of uncertainties. The applied modelling methodologies will also be reported in forthcoming modelling methodology report (Milnes et al., in prep.).

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The geological database used in the modelling has largely been collected and analysed after the production of the most recent version of the bedrock model from the site investigation phase (Vaittinen et al. 2003) and it is emphasised that, at this stage, the model is partly tentative, as much of the geological data has been acquired only a few months prior to the release of this report. Accordingly, the results and conclusions of this report reflect the current stage of the learning process of understanding the site-specific geological features. The quality and accuracy of the site model will be improved as the knowledge of the geology evolves through prediction-outcome studies and the acquisition of an increasing amount of data.

The modelled bedrock volume covers an area of 2 km x 2 x 1 km, which is named the Olkiluoto site area (Fig. 1-1). The geological model combines the geological surface and drill core studies and interpretations of geophysical airborne, ground survey, and drillhole measurements.

Figure 1-1. Nominal model areas of Olkiluoto, including the Olkiluoto site area.

The geological site model is composed of four submodels: the ductile deformation model, the lithological model, the alteration model and the brittle deformation model.

The ductile deformation model describes and models the products of polyphased ductile deformation, which makes it possible to define the dimensions and geometrical properties of individual lithological units determined in the lithological model and also to asses the orientation and effects of the anisotropy of the lithology. Ductile deformation is also an important precursor to the subsequent brittle deformation.

The lithological model provides a general view of the lithological properties of modelled rock units that can be defined volumetrically on the basis of the products of ductile deformation and the data acquired from outcrops and drillholes. In general, the

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lithological classification of crystalline rocks is based on whole-rock chemical composition, modal mineral composition, texture and/or macroscopic structural features. In the case of Olkiluoto, the method used for the classification of the metamorphic rocks is a synthesis, in which the modal compositions, textures and migmatite structures are jointly evaluated. The igneous rocks are classified on the basis of modal compositions and textures. The implications of the textural and structural properties of different lithologies for underground construction are assessed in chapters 4.9 and 5.7.

Hydrothermal alteration and subsequent low-temperature weathering have affected all the lithological units in the study area. Alteration transforms the physical properties of rock material and alteration products may have physical properties drastically different to those of primary, fresh materials. Thus the degree and type of secondary/retrograde alteration may be important parameters in the evaluation of, e.g., the mechanical strength of the rocks.

The brittle deformation model describes large-scale structures produced during the long history of brittle deformation, i.e. the fault zones and joint cluster zones. Brittle deformation products may have important implications for construction and long-term safety and a first attempt at evaluating their properties is given in the following text. This report focuses on the description of deterministic features of the brittle deformation and the results of discrete fracture network (DFN) modelling will be presented in a separate report.

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2 APPLIED INVESTIGATION DATA

2.1 Geological data

2.1.1 Surface data (outcrops, trenches)

Geological mapping of the outcrops has been carried out on several occasions during the site investigations. The first general geological mapping of the outcrops (Paulamäki 1989) included mapping of the rock types and the main structural features, especially fractures. The aim of the detailed structural geological mapping, carried out a few years later (Paulamäki & Koistinen 1991), was to describe the ductile deformation history of Olkiluoto. Ismo Aaltonen and Jussi Mattila of Posiva Oy have made additional lithological and structural observations from outcrops at Olkiluoto during investigations in 2003 and 2004. The geological mapping of the Olkiluoto 3 construction site was performed in 2004 (Talikka 2005).

Since only a small part of the bedrock at Olkiluoto is exposed, outcrop mapping has been supplemented by the excavation and mapping of several investigation trenches in the central part of the site (Paulamäki 1995, 1996; Lindberg & Paulamäki 2004; Paulamäki & Aaltonen 2005; Paulamäki 2005a; Paulamäki 2005b; Engström 2006; Nordbäck & Talikka in prep.; Mattila et al. in prep.). The purpose of the trenches was to obtain more bedrock and fracture data from areas with few or no outcrops. The trench mappings included observation of ductile and brittle deformation and the macroscopic determination of lithologies from the bedrock surface, after removal of the remaining loose soil with compressed air and cleaning with a high-pressure washer. The total length of the trenches is ca. 3500 m and they range in width from 0.5 m to 5 m. Additionally, in the area of the Korvensuo reservoir, the exposed surfaces of two sediment-filled basins each measuring 30 m x 85 m have been mapped (Äikäs 1995).

During the mapping, the rock types were determined macroscopically from the exposed outcrop surface. At the same time, samples for further microscopic, geochemical and petrophysical analyses of rock types were taken. The petrography of a total of 58 rock samples was determined. Geochemical data of 26 surface samples are included in Lindberg & Paananen (1991), Kärki & Paulamäki (2006) and Mänttäri et al. (2004). The petrophysical measurements of 24 surface samples are presented in Paananen (2004).

A total of 12137 tectonic measurements have been made, both at outcrops and in the investigation trenches, including 2827 measurements of ductile deformation (foliation, fold axis, axial plane, fault plane and lineation) and 11494 fracture measurements. Additionally, a detailed fracture mapping was carried out in the area of the Ulkopää cape, as part of the investigations for the repository for low- and intermediate-level waste, which included a further 1700 fracture measurements (Sacklén 1994).

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Figure 2-1. Location of the observation points (black crosses) and investigation

trenches at the Olkiluoto site area.

2.1.2 Drill core investigations

Deep core drilling has been carried out since 1988, the total number of deep drillholes now exceeding 35. However, only the data from drillholes OL-KR1 - OL-KR33 has been used in this modelling work (Fig. 2-2). Preliminary descriptions of all drill cores have been published as Posiva Working Reports. The most recent ones, for cored drillholes OL-KR15 – OL-KR33 (drilled between 2000 and 2004, before the start of underground excavations), which are written in English, are included in the list of references (Niinimäki 2002a-h, 2003a-d; Rautio 2002, 2003, 2004a-c, 2005a-b). The drill cores are mostly 300 – 1000 m in length, with a combined length of 17 000 m. Gehör et al. (1996b, 1997, 2000, 2005) and Lindberg & Paananen (1991, 1992) have presented the results of petrological studies from drillholes OL-KR1 – OL-KR28. These reports include the results of visual drill core loggings, polarisation microscope examinations and whole-rock chemical analyses of ca. 250 samples. Drillholes OL-KR29 – OL-KR33 were logged during this work.

In addition to deep drillholes, 36 shallow (10-20 m) drillholes have been drilled to supplement the bedrock mapping (Suomen Malmi 1989). In the site area, there are also 16 shallow drillholes with the depth range of 14-36 m drilled earlier in the 1970s and relogged in 1990 (Jokinen 1990).

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Pilot holes ONK-PH1 - ONK-PH3 have been drilled down the centre line of the ONKALO access tunnel, as part of the ONKALO investigations. In addition, 7 shallow (15.2-45.80 m) drillholes OL-PP40 - OL-PP41 and OL-PR5 – OL-PR9 have been drilled directly above the access tunnel.

Figure 2-2. Location of deep drillholes OL-KR1 – OL-KR33 in the Olkiluoto site area.

A productive short-term campaign was undertaken to gather the necessary basic structural data for both ductile and brittle deformation models during the spring and summer of 2005. Different elements and kinematic features of structural geological evolution were systematically logged along cored samples of drillholes OL-KR1 – OL-KR33B. A total of ca. 1 700 fault plane and fault vector directions were measured.

Foliation and ductile shear zones were systematically logged using 1-metre resolution. All 1-metre sections were systematically characterised according to the type and degree of foliation using the procedures outlined in Milnes et al. 2006. Also small-scale fold axes, axial planes and lineations were observed. OPTV drillhole images and WellCAD software were used for foliation orientation measurements. In some cases measurements were done from the oriented core. Logging was partly done at Olkiluoto and partly at the national drill core depot of Geological Survey of Finland at Loppi. In toto more than 17 000 observations and measurements were done on ductile features.

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Foliated rocks were subdivided into nine descriptive types. The two independent factors were type of foliation and degree of foliation. Visual estimation of degree of foliation classified rocks into weakly foliated (1), moderately foliated (2) and strongly foliated (3) ones. Subdivision into three categories of the degree of foliation was gneissic (rock dominated by quartz and feldspars; no continuous trains of micas or amphiboles), banded (intercalated gneissic and schistose layers), schistose (rock dominated by micas and/or amphiboles; these minerals are arranged in continuous trains so that the preferred orientation of crystallographic cleavages provide a general plane of mechanical weakness). Rocks with no foliation (e.g., most granites of Olkiluoto) are classified as massive. In that case foliation degree is 0. Also several migmatites without continuous foliation fall into that category and are called irregular. (Milnes et al., in prep).Concurrently with the foliation logging, the most obvious (> 1-m long sections) ductile shear zones were evaluated, and the general geological description, orientation, intensity and kinematic information were recorded.

The logging of brittle deformation events had two main objectives. The first step was to detect all those fractures, which carry imprints of tectonic movements, i.e. slickensides. These fractures were studied in order to obtain characteristics of fracture surfaces as shape, indicative traces of movement, orientation and kinematics (fault direction vector, direction of slip).

In the second step, along with the slickenside study, the deformation zone intersections were observed. Deformation zone intersection in this report is an observation of an inferred deformation zone in a drillhole, tunnel or other observation line or surface. Deformation zone is a tabular deformation unit or domain with sub-parallel and sub-planar margins, and has certain thickness, which is very much less than its lateral extent. In this work deformation zone intersections were divided into five classes: High-grade

ductile deformation zone intersection (HGI), Low-grade Ductile shear zone intersection(DSI), Semi brittle fault zone intersection (SFI), Brittle joint zone intersection (BJI) and Brittle fault zone intersection (BFI). Appendix 1 shows the hierarchical classification procedure for deformation zone intersections at Olkiluoto (Milnes et al. in prep.). Each intersection was assigned a unique label, which defines the type of deformation product and also the observed intersection interval in the drill core sample.

Indicators of intense ductile shear in sample were detected to recognise a HGI. Because of small sample size, identification of ductile zones was difficult. No low-grade ductile shear intersections (mylonites, phyllonites etc.) have been observed at Olkiluoto. During transition from the ductile deformation to brittle phases the rock was sheared and deformed in a semi-brittle fashion. These features were used to find SFI sections. BJI is a section with high fracture frequency compared to the surroundings but has no fault indicators. If at least one slickensided fracture surface is observed, the section can be classified as BFI. No fracture frequency limit (e.g. 10/m) was used for determining a brittle deformation zone intersection, but the determination was based on expert judgement. There can be large variation of thickness, fracture number etc. within the zone. Generally, brittle joint sets include intersections of fracturing that do not show traces of faulting and fractures are more or less parallel to each other and with ductile features. In the case of brittle fault intersections, fracturing is generally more intense, and faulting and cataclastic features are obvious but in some cases brittle fault

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intersections may show only one or few slickensided fracture surfaces. Logging of brittle faults intersections consisted of observations on rock type, especially fracture types, orientation of fractures and fracture sets, relation of fractures to ductile features (foliation, schistosity, shearing), cataclastic features, breccias, fault gouges. A note on drilling-induced fracturing was also given, as well as an estimation of traces of water-flow on fracture surfaces. From boreholes KR1-KR33, 42 high-grade ductile shear intersections, 8 semi-brittle fault intersections, 125 brittle fault intersections and 82 brittle joint intersections were determined. In this model only semi-brittle and brittle intersections were used.

Not all the broken drill core sections are intersections of brittle zones. Without careful mapping, technical breaks with only a few natural fractures within a short core section can be mapped as a zone intersection. In Table 1 of Appendix 2, descriptions of the mapped deformation zone intersections from drillhole OL-KR25 are presented as an example of the type of data produced during the structural geological mapping campaign mentioned in the preceding text. The descriptions are presented together with information of the intersection identification code, along-the-hole length of the intersection, type of intersection (classified according to the system presented in Appendix 1), geologist who performed the mapping and mapping date.

The kinematic database used in the present model contains data on about 1700 slickesides. In Table 2 of Appendix 2, the kinematic data mapped from drillhole OL-KR25 is shown as another example of the type of data produced during the structural geological mapping campaign. The column DRILLHOLE refers to the mapped drillhole, DEPTH to along-the-hole depth of a mapped fracture, SAMPLE to fracture orientations measured from oriented drill core, IMAGE to fracture orientations measured from WellCAD-image, DISPLACEMENT VECTOR to the orientation of measured slip-linear, U to the sense-of-movement of the slip-linear in respect to horizontal plane, E in respect to NS-striking vertical plane and S in respect to EW-striking vertical plane. CERTAINTY refers to the estimated confidence of the sense-of-movement where 1=certain, 2=uncertain and 3=very uncertain. In the DESCRIPTION column the quality of the fracture surface is described with abbreviations which refer to striated surfaces (STRIA), planar surfaces (PLAN), undulating surfaces (UNDU), irregular surfaces (IRREG), concave or convex surfaces (CONC), grooved surfaces (GROV). In addition, stepped surfaces are described with the abbreviation STEP and observed pressure shadow growth of minerals is described with PSGR. SOURCE-column indicates which of the fracture orientation measurements, either SAMPLE or IMAGE, is used in the measurement of the orientation of the slip-linear (DISPLACEMENT VECTOR).

In Table 3 of Appendix 2, a complete collection of geological and geophysical data from drillhole OL-KR25 is presented as a WellCAD-image as an example.

Hydrothermal alteration research benefited considerably from the very detailed study of fracture mineralogy and a newly redeveloped fracture database, which recently consisted of more than 40 000 fracture records. Simultaneously with re-logging of

14

fractures the drill cores were studied locate those sections, in which the hydrothermal alteration is clearly observable to the naked eye.

2.1.3 The VLJ repository

The VLJ repository (Fig. 2-3), situated at the depth of 70—100 metres in the crystalline bedrock, was constructed in Olkiluoto in 1988-1989 to be used for the disposal of low-level maintenance waste and intermediate-level operating waste. The geological studies performed before the excavation of the repository are summarised in Äikäs (1986). The results of the geological mapping of the tunnels, shafts and waste silos are presented in Ikävalko & Äikäs (1991). A short research tunnel within the repository was mapped in detail by Äikäs & Sacklén (1993).

Figure 2-3. The VLJ repository at Olkiluoto

2.1.4 ONKALO underground rock characterisation facility

The excavation of the ONKALO underground rock characterisation facility was started on the 22nd of September 2004 and in January 2006 the access tunnel has reached the length of 990 metres (corresponding to the depth of 90 metres below sea level, approximately). Geological mapping of the ONKALO tunnel has been performed

15

systematically in intervals of 5 meters, corresponding to the length of one excavation round. The mapping includes the determination of rock types, measurement of structural features (foliation, fold axis, axial planes, slip lineation and slip sense of brittle deformation features) and detailed mapping of fractures of all trace length distributions.

Sections of increased fracturing in the ONKALO tunnel were mapped and subdivided into brittle joint intersections (BJI) and brittle fault intersections (BFI). Sections showing evidence for high strain without the development of specific surfaces of rupture were mapped as high-grade ductile shear intersections (HGI). This classification corresponds to the system used in the logging of brittle deformation products from the drill cores. The results of the geological mapping of the first 840 m of the tunnel were used in the modelling and are shown schematically in 2D in figures 2-4 and 2-5.

Figure 2-4. Mapped deformation zone intersections from the ONKALO access tunnel

16

Figure 2-5. Lithology of ONKALO chainage 0-820 m.

2.2 Geophysical data

2.2.1 Airborne and ground geophysics

Geophysical airborne data have been available from two separate survey campaigns done by GTK and Scintrex (Suomen Malmi 1988). The airborne data include the following methods:

- Magnetic (total field and vertical gradient) - Multifrequency EM with 888, 3113 (GTK) 7837 and 51250 Hz - VLF - Radiometric (K, U, Th, total intensity)

Figures 2-6 and 2-7 show the magnetic data from both surveys.

17

Fig 2-6. Aeromagnetic data around Olkiluoto by GTK. Map from Korhonen et al.

(2005). The black frame indicates the Olkiluoto site area.

The first interpretations of the data have been carried by Paananen and Kurimo (1990), followed by two lineament interpretations (Paulamäki & Paananen 2001, Paulamäki et al. 2002). The most recent lineament interpretation, combining systematically topographic and geophysical data, is done by Korhonen et al. (2005).

18

Fig. 2-7. Aeromagnetic data by Scintrex (Suomen Malmi 1988). Map compiled by GTK.

(Korhonen et al. 2005). The black frame indicates the Olkiluoto site area.

Geophysical ground surveys comprise magnetic (Fig. 2-8) and horizontal-loop EM measurements (Suomen Malmi Oy 1989). Furthermore, seismic refraction (Lehtimäki 2003a,b; Fig. 2-9) and wide-band electromagnetic soundings (Jokinen 1990, Jokinen & Jokinen 1994; Ahokas 2003; Jokinen & Lehtimäki 2004) have been carried out as several separate campaigns.

The magnetic data have been used in delineating most intensely magnetized rock type units. According to petrophysical data (Lindberg & Paananen 1991a, 1991b, 1992; Paananen & Kurimo 1990; Paananen 2004), susceptibility does not directly indicate different rock types. However, the most significant magnetic anomalies are related to ferrimagnetic, pyrrhotite-bearing gneisses (vein gneisses, mica gneisses, diatexite).

19

According to most recent systematic 3D profile modelling, the dips of the magnetized units become gentler with depth, agreeing well with the foliation observations in the drillholes.

Figures 2-8 and 2-9 show ground magnetic and seismic refraction data and the lineaments (Korhonen et al. 2005) interpreted according to these datasets.

Figure 2-8. Lineaments interpreted from ground magnetic data (Korhonen et al. 2005).

The black frame indicates the Olkiluoto site area.

20

Figure 2-9. P-wave velocity data (Lehtimäki 2003a,b) and interpreted lineaments,

related to low-velocity zones (Korhonen et al. 2005). The black frame indicates the

Olkiluoto site area.

SAMPO Gefinex wide-band electromagnetic soundings were carried out at Olkiluoto as four separate campaigns in 1990, 1994, 2002 and 2004 (Jokinen 1990; Jokinen & Jokinen 1994; Ahokas 2003; Jokinen & Lehtimäki 2004). They have been used in mapping deep saline groundwaters, but they also provide information on sulphide minerals and possible deformation zones related to sulphide-rich locations. Previous interpretations have been done for each survey campaign (Paananen et al. 1991; Jokinen et al. 1995; Heikkinen et al 2004a), but they are all separate works and somewhat incoherent. During the present modelling work, the data from different years were uniformly interpreted, taking also into account the known electric conductors (Fig. 2-10).

21

Figure 2-10. SAMPO-Gefinex interpretation from vertical section Y =6791900 as an

example, coil separation = 200 m. The red sections represent interpreted conductors,

related to sulphide-rich zones. Arrows indicate the locations of probable ground

exposures of the conductors.

2.2.2 Drillhole geophysics

Single-hole geophysics

The single-hole data of the drillholes within the site area were re-interpreted. The drillholes examined were OL-KR1 - OL-KR28 (Niva 1989; Suomen Malmi Oy 1989, 1990; Julkunen et al. 1995, 1996, 2000a,b, 2002, 2003, 2004a,b; Laurila & Tammenmaa 1996; Lowit et al. 1996; Lahti et al 2001, 2003; Heikkinen et al. 2004b). Hydraulic data were from Rouhiainen (1999) and Pöllänen & Rouhiainen (2000a,b, 2001, 2002a,b). The locations of the drillholes are presented in Fig. 2-2. The interpretation is purely based on geophysical data; no geological logging information from the drill cores was used.

The single-hole data gathered comprises different seismic (p-wave and s-wave velocity, p-wave and tubewave attenuation), radiometric (gamma-gamma, neutron-neutron), electric (long normal, short normal/wenner), magnetic and caliper data. Also, hydraulic (OL-KR1 – OL-KR11) and thermal data were used to map the locations of hydraulic fractures or distribution of hydraulic conductivity). The seismic, radiometric, electric and hydraulic parameters have been mainly used in determining the locations of the deformation zones (however sulphides have a strong effect on electric measurements). The magnetic data are mainly used in locating ferrimagnetic, pyrrhotite-rich sections. Figure 2-11 presents the profiles of the most important geophysical single-hole

0Z

-500Z

1525000 1525500 1526000 1526500 1527000

0 – 500

500 - 1000

1000 - 3000

3000 -

Ohmm

22

parameters from drillhole OL-KR23 between c. 40 – 150 m. Table 2-1 shows the interpretation in details.

Figure 2-11. Single-hole geophysics and its interpretation, drillhole OL-KR23.

Rasterised area = fracturing, red = sulphides.

23

Table 2-1. Interpretation of drillhole OL-KR23 as an example: fractured and sulphide-rich sections.

Location (m) Assumed character integrated interpretation

36.7-42.3 fracturing

44.0-46.6 fracturing

47.6-56.4 intense fracturing

67.7-68 fracturing

70-73 fracturing?

85.4-89 fracturing

134.0-142 open? fracturing

104-187 pyrrhotite (several separate anomalies)

173.5-177.5 Intense fracturing, pyrrhotite

194-202.9 fracturing,pyrrhotite

244-246.6 fracturing

259-260.9 fracturing

265-269 intense fracturing

Petrophysics

In the Olkiluoto area, petrophysical measurements have been done from drillholes OL-KR1 – OL-KR6 (Lindberg & Paananen 1991a, 1992), bedrock outcrops and shallow drillholes (Paananen & Kurimo 1990) and the VLJ repository (Lindberg & Paananen 1991b). Recently, the data have been supplemented by the results from OL-KR8, OL-KR15, OL-KR19 – OL-KR23 and 24 minidrill samples from the ground surface (Paananen 1994).

Charged potential

Several charged potential cross-hole measurements have been carried out in Olkiluoto (Lehtonen & Heikkinen 2004; Lehtonen 2006). The groundings have been located in drillholes OL-KR4, OL-KR7, OL-KR25, OL-KR28 and OL-KR29. The locations of the current groundings are based on the previous bedrock model of Olkiluoto (Vaittinen et al. 2003). With the charged potential measurements, it has been possible to define mostly gently dipping, electrically conducting horizons that occasionally coincide with the deformation zones (Fig. 2-12).

24

Figure 2-12. Electric conductors defined by charged potential cross-hole survey, view

from SW. The frame indicates the Olkiluoto site volume.

Seismic drillhole measurements

Vertical seismic profiling (VSP) surveys have been carried out as several campaigns in Olkiluoto, starting in 1990. Over the years, the survey technique as well as the interpretation procedure has been greatly developed. In this study, the VSP interpretation results from each drillhole in the Site model area have been examined and correlated to geological data. The most recent VSP results are from the following drillholes, located in the ONKALO area:

OL-KR7, OL-KR8 (Cosma et al. 2003, Heikkinen et al. 2004) OL-KR4, OL-KR10, OL-KR14 (Enescu et al. 2004, Heikkinen et al. 2004).

Furthermore, HSP results from the Korvensuo reservoir (Cosma et al. 2003) and cross-hole surveys between OL-KR14 and OL-KR15 (Enescu et al. 2003) and KR4 and OL-KR10 (Enescu et al. 2004) have been available. In addition to this, the results of the Walkaway Vertical Seismic Profiling (WVSP) from drillholes OL-KR4, OL-KR8, OL-KR10 and OL-KR14 (Enescu et al. 2004, Heikkinen et al. 2004) were available.

In Figure 2-13, interpreted reflecting elements of OL-KR8 are presented as an example.

25

Figure 2-13. VSP reflectors from drillhole OL-KR8, showing mostly gently dipping

features. The frame indicates the Olkiluoto site volume.

26

27

3 METHODOLOGY OF DETERMINISTIC MODELLING

The geological modelling procedure involves four partially independent submodelling tasks to produce one geological model. The present geological model is composed of the lithological model, the ductile deformation model, the brittle deformation model and the alteration model (Fig. 3-1). Modelling work dealing with different thematic topics is based on the basic methods of geology and geophysics and principally on detailed evaluation of the results of various geological and geophysical measurements and analyses.

1) The lithological model provides a general view of the lithological properties of definite rock volumes or units that can be defined on the basis of a proper set of parameters. The goal of the model is to represent a spatial distribution of lithologically fixed and genetically related bedrock units, which, from the perspective of underground facilities building, have sufficiently constant properties.

2) The ductile deformation model describes the products of polyphase ductile deformation, which makes it possible to define the dimensions and geometrical properties of individual lithological units represented in the lithological model. Ductile deformation controls also the anisotropy of rock materials and orientation of structural elements and ductile deformation structures are important precursors for the subsequent brittle deformation.

Figure 3-1. Submodels of the geological model of the Olkiluoto site area.

Lithological

Model

•Metamorphic rocks•Igneous rocks

Ductile deformation

model

Deformation textures Ductile folds Ductile shear zones

Alteration model

Rock alteration oWeathering oHydrothermal alteration •Retrograde metamorphism

Brittle deformation

model

Brittle faults

28

3) The brittle deformation model describes the products of multiple phases of brittle deformation, fault zones and other fractures. The present model shows only the localities and orientations of specific brittle fault structures .

4) The alteration model deals with products of retrograde metamorphism, hydrothermal alteration and subsequent low-temperature weathering which have affected lithological units overall in the site area. These processes transform the physical and chemical properties of rock material and altered rocks may have physical properties drastically different to those of primary, fresh rocks. Thus the degree and type of secondary alteration and retrogressive metamorphism are important parameters in evaluation of, e.g., the mechanical strength of the rocks. The goal of the alteration model is to present the shapes and volumes of altered bedrock units as well as types of altered rocks.

All these submodels are more or less interconnected and serve as basic background data for, e.g., the models of rock mechanics, hydrogeology and hydrogeochemistry.

Modelling work dealing with different thematic topics is based on the basic methods of geology and geophysics and detailed evaluation of the results of various measurements and analyses.

The goal of the lithological model is to represent spatial distribution of lithologically related bedrock units, which have properties as similar as is required from the perspective of building underground facilities. The ductile deformation model deals with elements controlling the anisotropy of rock materials and orientation of structural elements and bedrock units, in general. All the lithological units in the site area may have been affected by retrogressive metamorphism and hydrothermal alteration. The aim of the alteration model is to present the shapes, volumes and types of altered bedrock. The brittle deformation model shows the localities and orientations of certain brittle fault structures and is aimed at illustrating all the fractures created by long-term evolution of ductile deformation.

3.1 Lithological model

The methods that can be applied in lithological classification are based on indication from wholerock chemical composition, modal mineral composition, texture or larger structural features. In the case of Olkiluoto, the appropriate method for classification of metamorphic rocks is a synthesis, in which the migmatite structures, textures and modal compositions are jointly evaluated. Igneous rocks are classified on the basis of modal compositions and textures.

Methods to generate the lithological model are:

Mapping of bedrock outcrops, trenches and tunnels according to standard mapping procedures. The input data include direct observations on mineral composition, texture, grain size, migmatitic structures, structures of the ductile deformation, crosscutting relationships, etc.

29

Drill core mapping: structural and petrographic description of rock cores including sample analysis.

Geophysical methods including aeromagnetic and ground geophysical surveys.

The data from these methods are integrated to produce the 2D and 3D lithological models. The 2D lithological map or model is, thus, an interpretation, which combines the direct observations of the lithologies and structures in outcrops, investigation trenches and drill holes with the interpretation of the geophysical investigations and the tectonic structure of the area (Fig. 3-2).

Figure 3-2. Flow diagram showing the methods used to produce the 2D and 3D

lithological models.

Integration

Outcrop,

trench and

tunnel

mapping

Drill core

mapping

Aeromagnetic

survey

Magnetic

ground survey

2D lithological

model

Ductile

deformation model

3D lithological model

30

3.2 Ductile deformation model

Ductile deformation takes place in the conditions found in the middle crust, typically at least in a metamorphic environment of greenschist or amphibolite facies. This process reshapes cohesive rock materials and creates ductile deformation structures, folds, ductile faults or shear zones and various pervasive deformation textures, such as foliations and lineations.

The study in the branch of ductile deformation deals, at the first stage, with the description of geometrical and petrographical features and determination of orientation of every single deformation structure. Detailed study of outcrops, trenches and drill core samples yielded a versatile data set, in which various ductile deformation elements, the places of observation and orientations are described.

The ductile structural evolution of the Olkiluoto site involves multiple events and the chain of ductile deformation processes is commonly known as polyphase deformation. The next phase of the ductile deformation modelling procedure involves evaluation of genesis or relative stage of generation of every individual structural element. This is based on crosscutting and overprinting relations of individual products of ductile deformation (see Paulamäki & Koistinen 1991; Kärki & Paulamäki 2006). The dating of the lithologies at Olkiluoto is currently in progress and it will make it possible to date also the phases of the ductile deformation. In addition, the metamorphic environment during the deformation process controls the type and character of arising structural elements, and knowledge of this is exploited as a tool of interpretation work. This stage of interpretation work yields an understanding of the number of the individual stages in ductile deformation and character of structural sequence, in general. The final structural interpretation is a summary of knowledge obtained from first stage geometrical analysis and subsequent evaluation of dynamic evolution and cogenetic and coexistent metamorphic evolution of every individual stage of ductile structural evolution. The effects of tectonic forces and thus the consequences of ductile deformation are not homogeneously dispersed in the bedrock. As a result of this, the final structural interpretation must take into account the regional variation in the strength of every deformation process. The evaluation in strain rate variation or strain partition in a specific manner in the Olkiluoto bedrock is employed as the last tool of structural interpretation work.

3.3 Brittle deformation structures

Brittle deformation operates in significantly solidified and rigid crust at higher levels than ductile deformation. Brittle deformation is a mechanism in which the failure of rocks produces diverse fractures. Fractures are mechanical breaks showing discontinuity across their surface. In nuclear waste disposal, fractures have a crucial role in the bedrock because a part of them constitutes pathways for groundwater flow.

Fractures can be separated on the basis of their origin by using process-derived characteristic features of shear fractures (faults) and extension fractures (cracks, joints).

31

Fractures initiate and propagate when stresses become equal to and exceed the strength of the rock.

Several mechanisms are capable of producing high stresses in the crust. In the case of Olkiluoto, most significant mechanisms that have operated and produced fractures are

regional tectonic processesregional or local fluid pressure (metamorphic or magmatic) cooling of the earth's crust unloading (erosion and uplift, postglacial isostatic rebound)

Isolated fractures are rare and originated in a process, which does not leave any other marks in the bedrock. In principle, bedrock fractures and fracture systems are closely linked to each other and form an aggregate due to a common origin. But the task to relate a fracture or a fracture system to a specific process is demanding and time-consuming patchwork, especially for rocks and regions that have undergone multiple deformation events like Olkiluoto has and showing overlapping fractures or fracture systems. Multistage evolution is also obvious for the fracture systems of Olkiluoto.

Tentatively, the results of fracture mapping and the evaluation of kinematics have been analysed. On the basis of fault vector orientation, the fractures were classified into groups, the members of which have a possibility of originating from one, single event of faulting. As a first stage result, a brittle fault model is compiled to visualise plausible fault structures and their geometrical properties.

3.4 Retrogressive metamorphism and alteration

Lithological units overall in the site area may have been affected by retrogressive metamorphism and hydrothermal alteration. Alteration transforms the physical properties of rock material and alteration products may have physical properties drastically different from those of primary, fresh materials. Thus the degree and type of secondary alteration are important parameters e.g. in evaluation of the mechanical strength of the rocks.

Secondary hydrothermal alteration is associated with the late stages of metamorphism and igneous activity, which involve heated or superheated water. Two types of alteration are recognised: fracture-controlled and pervasive. The drill core samples were logged in order to determine the most typical alteration minerals or mineral assemblages and the location of the most altered sections and the length of these zones as well as to study the style and intensity of hydrothermal alteration. Until now, the geological information obtained from the state of alteration is obtained solely from visual mapping.

32

3.5 Modelling and visualisation in 3D

The basis for 3D modelling was the geological and geophysical observations in drillholes, in ONKALO rock characterisation facility and on the ground surface. The modelling principles and technique in each separate model differ to some extent. However, their primary nature is similar: they are essentially descriptive geometrical models, determining the locations, continuities, orientations and volumes of geological features. The modelling and visualisation software was Surpac® Vision (version 5.0).

3.5.1 Modelling of ductile deformation and lithology

As a result a polyphase ductile deformation together with extensive partial melting (anatexis) under high-grade metamorphic conditions (see Chapter 5), a pervasive, composite foliation and associated abundant granitic leucosome veins were produced. Both the surface and drillhole studies clearly indicate that, in the site area, the composite foliation is fairly constant over large distances, the dip direction being to the southeast. Thus, the strike and dip of the foliation has served as a guide, through which the lithologies have been correlated between the drillholes and from surface to drillholes.

The lithological modelling mainly comprises modelling of the tonalitic-granodioritic-granitic gneisses and the pegmatitic granites. In addition, the contact zone between the diatexitic gneisses and veined gneisses has been modelled, as well as the narrow diabase dykes. The veined gneisses form the main volume of the model area. The tonalitic-granodioritic-granitic gneisses have the same origin as the migmatitic gneisses, and they have, thus, gone trough the same ductile deformation phases as the migmatitic gneisses, which form the main volume of the bedrock. Consequently, the orientation of the foliation is used as the basis of the modelling of the tonalitic-granodioritic-granitic gneiss units. The pegmatitic granite veins in the outcrops, investigation trenches and in the VLJ-repository mostly follow the strike and dip of the foliation (Paulamäki 1989, Paulamäki & Koistinen 1991, Ikävalko & Äikäs 1991, Paulamäki 2005a). Although also veins cross-cutting the foliation do occur, an assumption has been made in modelling of the pegmatitic granites at depth that they are concordant (i.e. have the same dip direction and dip as the foliation) and are rather continuous. From the experience in the ONKALO access tunnel and in the investigation trenches, the mica gneisses, quartz gneisses and mafic gneisses are assumed to be just small inclusions with limited extension. Consequently, the have not been modelled but incorporated into veined gneiss, which serves as the ‘background’ in the model.

In 3D modelling of the lithologies, tonalitic-granodioritic-granitic gneiss and pegmatitic granite intersections in drillholes more than ca. 10 metres in thickness have been distinguished as separate units (Fig. 3-3). Furthermore, adjacent pegmatitic granite sections less than 10 m in length, separated by only short gneiss and migmatite sections were combined into larger units with the assumption that the gneisses represent inclusions within the pegmatitic granite. All the observed and interpreted diabase dykes have been modelled regardless of their width.

33

Figure 3-3. Tonalitic-granodioritic-granitic gneiss (orange), mica gneiss (dark blue)

and pegmatitic granite (red) sections more than 10 m in thickness in drillholes. View

from the E.

The lithological model has been constructed with the help of Surpac Vision 3D modelling software. In the modelling procedure, the simplified lithological data from drillholes OL-KR1 – OL-KR33 (Fig. 3-3) were transferred to the Surpac Vision drillhole database and the data from outcrops and investigation trenches were converted into Surpac string files. Figure 3-4 shows a N-S trending vertical section of the ONKALO area and shows how the pegmatitic granite unit were connected from the surface to the drillholes and from drillhole to another using the orientation of the foliation as a guide. The same also applies the modelling of the TGG-units.

34

Figure 3-4. N-S trending vertical section with lithological and foliation data from the

drillholes and digitised pegmatitic granite unit (magenta). The pegmatitic granite unit

on the surface (upper right corner) is connected to the drillholes using the foliation

measurements as a guide.

The lithological units were constructed by combining vertical profiles with a spacing of 50 m, occasionally 25 m, together with surface observations. The units were first digitised at one two central profiles, using the data from several drillholes, when available. These interpretations were then extrapolated to neighbouring profiles, and edited with respect to the available drillhole and surface data, and the resulting modified interpretation was extrapolated to the next profile. The result of this process was that there were several vertical profiles (Fig. 3-5a), which were then connected to a continuous unit (Fig. 3-5b). Figure 3-6a illustrates a TGG-gneiss unit that was observed at the surface and only in one drillhole. The uppermost section in the figure is the interpretation of the rock unit at the surface, based on outcrop observations. The measured dip of the foliation in the outcrop and in the drillhole resulted in the same horizontal segment being extrapolated to the observed TGG-gneiss intersection in the drillhole. The segment was further extrapolated to depth at ca. 50 m steps, and was made smaller with depth, in order to make the object geologically reasonable. The assumption regarding the extent to depth of such a rock unit is that it is approximately equal to its greatest lateral extent. Figure 3-6b shows the rock unit as a completed 3D solid, which extends to a depth of c. 200 m.

35

Figure 3-5. a) Digitised sections of the modelled pegmatitic granite unit, b) completed

3D solid object. View from up/SSE. The frame indicates the Olkiluoto site volume.

a)

b)

36

Figure 3-6. a) Construction of a TGG-gneiss unit observed at the surface and in one

drillhole. a) Interpretation on horizontal planes at about 50 m steps, b) completed solid

TGG-unit.

3.5.2 Modelling of hydrothermal alteration

The alteration model is based on macroscopic examination of the drill cores. The data were transferred to the drillhole database of Surpac Vision for 3D visualisation and modelling. Occurrences of the main components of alteration (illitisation,

OL-KR14

OL-KR7

OL-KR10OL-KR30

a)

OL-KR14

OL-KR7

OL-KR10OL-KR30

b)

37

kaolinitisation, sulphidisation) as well as the nature of alteration (fracture filling, pervasive) were considered. From the kaolinisation and sulphidisation data, volumetric models were constructed by interpolating and triangulating the bottom surfaces of the models (the tops of the models coincide with the ground surface) (Fig. 3-7a). Subsequently, triangulation was carried out between the boundary polygons of the top and bottom surfaces of both models (Fig. 3-7b).

Figure 3-7. a) The bottom surface of the sulphidisation model, b) completed volumetric

model. View from the SW. The frame indicates the Olkiluoto site volume.

Sulphides,drillhole data

Pervasive

Fracture filling

a)

Sulphides,drillhole data

Pervasive

Fracture filling

b)

38

3.5.3 Modelling of brittle deformation

The starting point for brittle deformation modelling was the observed intersections of deformation zones in the drillholes, including also their kinematic data and geophysical indications. Since the brittle fault zones (BFZ’s) were supposed to be spatially the most continuous brittle features, the modelling work was strongly focussed on them. Brittle joint zones (BJZ’s) are probably more local and lacking kinematic indications.

As described farther on in Chapter 7, statistical examination of the slickenlines revealed five separate kinematic fault groups (designated Group A – E). All these groups were modelled separately. The orientation of the modelled zone was assumed to be the same as the average orientation of the fault planes within that zone, having the same fault-slip orientation and sense-of-shear. If the same brittle fault intersection in the drillhole had two (or more) distinctly separate fault orientations each belonging to a different fault groups, two (or more) brittle fault zones were modelled to the same drillhole intersection. Drillhole intersections lacking kinematic data (brittle joint intersections) were generally not modelled. However, if there has been supporting data, brittle joint intersections could have been connected to the modelled brittle fault zones.

In the modelling work, the drillhole intersections of each fault group were viewed separately in 3D and in 2D vertical sections. Orientation of the faults is based on orientations of slickensided fractures, geophysical data and crosshole correlation. There were two different procedures to construct the fault zones:

1) Digitising in 2D sections and triangulation between the digitised polygons into 3D solids (Figs. 3-8 and 3-9)

2) Construction of the upper and lower contact planes and triangulation into 3D solids (Fig. 3-10).

39

Figure 3-8. N-S trending vertical section with two drillholes. Green labels indicate

drillhole intersections of deformation zones. Tickmarks depict orientations of the fault

plane belonging to group A. Violet lines indicate digitised deformation zones.

40

Figure 3-9. Construction of fault OL-BFZ-009, a) digitised vertical polygons, b)

completed solid. Intersection OL-KR21-BFI-20484 – 22070 (single fault plane at OL-

KR19 89.58 m). Dip direction/dip 173°/26°. View from SW.

OL-KR19

OL-KR21

a)

OL-KR19

OL-KR21

b)

41

Figure 3-10. Construction of a planar fault OL-BFZ012. a) Creation of upper and

lower contact planes, b) triangulation of the contact planes, c) triangulation between

the contact planes, d) completed solid. Intersection OL-KR27-BFI-8450-9650, Dip

direction /dip 128/53°.

The basic idea of the modelling is that the faults are planar/semiplanar features. In most cases, their continuity is difficult to estimate. However, the site area is rather densely drilled, whereupon the surrounding drillholes largely control the extent of the faults. Also, geophysical data and interpretations were used in order to orient the faults and to assess their continuity between the drillholes. In this respect, seismic VSP and mise-à-la-masse have been the most important methods. Generally, VSP and mise-à-la masse results indicate numerous gently dipping features with a dip direction to the SE-S, supporting the geological data (fracturing, foliation).

From the whole population of numerous VSP reflectors, those features actually related to observed deformation zone intersections (in single drillholes), were examined in more details. The reflector planes were extrapolated to neighbouring drillholes in order to find appropriate deformation zone intersections (within 10 meters) from them. On the basis of this cross-hole correlation, several potential VSP-based deformation zones were determined (Fig. 3-11). Later on, these zones were checked against the kinematic data.

OL-KR27 OL-KR27

OL-KR27 OL-KR27

a) b)

c) d)

42

Figure 3-11. Potential brittle deformation zones according to VSP. The frame depicts

the Olkiluoto site volume.

As presented in Chapter 2.2, an extensive mise-à-la-masse survey campaign has been done in Olkiluoto in order to determine the geometry of certain deformation zones (Lehtonen 2006). The survey reveals numerous galvanic connections between the drillholes, probably dominated by sulphide minerals. However, a portion of them is also related to deformation zone intersections. Mise-à-la-masse has been used as a supporting tool in determining the geometry of several fault zones of the present model. Specially, gently dipping and rather continuous fault zones OL-BFI098 and OL-BFI099 (see Chapter 7.2.3) are strongly based on mise-à-la-masse results.

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4 LITHOLOGICAL MODEL

4.1 Description of the lithologies

On the basis of texture, migmatite structure and major mineral composition, the rocks of Olkiluoto can be divided into two major classes: 1) high-grade metamorphic rocks including various migmatitic gneisses, tonalitic-granodioritic-granitic gneisses, mica-bearing gneisses and quartz gneisses and amphibolites and other mafic gneisses, and 2) igneous rocks including abundant pegmatitic granites and sporadic narrow diabase dykes (Kärki & Paulamäki 2006). Posiva’s nomenclature practice of the rock types is described in Mattila in press.

The migmatitic gneisses of Olkiluoto can be divided into three subgroups in terms of the type of migmatite structure: veined gneisses, stromatic gneisses and diatexitic gneisses, the last mentioned representing distinct end members in a transition system of gneisses and migmatites. The change from a texture typical of certain gneiss variants to a migmatite structure typical of a particular migmatite type takes place gradually, so that no natural borders between these end members can be defined. Thus, an artificial border between the gneisses and migmatitic gneisses has been set at 10% or 20% of the leucosome, with the name of each migmatitic gneiss determined by the dominant type of structure (Fig. 4-1).

Figure 4-1. Textural and structural end members in the migmatite - gneiss system of

Olkiluoto (Kärki & Paulamäki 2006).

44

4.1.1 Migmatitic gneisses

Migmatitic gneisses at Olkiluoto are composed mostly of a mica-rich older component, or palaeosome, which can also be called a mesosome, and a younger component, the neosome. The neosome is composed of granitic material that can also be referred to as a leucosome due to its light colour and lack of mafic minerals. The migmatitic gneisses of Olkiluoto have been defined as rocks that include more than 10 – 20% leucosome. The typical migmatites of Olkiluoto contain 20 – 40% leucosome on average, but the proportion can be less than 20% or in excess of 80% in individual samples.

Migmatites of veined gneiss-type contain elongated leucosome veins, which show a distinct linear symmetry and appear as swellings in the dykes or roundish quartz-feldspar aggregates that may be composed of augen-like structures with diameters varying between 1 and 5 cm (Fig. 4-2A). The palaeosome is often banded and can accommodate products of powerful shear deformation, e.g. asymmetric mylonitic foliation. Veined gneisses make up 43% of the drill core samples studied so far, and it is the dominating migmatite type in the central part of the Olkiluoto site.

Diatexitic gneisses include migmatites that may even contain more than 70% leucosome and in which the palaeosome occurs as fragments of different shape and size (Fig. 4-2C and D). The palaeosome fragments can be totally assimilated into granitic vein materials, or the border zones of these particles may be gradual, progressive areas of transformation, as in schollen migmatites. In general, all the migmatite variants, in which the shapes of the palaeosome and leucosome are random and which are structurally asymmetric in their entirety, have been classified into this group. Diatexitic gneisses make up 21% of the total length of the drill cores studied so far.

Stromatic gneisses represent only 0.4% of the length of the drill cores studied so far. The most characteristic feature of these stromatic migmatites is the existence of plane-like, linear leucosome dykes or layers varying in width from several millimetres to 10 – 20 cm (Fig. 4-2B). The palaeosome in these migmatites is often well foliated and shows a linear metamorphic banding or schistosity. Plate symmetry is typical of all the physical parameters of bedrock units dominated by stromatic gneisses.

45

Figure 4-2. A) Veined gneiss, B) stromatic gneiss, C) and D) diatexitic gneiss. Photos

by Seppo Paulamäki, Geological Survey of Finland.

4.1.2 Gneisses

The homogeneous, banded or only weakly migmatised gneisses include mica gneisses, mica-bearing quartz gneisses, hornblende- or pyroxene-bearing mafic gneisses and tonalitic-granodioritic-granitic gneisses. Although the more mica-rich gneisses at Olkiluoto are, in general, intensively migmatitised, fine-and medium-grained mica

gneisses with less than 10% leucosome material are also common and make up ca. 7% of the total length of the drill cores (Fig. 4-3A). The proportion of micas or their retrograde derivatives exceeds 20% in these rocks. Cordierite or its retrograde derivative pinite is a typical constituent, occurring often as large, roundish, very dark porphyroblasts ca. 5 – 10 mm in diameter. The fine-grained mica gneisses are typically schistose, but the medium-grained variants show a distinct metamorphic banding.

Fine-grained, homogeneous and typically poorly foliated quartz gneisses contain more than 60% quartz and feldspars but 20% micas at most. Certain variants may contain some amphibole and in places some pyroxene in addition to amphibole. Garnet is also typical of some quartz gneisses. The quartz gneisses compose less than 1% of the total length of the drill cores.

A B

C D

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Mafic gneisses, in which hornblende or chlorite comprises the dominant mafic mineral, occur sporadically. Some mafic gneisses may exceptionally contain some pyroxene or olivine in addition to mica and hornblende. Mafic gneisses make up less than 1% of the bedrock of Olkiluoto.

The tonalitic-granodioritic-granitic gneisses are medium-grained, relatively homogeneous rocks, which sometimes resemble plutonic, non-foliated rocks and sometimes coarse-grained mica gneisses (Fig. 4-3B). In places, they can also show a weak metamorphic banding or mylonitic foliation. The tonalitic-granodioritic-granitic gneisses form homogeneous and typically weakly fractured units. The contacts can be gradual varying in width from several tens of centimetres to several metres but they may sometimes resemble the sharp, intrusive contacts typical of igneous rocks. In places, leucosome-like granitic veins and cross-cutting pegmatitic granites comprise up to 20% of the volume of the gneisses but homogeneous rocks without any leucosome are also typical. The proportion of tonalitic-granodioritic-granitic gneisses in the drill cores studied so far is 8%.

4.1.3 Pegmatitic granites

The pegmatitic granites are typically leucocratic and very coarse-grained granitic rocks (Fig. 4-3C), which occur as dykes ranging in width from a few tens of centimetres to tens of metres, or as large, uniform intrusions. Large garnet phenocrysts, or tourmaline and cordierite grains of variable size, are in places present and mica gneiss inclusions of highly variable sizes and proportions are typical within the wider pegmatite dykes. Pegmatitic granites constitute a fairly large proportion of the bedrock of Olkiluoto, the pegmatite sections representing 20% of the total length of the drill cores studied so far.

4.1.4 Diabases

Diabases have been observed in investigation trenches OL-TK3 and OL-TK8, the shallow drillhole OL-23 and the deep drillhole OL-KR6 and in the construction site of the OL3 power plant (Paulamäki 1989, Gehör et al. 2001; Lindberg & Paulamäki 2004; Engström 2006; Talikka 2005). The diabases appear as very narrow dykes, of widths varying from 5 to 50 cm, and they are typically blackish, dense and fine-grained (Fig. 4-3D). The contacts of the dykes are very sharp but without chilled margins. The diabases contain quartz- and carbonate-filled amygdales, 0.1- 0.3 mm to ca. 2 mm in diameter. All the microscopically examined diabases have been thoroughly altered, the original mafic minerals being replaced by microcrystalline saussurite (epidote, calcite and sericite), and the plagioclase has recrystallised into pure albite. Plagioclase is visible in 1 – 2 mm long plate-like crystals, making the texture similar to the ophitic texture of diabases. The geochemical, petrological and U-Pb age data of the dyke in OL-TK3 (Mänttäri et al. 2005) indicate that the Olkiluoto diabase dykes are probably Mesoproterozoic (ca. 1600 Ma) in age.

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Figure 4-3. A) Mica gneiss, B) tonalitic-granodioritic-granitic gneiss, C) pegmatitic

granite, D) diabase dyke. Photos by Seppo Paulamäki (A, B, C) and Jon Engström (D),

Geological Survey of Finland.

4.2 Whole rock chemistry and petrography

Based on whole-rock chemical analyses, the supracrustal rocks of Olkiluoto can be divided into four distinct series: the T series, S series, P series and basic, volcanogenic gneisses (Fig. 4-4) (Kärki & Paulamäki 2006). In addition, pegmatitic granites and diabases form groups of their own that can be identified both macroscopically and chemically. The identification of the members of the different series is mostly based on the concentrations of phosphorus and calcium, their mutual ratios and their ratios to other elements. Ternary plots of calcium (Ca), phosphorus (P) and aluminium (Al) or titanium (Ti) provide one basis for classification, as the members of the P series are enriched in phosphorus and the members of the S series in calcium (Fig. 4-4). Differences are also visible in variation diagrams, which show the element oxide concentrations versus that of SiO2. Rocks of the T, S and P series are estimated to make up 42-46%, 7-12% and 26-28%, respectively, of the volume of central part of the island of Olkiluoto and the various pegmatitic granites about 20%.

A B

C D

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Figure 4-4. Classification of the lithologies of Olkiluoto on the basis of whole-rock

chemical analysis. Blue = T-series, orange = S-series, violet = P-series, red =

pegmatitic granite, green = basic metavolcanic rock, black = diabase and + =

penetratively altered gneiss or migmatite (Kärki & Paulamäki 2006).

4.2.1 The T series

The rocks of the T series constitute a transition series, in which the end members are often cordierite-bearing mica gneisses, veined gneisses and diatexitic gneisses with less than 60% SiO2, and quartz gneisses, in which the SiO2 content exceeds 75%. Cordierite is totally absent from the quartz gneisses of this series. The members of the T series are assumed to be derivatives of turbidite-type sedimentary materials, and the above end members have been presumed to represent clay mineral-rich pelitic materials and greywacke-type impure sandstones. The most typical mineral assemblages for the migmatites and mica gneisses of the series include quartz, plagioclase, K-feldspar, cordierite and sillimanite.

The granitic tonalitic-granodioritic-granitic gneisses belonging to the T series are often richer in aluminium and alkalis, and their titanium, iron and magnesium concentrations are lower than in typical T-series migmatites and gneisses with similar SiO2 contents. The differences in chemical composition are most probably caused by metasomatic alteration, which may have affected the content of every major element.

CaO P2O5*10

Al2O3/5

T Series

S Series

P Series

49

Trace element concentrations are very close to the average composition of the upper crust in every member of the T –series, and the variations in composition between the samples in the series are insignificant.

4.2.2 The S series

The members of the S series are quartz gneisses, mica gneisses, and mafic gneisses and rarely migmatitic gneisses. They typically occur as homogeneous, often fine-grained gneiss layers, and concretions or roundish budins differing in composition from the host rock. The most essential difference between these and the members of the other series is their high calcium concentration, which typically exceeds 2%, the maximum concentrations being over 13%. A relatively low alkali contents and high manganese content are also typical. In terms of silicity and calcium content, the S-type gneisses have been classified into low-Ca, high-Ca and mafic gneiss subgroups. The characteristic mineral assemblage for the low-Ca subgroup is quartz, plagioclase and biotite, with or without hornblende and garnet. The members of the high-Ca subgroup are mostly quartzitic and composed of quartz, plagioclase, hornblende, garnet and sporadically pyroxene. A typical paragenesis for the S-type mafic gneisses is hornblende, plagioclase, quartz, biotite and sometimes pyroxene.

The members of the S series are assumed to have originated from calcareous sedimentary materials or have been affected by other processes that produced these skarn-type formations. The similarity in trace element concentrations between the members of the T and S series supports the interpretation that the high-Ca and low-Ca S-type gneisses may be calcium-enriched derivatives of the T series gneisses. The trace element ratios of the mafic S-type gneisses, however, indicate a volcanism-related process that has added magnesium and iron to the material mixture.

4.2.3 The P series

The P series is largely composed of tonalitic-granodioritic-granitic gneisses, although some of the veined gneisses, diatexitic gneisses, mica gneisses and mafic gneisses also belong to this series. The members of the P series are characterised by their P2O5

concentrations that exceed 0.3%, whereas the members of other series contain less than 0.2% P2O5. Another characteristic feature of the P series is the comparatively high calcium concentration, which is mostly between the T and S series.

Within the P-type tonalitic-granodioritic-granitic gneisses, the SiO2 content varies between 55 and 70%, and the P2O5 concentrations decrease from 1.2% in the most basic members to below 0.3% in the most silicic members. Similarly, the CaO concentration decreases from 6% to less than 2%. The characteristic mineral sequence is plagioclase, quartz, biotite, K-feldspar and apatite. The typical mineral sequence of the P-type mafic gneisses comprise plagioclase, hornblende, biotite and quartz, with apatite and some sphene. In the mafic gneisses, the P2O5 concentration decreases from 3.5 to 1% and the CaO from 15 to 5% as the concentration of SiO2 increases from 42 to 52%. The

50

characteristic mineral paragenesis of the P-type mica gneisses and migmatitic gneisses is plagioclase, quartz, biotite and apatite. Their SiO2 content is in the range 55 - 65% and the P2O5 concentration decreases linearly from 1.2% in the most basic members to less than 0.4% in the most silicic variants. Similarly the CaO concentration decreases from 6 to 2%.

The comparison of the chemical compositions of the different series indicate that the origin of the protolith for the P-type gneisses most likely include mixing of the volcanic and turbiditic components and subsequent physical and chemical enrichment processes. The final product was presumably affected by a rather high degree of metamorphism and some kind of metasomatism, especially in the case of the P-type tonalitic-granodioritic-granitic gneisses.

4.2.4 Mafic and ultramafic metavolcanics

The mafic or ultramafic, probably volcanogenic gneisses from drill holes OL-KR13 and OL-KR17 possibly come from the same layer or layers. The mineral composition of one type of mafic gneiss is amphibole, phlogopitic biotite, olivine and apatite, whereas another type is composed for the most part of amphibole and biotite. Chemically they resemble the mafic gneisses of the P series in many respects, but they are not identical. The alkalis vs. SiO2 ratios of these gneisses show a clear similarity to those of basalts, and in some cases picrites or picritic basalts. The same tendency is visible in the trace element concentrations. Also the characteristically high concentrations of MgO, TiO2

and P2O5 are similar to those found in high-magnesium basalts, picrobasalts and picrites. The chemical similarity between these picrite-type metavolcanic rocks and the mafic gneisses of the P series indicate that this volcanogenic material most probably yielded one component to the source material for the P-type protolith.

4.2.5 Pegmatitic granites

Pegmatitic granites at Olkiluoto are typically very coarse-grained leucocratic rocks, which may contain various amounts of inclusions, composing of all kinds of gneisses and migmatitic gneisses found at Olkiluoto. Restite particles, mostly biotite-rich schlieren, indicate the assimilation of the gneisses into pegmatitic granites. Consequently, the proportion of assimilated materials has a great impact on the total composition of the pegmatitic granites.

The only consistent chemical properties of the pegmatitic granites are high silica content and a pronounced peraluminous character. Chemically, all the pegmatitic granites are highly acidic granitoids with SiO2 content between 70 and 80% and a total alkali content between 4 and 12%. The total alkali - silica ratios of the pegmatites are similar to those of rhyolitic extrusive rocks and the trace element ratios indicate generation in a volcanic arc environment. Leucogranites of this kind have mostly been thought to be generated by partial melting of metasedimentary rocks as a result of isothermal decompression in the late stage of orogeny (e.g., England et al. 1984), and this

51

interpretation is most probably valid also in the case of the Olkiluoto pegmatitic granites.

4.3 Metamorphic mineral assemblages and secondary alteration products

The gneisses and migmatites of Olkiluoto represent relatively high-grade metamorphic derivatives of different, mostly supracrustal materials (Kärki & Paulamäki 2006). The mineral assemblage of T-type gneisses is typical of metapelites of the cordierite-biotite-sillimanite-K-feldspar zone of prograde metamorphism. The temperature in such an environment would have exceeded 620 - 700oC. The presence of sillimanite in the metapelites and sphene in the mafic gneisses limits the possible pressure range to between ca. 3.5 and 5.5 kbar (Frost et al. 2000). Consequently, the peak metamorphic conditions for the Olkiluoto gneisses represent the uppermost amphibolite facies. H2O-fluxed melting, near-isothermal decompression and dehydration melting are the processes that may have caused the melting of pelitic and greywacke-type materials under the conditions indicated by the metamorphic mineral assemblages typical of Olkiluoto (Kärki & Paulamäki 2006). The temperature capable of producing the migmatite structures and metamorphic mineral assemblages found at Olkiluoto is estimated to be ca. 650 – 700oC, representing the conditions of the highest amphibolite facies at pressures of ca. 3 – 4 kbars.

The similarity in chemical composition between homogeneous gneiss relicts and the corresponding migmatitic gneisses, which can contain up to 40 – 50% leucosome, support an isochemical character for the migmatisation process. The loss of anatectic melt from the migmatite system is, thus, minimal. Subsequent injection of granitic magmas from an external source is however possible, and most probably at least some of the largest pegmatitic granites of Olkiluoto have originated in that way.

The chloritisation of biotite, pinitisation of cordierite and saussuritisation of plagioclase and amphiboles are common processes in the retrograde evolution of migmatites of the kind found at Olkiluoto, representing products equilibrated under conditions of lower-grade metamorphism. Subsequent evolution at fairly low temperatures has drastically affected the mineral composition of the gneisses in certain subareas. One consequence of this alteration is visible in the mineral composition of the diabases (see Chapter4.1.4). The first retrograde mineral phases may be the results of crystallisation of the residual melt, which will exsolve H2O, leading after the peak in metamorphism to a reaction between k-feldspar, sillimanite and water-producing muscovite and quartz (Brown 2002). Analogous reaction model is also possible for the chloritisation of biotite.

Subsequent retrograde metamorphism and alteration under low temperature conditions took place simultaneously with the brittle deformation. These processes produced the brittle faults and fractures, but also again affected the mineral composition of the bedrock. These events are evident today as zones of abundant fracturing and low-temperature mineral assemblages, in which the high-grade mineral phases have been

52

replaced by, for instance, illite or kaolinite. The intrusion of rapakivi granites ca. 1583 Ma ago and olivine diabase dykes ca. 1270 – 1250 Ma ago markedly increased the hydrothermal activity and intensity of low-temperature alteration. Moreover, the period from the intrusion of the olivine diabases to the present represents the longest individual stage in the evolution of the Olkiluoto bedrock and will certainly have had a distinguishable impact on its properties.

4.4 Two-dimensional lithological model

The bedrock map of Olkiluoto presented in Vaittinen et al. (2003) has been revised on the basis of new drill holes and drill core sample studies, and new trench and outcrop mapping described in Chapter 2 (Fig. 4-5). Some of the lithological and tectonic observations made in 1988 (Paulamäki 1989) and 1991 (Paulamäki & Koistinen 1991) were re-interpreted. Additionally, two field excursions were made to check the new interpretations. The new ground survey magnetic map of the eastern part of the island and the reprocessed magnetic map of the central investigation area have also been utilised.

Figure 4-5. Lithological map Olkiluoto. The Olkiluoto site area is marked with a black box.

53

54

4.5 Three-dimensional lithological model

The basic idea behind the 3D interpretation of the lithologies is described in Chapter 3-7. The 3D lithological model is composed of 17 units of tonalitic-granodioritic-graniticgneisses, 35 units of pegmatitic granite, one diatexitic gneiss unit and six diabase dykes. The veined gneisses form the main volume of the model area and serves as the ‘background’ in the model. The modelled tonalitic-granodioritic-granitic gneiss, pegmatitic granite and diabase units are designated TGG+number, PGR+number and DB+number, respectively.

Figure 4-6 shows a vertical section in N-S direction from the central part of the site area presenting the modelled lithologies.

Figure 4-6. Vertical section in N-S direction along the coordinate line y = 1525600.

View from the E.

4.5.1 Diatexitic gneiss/veined gneiss contact zone

The NW transitional contact between the diatexitic gneiss and the veined gneiss has been constructed on the basis of the distribution of the lithologies in drillholes OL-KR4, OL-KR8, OL-KR22, OL-KR23, OL-KR24, OL-KR25, OL-KR26, OL-KR27, OL-KR28 and OL-KR31 and the tectonic observations therein. The contact zone is suggested to be due to thrust related deformation. During D3 deformation (see Chapter 5) diatexitic gneisses have been thrusted from the southeast upon the veined gneisses (Figs.4-7 and 4-8).

Pegmatitic granite

Diabase

Diatexitic gneiss

TGG gneiss

Veined gneiss

LEGEND

55

Figure 4-7. Diatexitic gneiss unit. View from the NW. The black frame indicates the

Olkiluoto site volume.

Figure 4-8. Diatexitic gneiss unit. View from the NE. The black frame indicates the

Olkiluoto site volume.

4.5.2 Tonalitic-granodioritic-granitic gneiss units (TGG1 – TGG17)

The interpreted tonalitic-granodioritic-granitic gneiss (TGG gneiss) units in 3D are shown in Figs. 4-9 and 4-10.The TGG gneiss unit TGG1 is present at the surface in outcrops and in investigation trenches TK1, TK5, TK6 and TK7 (Paulamäki 1995, Paulamäki 2005b, Paulamäki & Aaltonen 2005). It has been connected to the TGG-gneiss sections at 15 – 31 m in drillhole OL-KR8, at 5-7 m in OL-KR26, at 0-34 m in OL-KR28 and 16-33 m in ONK-PH1 (Table 4-1).

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The TGG gneiss intersection at 210-252.5 m in drillhole OL-KR8 has been modelled as unit TGG2. The alignment of the unit is based on the foliation measurements, which indicate gentle (ca. 30°) dip to the SE.

The TGG gneiss intersections in investigation trench TK4 in mapping sections P43-P45 and in drillhole OL-KR30 at 4.20-27.65 m have been connected to form unit TGG5. The foliation measurements in the trench and in the drillhole results as a rock body dipping gently to the SSE.

Unit TGG7 outcrops about 250 m north of drillhole KR2. It has been connected to the drillhole sections 297 - 398 m in drillhole OL-KR2, 271 - 410 m in OL-KR13, 406 - 495 m in OL-KR12, 373 - 441 m in OL-KR14 and 360-396 m in OL-KR15 (Table 4-1). The interpretation results in a TGG unit dipping moderately to gently southwards, the dip becoming gentler at depth. This attitude is supported by foliation measurements in outcrops and in drill core samples. The maximum depth of the lower edge of TGG7 is about 450 m, since no TGG gneisses are present in drillhole OL-KR10.

Unit TGG13 has been observed in outcrops, in investigation trench OL-TK3 and in drillhole OL-KR21 at 82-111 m. The foliation measurements indicate moderate to gentle dip to the south. The occurrence of the unit in drillhole OL-KR5 is uncertain, since the first 40 m of the drill core sample is missing.

Two conformable units of the TGG gneisses, TGG15 and TGG16, are present in the northwestern part of Olkiluoto. The gneiss sections in drillhole OL-KR5 at 171 – 240 m, in OL-KR20 at 251 - 359 m and in OL-KR33 at 143-267 m have been modelled to unit TGG15. Unit TGG16 has been connected to the gneiss intersection in drillhole OL-KR5 at 342 - 386 m. The outcrop and trench (OL-TK9) observations combined with drillhole sections result in a moderate to gentle dip in both of the units, corresponding well with the foliation measurements both in outcrops and in drill core samples. The units do not extend deeper than about 450 m, because no TGG gneisses have been penetrated in drillhole OL-KR1 at that depth. In its western part, the depth of unit TGG15 is 250 - 300 m according to drillhole intersections (Äikäs 1986).

TGG gneisses in drillholes OL-KR1 at 935 - 946 m, OL-KR2 at 827 - 843 m and 937 - 953 m and OL-KR11 at 977 - 1002 m have been modelled as being parts of a probable large-scale overturned fold structure (TGG17). The unit does not outcrop.

No drillholes intersect TGG gneiss units TGG3, TGG4, TGG6, TGG8, TGG9, TGG10, TGG11, TGG12 and TGG14. The modelling of these units is based on foliation measurements on the outcrops. The extension of the units at depth is uncertain. However, in the case of units TGG3 and TGG4, their maximum extension is no more than 200 and 100 m, respectively, because they cannot be found in the nearby drillholes OL-KR9 and OL-KR29.

Table 4-1. Occurrence of modelled tonalitic-granodioritic-granitic gneiss units in drillholes OL-KR1 – OL-KR33.

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TGG1 TGG2 TGG5 TGG7 TGG13 TGG15 TGG16 TGG17OL-KR1 935.3-946.0OL-KR2 297.1-398.5 827.15-843.36

937.3-953.6OL-KR3OL-KR4OL-KR5 171.5-240.05 342.05-385.9OL-KR6OL-KR7OL-KR8 15.45-30.8 210.2-252.5OL-KR9OL-KR10OL-KR11 989.4-1002.11OL-KR12 406.65-495.4OL-KR13 275.2-410.0OL-KR14 373.3-441.4OL-KR15 360.0-396.0OL-KR16OL-KR17OL-KR18OL-KR19OL-KR20 251.4-279.0

286.7-359.2OL-KR21 82.4-111.2OL-KR22OL-KR23OL-KR24OL-KR25OL-KR26 4.8-7.3OL-KR27OL-KR28 0.3-34.2OL-KR29OL-KR30 4.2-27.65OL-KR31OL-KR32OL-KR33 143.05-266.5ONK-PH1 16.24-32.89OUTCROP + - + + + + + -

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Figure 4-9. Modelled tonalitic-granodioritic-granitic gneiss units. View from the SW.

The black frame indicates the Olkiluoto site volume.

Figure 4-10. Modelled tonalitic-granodioritic-granitic gneiss units. View from the SE.

The black frame indicates the Olkiluoto site volume.

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4.5.3 Pegmatitic granite units (PGR1-PGR36)

Massive, coarse-grained, reddish or pale-coloured pegmatitic granites are abundant in the site area, both at the surface and in drillholes. The outcrops have shown that the pegmatitic granites are very heterogeneous rocks containing numerous inclusions and granitised restites of different gneisses and migmatites. The pegmatitic granite sections in drillholes are even more heterogeneous, since the modelled pegmatitic granite units are partly assembled so that several nearby sections, a few metres in length, separated by short sections of gneisses and migmatites, have been combined into larger units.

The drillhole intersections of the modelled pegmatitic granite units are listed in Tables 4-2 and 4-3. The modelled pegmatitic granite units are presented in Figs. 4-11 and 4-12.

Pegmatitic granite units PGR2, PGR5, PGR6, PGR13, PGR14, PGR15, PGR16, PGR18, PGR19, PGR20 and PGR24 occur both at the surface and in drillholes. Unit PGR2 is only exposed in mapping sections P21-P24 in investigation trench OL-TK8. Otherwise it is determined on the basis of drillholes. The unit is connected to pegmatitic granite intersections in the drillholes OL-KR1, OL-KR2, OL-KR4, OL-KR10, OL-KR12, OL-KR13, Ol-KR14, OL-KR15, OL-KR24, OL-KR25, OL-KR28 and OL-KR32 (Tables 4-2 and 4-3).

The pegmatitic granite unit PGR5 is visible in outcrops and in investigation trench OL-TK3, as well as in drillholes OL-KR20, OL-KR21 and OL-KR33. In the outcrops and in the trench, the pegmatitic granite is quite uniform and homogeneous, containing only a few small mica gneiss restites.

The large pegmatitic granite in the middle of the site area is divided into two separate units PGR6 and PGR19. On the basis of investigation trench OL-TK2, both of the units contains considerable amounts of migmatitic gneisses. Unit PGR19 is connected to pegmatitic granite intersections in drillholes OL-KR1, OL-KR3, OL-KR10, OL-KR7, OL-KR12 and OL-KR14 – OL-KR18. No drillholes intersect unit PGR6.

Pegmatitic granite dyke in mapping section P51 in trench OL-TK4 with oriented and unoriented aggregates of strongly altered biotite (Paulamäki 2005a) is connected to the pegmatitic granite intersected by the shallow drillhole OL-14. The lower and upper contacts of the dyke are in OL-TK4 are 150/45° and 145/50°, respectively. The resulting pegmatitic granite unit PGR20 is further connected to the pegmatitic granite section at 130.85-140.90 m in drillhole OL-KR25.

The pegmatitic granite unit PGR24 is present in investigation trench OL-TK2 and it has been connected to the pegmatite section at 88 - 117 m in drillhole OL-KR7.

Pegmatitic granite units PGR25 and PGR26 are not exposed but their surface expressions are determined on the basis of pegmatite sections in drillhole OL-KR11, assuming that they follow the trend and dip of the foliation. The former unit is supported by observations in a shallow drill hole OL-11, which entirely consists of pegmatite (Suomen Malmi 1989).

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Pegmatitic granite units PGR1, PGR8 - PGR9, PGR11, PG13 - PG18, PGR21, PGR23 and PGR27-PGR33 are only present in drillholes (Tables 4-2 and 4-3) and due to their gentle dip to the south or southeast are not exposed at the surface. Their occurrence seems to be restricted to the central part of the site area, since drillholes OL-KR5, OL-KR6 and OL-KR19 in the northern part are lacking in significant granite pegmatite sections at the relevant depths. This assumption is supported by the outcrop observations, which indicate that most of the pegmatitic granites are located in the central part of the site area.

No drillholes intersect pegmatitic granite units PGR6, PGR12, PGR13, PGR17, PGR34 and PGR36.

Table 4-2. Occurrence of modelled major granite pegmatite units PGR1-PGR20 in drillholes OL-KR1 – OL-KR33.

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PGR1 PGR2 PGR5 PGR6 PGR8 PGR9 PGR11 PGR14 PGR15 PGR16 PGR18 PGR19 PGR20OL-KR1 169-199.4 441.9-488.95 0.0-38.4

OL-KR2139.85-174.8 421.3-455.9

OL-KR3 0.0-43.7OL-KR4 464.5-483.2 769.65-807.0 815.8-866.4OL-KR5 0.0-9.0OL-KR6OL-KR7 213.8-225.4 653.0-723.3 9.8-14.8 258.6-285.95OL-KR8 565.4-600.59OL-KR9 352.8-370.1 304.1-328.4OL-KR10 336.85-364.95 0.0-17.63 128.7-136.1 202.6-246.6 OL-KR11OL-KR12 208.1-225.3 509.7-567.1 0.0-57.0OL-KR13 68.05-150.6OL-KR14 282.7-311.1 485.7-508.85 14.15-22.2 95.35-153.65OL-KR15 292.7-306.4 479.0-505.0 39.9-88.78OL-KR16 58.75-117.75OL-KR17 30.0-45.3OL-KR18 58.4-79.0OL-KR19OL-KR20 73.5-87.6

144.15-162.95374.8-400.0?

OL-KR21 2.95-19.3 57.2-82.4

OL-KR22OL-KR23OL-KR24 539.3-548.05 130.85-140.9OL-KR25 437.95-462.45OL-KR26OL-KR27 421.1-440.3OL-KR28 520.8-559.87OL-KR29OL-KR30 27.65-37.9OL-KR31OL-KR32 104.5-116.95OL-KR33 13.35-29.05OUTCROP - + + + - - - + + + + + +

Table 4-3. Occurrence of modelled major granite pegmatite units PGR21-PGR32 in drillholes OL-KR1 – OL-KR33.

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PGR21 PGR22 PGR23 PGR24 PGR25 PGR26 PGR27 PGR28 PGR29 PGR30 PGR31 PGR32OL-KR1 961.6-976.55

1000.8-1012.9336.6-348.1

OL-KR2 742.9-758.75 768.5-815.1

858.45-878.5 909.5-937.3 238.3-245.9

OL-KR3OL-KR4 589.65-606.65OL-KR5OL-KR6OL-KR7 105.5-117.3OL-KR8OL-KR9 551.8-560.85OL-KR10 537.8-544.55OL-KR11 825.1-848.72 305.37-330.35 180.2-192.05 860.05-881.75OL-KR12OL-KR13OL-KR14 354.5-368.3OL-KR15 357-367OL-KR16OL-KR17OL-KR18OL-KR19OL-KR20 181.7-199.7

OL-KR21

OL-KR22OL-KR23OL-KR24OL-KR25OL-KR26OL-KR27OL-KR28OL-KR29OL-KR30OL-KR31OL-KR32OL-KR33OUTCROP - - - + - - - - - - - -

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Figure 4-11. Modelled pegmatitic granite unit. View from the SW. The black frame

indicates the Olkiluoto site volume.

Figure 4-12. Modelled pegmatitic granite units. View from the SE. The black frame

indicates the Olkiluoto site volume.

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4.5.4 Diabase dykes (DB1-DB6)

Four approximately E-W trending magnetic anomalies interpreted as diabase dykes occur north and northeast of drillholes OL-KR5 and OL-KR6 (Vaittinen et al. 2001). Two of these anomalies have recently been confirmed to be diabase dykes. The dykes occur in the northern part of investigation trench OL-TK8 in sections P72-P73 (DB1) and P138-P139 (DB2) (Engström 2006). The dykes DB1 and DB2 are approximately 2.5 m wide with a dip direction/dip of 351/82° and 343/70°, respectively. The magnetic anomalies north of drillhole OL-KR5 and northeast of drillhole OL-KR6 have no surface exposures but compared to the confirmed anomalies, it is most likely that they also indicate diabase dykes. In this model they have been modelled as a diabase dyke DB3 and DB4, respectively. DB3 may be present in drillhole OL-KR6 at 393.7 - 395.8 m and 398.6 - 399.5 m. The dyke in trench OL-TK3 (DB4) is ca. 60 cm wide, has sharp contacts with the country rock and dips 55° to the NW (Lindberg & Paulamäki 2004). A similar diabase dyke observed in shallow drillhole OL-23 (DB5) is interpreted on the basis of ground geophysical data as dipping 65 - 75° to the NW or NNW (Paananen & Kurimo 1990, Vaittinen et al. 2001). The modelled diabase dykes are shown in Fig. 4-13.

Figure 4-13. Modelled diabase dykes. View from the SW. The black frame indicates the

Olkiluoto site volume.

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4.6 Correlation to lithology in southern Satakunta

Olkiluoto is located within a bedrock area, covering approximately 800 million years of geological history of the Precambrian Fennoscandian Shield (Fig. 4-14). The oldest part of the bedrock is composed of supracrustal, metasedimentary and metavolcanic rocks deformed and metamorphosed during the Palaeoproterozoic Svecokarelian orogeny ca. 1900 - 1800 million years ago. They are mostly migmatitised, high-grade metamorphic mica gneisses, containing cordierite, sillimanite or garnet porphyroblasts (Suominen et al. 1997, Veräjämäki 1998). Amphibolites, uralite porphyrites and hornblende gneisses, which were originally mafic and intermediate volcanics, occasionally occur as narrow interlayers in the supracrustal sequences. Plutonic rocks consisting of trondhjemites, tonalites, granodiorites, coarse-grained granites and pegmatites intrude the migmatites (Pietikäinen 1994, Suominen et al. 1997, Veräjämäki 1998). Except for a few small bodies, more mafic intrusive rocks, gabbros and diorites, are encountered only as small xenoliths.

Large parts of the southern Satakunta area are composed of the Mesoproterozoic, anorogenic Laitila rapakivi batholith, 1583 million years in age (Vorma 1976, Vaasjoki 1996). The Eurajoki rapakivi stock, which is a satellite massif to this batholith, is located only about 5 km east of Olkiluoto and can be divided into the marginal hornblende-bearing Tarkki granite and the younger, central Väkkärä granite (Haapala 1977), both of which are somewhat younger than the Laitila batholith.

The margin of the Satakunta sandstone formation, at least 1400 - 1300 million years in age, is located ca. 12 km NE of Olkiluoto. It was deposited fluvially in a deltaic environment and has been preserved in a NW-SE trending graben structure (Kohonen et al. 1993). It is cut by olivine diabase dykes 1270 - 1250 million years in age (Suominen 1991). Lake Sääksjärvi, ca. 50 km NE of Olkiluoto, is situated in an impact crater of early Cambrian age.

Figure 4-14. Regional geology of Olkiluoto. The lithology of the Olkiluoto area is shown in the upper left corner.

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67

4.7 Correlation to previous bedrock model

The lithological model in the previous bedrock model (Vaittinen et al. 2003) was constructed in co-operation between the members of the present Geological Modelling Task Force from the GTK, VTT and Kivitieto Oy. The basic idea of interpreting the geometry of the lithological units in 3D is the same in both models (see chapter 3.7). As now, lithological model in bedrock model 2003/1 was compiled using the Surpac®

Vision 3D modelling software. The completed objects of different rock types were then transferred to the ROCK-CAD modelling system in Fintact Oy.

The most striking difference between the two models is that the practice for naming rock types in the present model is different from that presented in the previous bedrock model. The nomenclature of the rock types in that model and the comparable names of the present model are presented in Table 4-4.

Table 4-4. Comparison of the nomenclature of the rock types in the previous bedrock

model 2003/1 and the Olkiluoto site area model v.0.

Bedrock model 2003/1 Olkiluoto site area model, v.0

Veined migmatite Veined gneiss Dyke migmatite Stromatic migmatite Mica gneiss migmatite Diatexitic gneiss Grey gneiss Tonalitic-granodioritic-granitic gneiss Mica gneiss Mica gneiss Quartz-feldspar gneiss Quartz gneiss Mafic gneiss Mafic gneiss Granite pegmatite Pegmatitic granite Diabase Diabase

The lithological model in the previous bedrock model consists of 24 pegmatitic granite units, 15 tonalitic-granodioritic-granitic gneiss units and one diabase dyke. In the model, all the different migmatite types were incorporated in to one single unit, the migmatitic mica gneisses, which form the main volume in the model. In the present model, the migmatitic gneisses are divided into veined gneisses and diatexitic gneisses, the former forming the main volume of the rock. As before, the different non-migmatitic gneisses, except the tonalitic-granodioritic-granitic gneisses, have been included in the veined gneisses. The present model consists of one diatexitic gneiss unit, 17 units of tonalitic-granodioritic-granitic gneisses, 35 pegmatitic granite units and six diabase dykes. Almost all the units, which were modelled in the previous bedrock model, are also included in this model. In general, only minor adjustments have been necessary to their location, form and continuation at depth and at the surface on the basis of new drillhole, tunnel and trench data. The clearest difference between the two models is that the continuous pegmatitic granite unit PG1 in the previous bedrock model has in the present model been divided into three separate units PGR1, PGR2 and PGR5.

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4.8 Correlation to ONKALO area model version 0

The ONKALO area is a part of the Olkiluoto site area and the lithological model presented in Paananen et al. 2006 is, therefore, a part of the lithological model described in the present report. The ONKALO area model includes one diatexitic gneiss unit, seven tonalitic-granodioritic-granitic gneiss units and 22 pegmatitic granitic units, all of which are included in the present model.

4.9 Evaluation of implications for construction

Different rock types have different implications for construction and the main features, which seem to control the constructional properties of the rock mass are anisotropy and heterogeneity. Migmatitic gneisses, especially stromatic and veined gneisses have usually well developed foliation which controls the orientation of fractures and the formation of weakness planes. Stromatic gneisses have strongly developed planar symmetry, which may result in the detachment of sheets of rock if the tunnel is unfavourably oriented in relation to the foliation. For example, subhorizontal foliation in stromatic gneiss may greatly increase the possibility of formation of dropping blocks and, consequently, rock re-enforcement is needed. Considering the construction, the most favourable circumstance would be if the tunnel intersected the foliation planes of stromatic gneisses perpendicular.

Veined gneisses show more asymmetry than stromatic gneisses, but still the orientation of the foliation is important regarding constructional properties. Therefore, veined gneisses are likely to have similar implications as stromatic gneisses, but where the amount of leucosome is higher and the intensity of foliation is lower, these properties are greatly reduced.

Diatexitic gneisses have a high proportion of leucosome and the type of foliation in diatexitic gneisses is mostly irregular or massive; therefore, the amount of possible planes of weaknesses, which may cause the formation of dropping blocks, is quite low. Accordingly, the implications for construction of diatexitic gneisses are considered quite small.

Gneisses are more isotropic than the migmatitic gneisses and as a consequence the effect of foliation in these rock types is minimal. Gneisses usually have quite low fracture density, but typically three different fracture orientations dominate in these rock types and the formation of blocks of different dimensions is possible. Therefore extra rock re-enforcement may be required. A typical example of this is the fracturing in mica and quartzitic gneisses – these are most commonly just small inclusions occurring conformable to the foliation but occasionally these exist as larger inclusions with a diameter of several metres. These inclusions typically have three well-developed fracture sets with sub-orthogonal orientations. Accordingly, the formation of cubic blocks is probable within these inclusions.

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5 DUCTILE DEFORMATION MODEL

Ductile deformation is a physical process that reshapes cohesive rock materials and rearranges bedrock units affected by tectonic forces in compressional or tensional stress fields. Ductile deformation is possible in the middle crust typically at least 5 – 10 km below the upper surface of the lithosphere or continental crust. The bedrock of Olkiluoto belongs to the Svecofennian domain of Southern Finland, which was deformed in a ductile manner during the Svecokarelian (Gaál 1982) or Svecofennian (e.g. Gaál & Gorbatsvhev 1987; Nironen 1997) Orogeny ca. 1.91 – 1.80 Ga ago. The deformation process is an irreversible change in the shape and/or volume of a bedrock unit that has been stressed beyond its elastic limit. Folds and ductile shear structures associated with various penetrative foliations, such as metamorphic bandings, schistosities and ductile fault rocks, are characteristic products of that process. The bedrock of Olkiluoto conceals a manifold collection of various ductile deformation structures ranging from microscopic foliations to large-scale folds and ductile shear structures. The goal of the work is to generate two- and three-dimensional descriptions of ductile deformation structures. The tools exploited in this work are described in the previous chapter.

5.1 Description of the ductile deformation

The Palaeoproterozoic bedrock of Olkiluoto has been affected by five stages of ductile deformation, as determined on the basis of refolding and cross-cutting relations (Paulamäki & Koistinen 1991; Aaltonen 2005). Subsequently, after the last cooling below ca. 300 - 400oC, the domain was affected by several events of semi-ductile and brittle deformation and the study site is penetrated by numerous faults, which sheared and crushed the bedrock and increased its structural complexity. Bedrock anisotropy was caused by ductile deformation and that, as well as the border zones between bedrock units of different rheology, controlled the subsequent geological evolution.

The lithological layering (S0) and the slightly segregated foliation S1 of deformation phase D1 (Fig. 5-1a) mostly (sub)parallel to S0 are the oldest observed structural elements at the site. Structures of this category have been detected only sporadically at the hinges of isoclinal, intrafolial folds thus making it difficult to evaluate the exact significance of the earliest deformational events.

Subsequent deformation phase D2 is characterised by intense thrust-related folding and leucosome production. At this stage tight or isoclinal F2 folds were produced into originally subhorizontal orientation (Paulamäki & Koistinen 1991). Penetrative axial plane foliation, schistosity or metamorphic banding S2 can be separated from S1

foliation at the hinges of certain F2 folds (Fig. 5-1a). These early structures have more or less been overprinted by the later deformations and well-preserved, original D2

structures may occur in more competent units within the migmatite complex. However, several subdomains in the Olkiluoto site preserved in spite of the later deformations and D2 is estimated to be the most important structural factor within those. The northwestern

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and southeastern corners of Olkiluoto (Fig. 5-4) are the most potential localities to find subdomains dominated by D2 structural features.

During the D2 deformation the earlier structures were overprinted by a generation of the penetrative S2 schistosity or metamorphic banding associated with strong migmatisation and abundant production of leucosome veins parallel to the F2 axial surface. Due to tightness of F2 folds and intensity of D2 deformation, the lithological layering and earlier foliations have often been rotated parallel to the S2 foliation which can, in fact, be expressed as a composite structure S0/1/2. In the course of progressive D2 deformation the production of leucosome continued and the veins formed at an early stage of deformation may be folded isoclinally accompanied by semiconcordant shearing. Shear related structures have been observed as the most important D2 elements in certain zones or lithological units. Several veined gneiss units are dominated by asymmetric, augen gneiss like migmatite structures and certain pervasively sheared TGG gneisses are also one candidate for this category. D2 deformation is assumed to be the most powerful stage in the structural evolution of the Olkiluoto domain. It has pervasively deformed the whole paragneiss complex simultaneously with metamorphism at the uppermost amphibolite facies conditions. Thus, it is possible to interpret most of the structural elements as some kind of composite or interference structures with the products of D2 deformation.

In deformation phase D3, the earlier deformed migmatites were zonally refolded or rotated (Figs. 5-1b and 5-1d). Several zones dominated by ductile D3 shear and fold structures were formed, and often the S2 foliation was rotated parallel to the F3 axial plane (S3). Typically no new crenulation or overprinting foliation was created but still the foliations in the zones strongly affected by D3 deformation must be described as a S2/3 composite structure. Simultaneously with D3 deformation new granitic leucosomes and cogenetic pegmatite dykes intruded often parallel to the F3 axial surfaces (Fig. 5-1c). The F3 fold axes often plunge gently to the NE or SW indicating the subhorizontal orientation of previous planar structural elements. Overturned F3 folds with axial planes dipping to the SE have been mapped in the eastern part of the Olkiluoto site (Fig. 5-1d). The S3 foliations and F3 axial planes dip to the SSE with an average angle between 40 – 50 degrees. The mean orientation of the S3 foliation is 160/45° (Fig. 5-2).

The NW contact zone of the diatexitic gneisses against the veined gneiss domain is one probable candidate for a SE dipping D3 ductile shear zone. Thrust related deformation along that zone would explain the differences in the types of migmatite structures between those lithological units. As a whole, the intensity of the D3 deformation seems to be highest in the central part of the study site.

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Figure 5-1. A) S1 foliation folded by F2 folding with S2 axial plane foliation. B) S2

foliation folded by F3. C) Pegmatitic granite dyke subparallel to the F3 axial plane. D)

Overturned F3 fold with axial plane surface dipping by ca. 40 degrees to the SE. Photos

by Seppo Paulamäki Geological Survey of Finland.

Figure 5-2. Foliation directions (dip direction/dip) measured from drill core samples

OL-KR1 – OL-KR33b from Olkiluoto site (N = 9425). Equal area, lower hemisphere

projection. Concentrations % of total per 1% area.

D

S1

F2, S2

D2 -

leucosome

S2

F3

C

F3

D3 pegmatite

D

A B

S3

S4

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Subsequently, the D3 elements and earlier structures were again redeformed in the stage D4, which produced close to open F4 folds (Figs. 5-3a and 5-3b) with axial planes trending ca. NNE -SSW and dipping to the SEE. The D4 structures were previously detected in a few outcrops in the western part of the Olkiluoto study site but according to the latest outcrop and trench mapping, the central and southeastern parts of the Olkiluoto site, the ONKALO area and the regions eastward from that, have been affected more strongly by the fourth stage of deformation. Due to D4 deformation, the S2/3 composite structures were zonally reoriented towards the trend of F4 axial plane (S4)(Fig. 5-4). Locally, ductile D4 shear zones subparallel to the regional S4 plane have been observed (Fig. 5-3c). The mean orientation of the S4 direction is 135/42 (Fig. 5-2) on the basis of measurements carried out from outcrops and all drill core samples, but the S4 surfaces bend to a more gentle orientation in the deeper parts of bedrock.

The latest ductile structures to be identified are the open F5 folds, the fold axes plunging gently to the ESE and the axial planes to the SSW (Fig. 5-3d).

Figure 5-3. A) Tight F3 folding re-folded by F4. B) Open F4 fold with roughly N-S

trending axial surface. C) Augen gneiss-like D4 fault rock (ductile D4 shear zone)

subparallel to the regional S4 plane at a wall of the ONKALO access tunnel. D) Open

F5 folding with NW-SE trending axial surface.

F5

B

C DS2/S3

F4

F3

A

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5.2 Two-dimensional Model

A two-dimensional model or regional structural interpretation involves the results of works dealing with the products of polyphase structural evolution and intensity variation of different deformations (see above and chapter 3) at the present surface section of the bedrock. The shape and orientation estimations of individual lithological units are one result of that interpretation and the lithological map with structural trend lines presented in Fig. 5-4 is a summary of the work.

According to the observations, the earliest structural elements, primary sedimentary structures, S1 foliations and other products of the D1 deformation are rarely identifiable and mostly destroyed or totally overprinted by later deformations. Thus the interpretation does not involve the regional products of the early stage deformation.

The second stage in the structural sequence, D2 deformation, is assumed to be the most remarkable and intense event in the structural evolution and the bedrock is pervasively affected by it. Symmetry of ductile deformation structures and shapes of lithological units created by that deformation are slightest disturbed in the northwestern and southeastern parts of the study site. Thus, D2 deformation is assessed as the dominating factor in the modelling procedure concerning those subareas where E-W striking lithological units (Fig 5-4) and migmatite structures or regional foliations parallel those are apparent results of D2 deformation.

Intensities of the subsequent deformations have been more fluctuating and identifiable structural elements created by those events were concentrated into particular subzones. The NE – SW trending zone, which passes through the middle of the study site (Fig. 5-4), was most powerfully affected by D3 deformation. Pervasive foliations trending NE –SW or axial surfaces parallel to that direction are frequently detected inside that zone. In addition, several narrow subzones in other places are characterised by the same structural trend (Fig. 5-4), which demonstrates the significance of the D3 deformation within those.

The next deformation, stage D4 affected most strongly the bedrock unit exposed around the ONKALO area, in the middle part of the study site and extending as a 0.5 km wide zone to the north and south. Within that zone the F4 axial surfaces, ductile D4 shear zones and foliations in general are NNE-SSW trending (Fig. 5-4).

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Figure 5-4. General trends of planar D3 – D

5 ductile deformation elements. Tentative

form lines of the pervasive foliation by Ismo Aaltonen, Posiva Oy.

5.3 Three-dimensional Model

The three dimensional ductile deformation model or, in this case, the foliation model extends downward from the 2D model. The most comprehensive demonstration of the results of the structural interpretation is included in the lithological 3D model. The trends of structural symmetry meaning the orientations of axial surfaces and rarely developed axial surface foliations and the domains of the most intense D3 and D4

deformation are determined on the basis of drill core sample investigations. The 3D model visualises the domains affected most intensively by these late stage deformations (Fig. 5-5). The model also shows the anticipated orientations of S3 and S4 axial surfaces down to the depth of 500 m.

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Figure 5-5. 3D model of the orientation of the composite foliation S2/3/4 dipping gently

to the S and SE. The colours are from the Surpac software and do not refer to any

specific foliation.

5.4 Correlation to ductile deformation of the Svecofennian Domain

Ductile deformation is one consequence of the Svecofennian orogeny (Gaál & Gorbatscev 1987), which created compressional deformation structures at the convergent stage of the orogeny but probably also tensional structures in the progress of it. The earliest deformation structures are identical everywhere in the Svecofennian domain. Typical structural section includes relicts of primary stratification with coplanar S1 foliation associated with isoclinal folds (e.g. Väisänen & Hölttä 1999, Paulamäki et al. 2002 and references therein). Sedimentation at island arc environments and developing arc system may accomplish similar structural features in multiple variations. The depositional ages of Svecofennian supracrustal, volcanogenic rocks often range from 1910 to 1885 Ma (Welin 1987; Vaasjoki et al. 1994; Kähkönen 1999; Väisänen et al. 2002; Ehlers et al. 2004) demonstrating the activity and volcanic arc evolution during that period. In most cases, the next and often most prominent stage in the structural sequence is defined by isoclinal folding and other structures of stage D2,which subsequently were overprinted by more open folding by stage D3 (Väisänen et al. 1994; Kilpeläinen 1998; Mäkitie 1999,;Nironen 1999; Väisänen & Hölttä 1999; Paulamäki et al. 2002; Väisänen et al. 2002; Rutland et al. 2004). In spite of the similar character of structural sequences in those Svecofennian subdomains, dynamic and chronological correlation of individual events of the structural evolution is not unambiguous. Nevertheless, N - S or NNW- SSE directed tectonic stress fields are in the most cases dominant factors in the structural evolution.

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A completely similar structural sequence as determined from the Olkiluoto site is described from the Loimaa – Alastaro region (Nironen 1999), westward from Olkiluoto. Deformations D1, D2 and D3 have similar characteristics and D4 structures with roughly N-S striking axial traces in both areas may be the consequence of the same tectonic events. According to Nironen (op. cit.), the age of the D2 deformation is 1880 - 1870 Ma and the D3 deformation took place ca. 1870 Ma ago. E-W compression and D4

deformation acted 1850 – 1800 Ma ago, simultaneously with high-grade metamorphism in the adjacent Late Svecofennian granite – migmatite zone (Ehlers et al. 1993). A more accurate age for the migmatite zone is given by Ehlers et al. (2004), and the age, 1830 Ma, can be accepted as the age of the D4 deformation of the Olkiluoto site. Ductile deformation in Southeastern Finland, within the Southern Finland Shear Zone ceased 1790 Ma ago (Ehlers et al. 2004) and the age of D5 deformation in Olkiluoto is at least the same. Ductile structural evolution of the Olkiluoto supracrustal seems to have started simultaneously with the Svecofennian island arc evolution, ca. 1910 Ma ago and ended at the latest 1790 Ma ago. Ductile deformation events are highly synchronous with the deformational events of the adjacent regions but exact correlation is impossible without direct age determinations of deformation processes.

5.5 Correlation to previous bedrock model

No independent ductile deformation model was included in the previous bedrock model by Vaittinen et al. (2003) and thus a direct comparison of this and the earlier model version is not possible. However, as in the present model the 3D lithological model was based on interpretation of the various phases of ductile deformation presented in Paulamäki & Koistinen (1991). One difference in the results of ductile deformation interpretation utilised in the previous model version and the present one is in the influence of the D4 deformation. Currently, the intensity of that deformation in the middle part of the Olkiluoto site is evaluated to be significantly higher than during construction of the earlier model.

5.6 Correlation to ONKALO area model version 0

The Olkiluoto Site area model is an extension of the ONKALO area model. Thus the ONKALO area submodel dealing with ductile deformation structure is identical to the model represented in this report.

5.7 Evaluation of implications for construction

The characterisation of the foliation, which is considered as the most important element of the ductile deformation in Olkiluoto, is essential for both the understanding of rock mass properties and rock engineering. Foliation planes represent incipient planes of weakness and this means that the rock strength is anisotropic, i.e. dependent on the orientation of the foliation. (Milnes et al. 2006) and, consequently, the orientation of

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foliation can have implications on the constructional properties of the rock mass. Different rock types show variations in the foliation type and degree of foliation intensities. Foliation of diatexitic gneiss, for example, is mostly irregular and weak (Aaltonen 2005); this decreases the rock’s mechanical significance of the foliation in the southeastern part of site area.

The foliation in the ONKALO area has usually a quite consistent dip direction to the SE and a subvertical dip. Still, foliation observations from the drillholes of the ONKALO area indicate a slightly more gently dipping foliation below depths of about 300 metres in the ONKALO area (Aaltonen 2005). If the tunnel direction is parallel to the strike of the foliation, in conjunction with high degree of foliation intensity, the foliation poses higher risk for the formation of blocks and therefore rock enforcement may be needed. Subhorizontal foliation orientation is also more likely to increase the need for re-enforcement than subvertical orientation.

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6 ALTERATION MODEL WITH SPECIAL EMPHASIS ON HYDROTHERMAL ALTERATION

In the Olkiluoto bedrock, the influence of three different modes of alteration can be identified in the repository and ONKALO tunnel rock mass volumes. Each of these has produced its own alteration assemblage and can be distinguished from the others. The alteration events have had an influence on the whole chemical composition and the mineralogical character of the altered rocks and, as a result, they have consequences on the physical properties of the bedrock.

Although the three alteration events are independent and very remote processes over the huge period of time, without a doubt, they are interrelated and have successive multiplicative effects on minerals and rock quality. The alteration episodes are the following in chronological order:

Retrograde phase of metamorphism affected the rock ca. 1900 - 1800 Ma ago. These changes can be seen as sericitisation and saussuritisation of feldspars, and chloritisation and pinitisation of mafic minerals. Temperatures were high at the moment of these retrograde processes, significantly higher than during the hydrothermal alteration event. The products of the retrograde metamorphism are observable throughout the Olkiluoto island and they represent a rather common regional metamorphic condition in Finnish bedrock. In construction and long-term safety issues they remain inconsequential. Instead, hydrothermal alteration and weathering are recognized as having great importance to those topics and therefore these two areas requires a further research.

Hydrothermal alteration processes are estimated to take place at temperatures from 50°C to slightly over 300°C (Blyth et al. 1998; Gehör et al. 2002; Gehör, inpress). These processes are thought to be linked to late stages of metamorphism and specifically at Olkiluoto to the rapakivi granite igneous activity 1580 - 1570 Ma ago and intrusion of the olivine diabase dykes 1270 - 1250 Ma ago. Typical products of hydrothermal alteration are Fe-sulphides (pyrrhotite, pyrite), clay minerals (illite, smectite-group, kaolinite group) and calcite.

Surface weathering is a process that affects rocks in situ mechanically or chemically at the surface. In general, weathering is restricted to the destructive processes caused by temperature changes and corrosion by surface waters and atmospheric oxygen. This is the youngest of the alteration processes at Olkiluoto and is still active. It is probable that it has its roots going back to at least tens of million of years and has a spatial connection to locations of strong hydrothermal alteration.

Petrologic and fracture mineral studies of the drill core samples have indicated remarkable changes in mineralogical composition due to multistage and extended hydrothermal events in the Olkiluoto high-grade gneisses and granitic rocks. Alteration products have been detected at least in small amounts practically in every drillhole and throughout the site volume. Recognizing that the alteration products may reduce the

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mechanical stability of the bedrock, it was decided to undertake a pilot study on core samples from drillholes OL-KR1 to OL-KR33.

The drill core samples were studied in order to solve some basic issues on hydrothermal alteration at Olkiluoto. The task was intended to:

determine the most typical alteration minerals or mineral assemblages

find out the location of the most altered sections and the length of these sections

study the style and intensity of alteration and estimate the alteration-related geochemical modification

present the alteration domains in 3D files

The observations from the drillhole loggings give the impression that alteration is linked to the phases of magmatic activity and to some extent it is assumed to represent an alteration halo of the granite intrusion, which has been a source of longstanding (at least tens of millions of years) thermal charge. The effect which these fluids have had on the rocks, implies that the heat flow has created an extensive circulating hydrothermal fluid system and further that these fluids, which in all evidence have undergone extensive pH increases and decreases during the bedrock evolution, are the reason for the hydrothermal alteration.

Hydrothermal alteration episodes have taken place at quite low temperature conditions; the estimated temperature interval ranges from 300oC to less than 100oC (Blyth et al. 1998; Gehör et al. 2002; Gehör, in press.) based on fluid inclusion studies on fracture calcites. Typically for the hydrothermal regimes, high permeability zones formed and these zones appear to have repeatedly acted as pathways for the periodical thermal fluid circulation.

The main topics for consideration and further research include the following: Hydrothermal alteration has widely produced from the primary anhydrous framework silicates (mostly feldspars) the secondary hydrated clay minerals. The precipitation of sulphides and calcite is similarly related to these events and all these changes are most likely to influence the rock quality due to their physical properties and intense fracturing adjoining the hydrothermal system. The effects can be found in rock mechanics and groundwater chemistry. Clay minerals are recognized to contain smectite group phases, the swelling property of which has not been specified this far. Connection of surface weathering to hydrothermally altered domains

For example, in the area close to the ONKALO access tunnel entrance, the softened section occurs in the same locations as the pervasive hydrothermal alteration, particularly kaolinisation, sulphidisation and carbonatisation. This feature has been reported from the tunnel and from investigation trenches (Paulamäki 2005a, 2005b).

The weathering front has proceeded from the particular surficial zone downwards, under the influence of meteoric water circulation and under elevated redox potential. Under these conditions the water-rock interaction has controlled the pH of the water and

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progressively advanced the overall dissolution of ions. These processes have affected in particular the porous bedrock, which already has been mechanically and chemically prepared by hydrothermal fluid circulation.

The hydrothermal alteration in the site area outlines the distribution of three main alteration types found at the bedrock area. These are kaolinisation, sulphidisation and illitisation. In addition to these, the occurrence of calcitic fracture fillings and the sets of calcite stockworks have been evaluated in this report.

6.1 Description of hydrothermal alteration

In the drill core logging, the core sections were mapped as hydrothermally altered zones, if there was clear observable pervasive changes in mineralogy or repeated fractures with visible infilling and they formed at least 1-m long continuous section. In the first 28 drillholes a total of 266 altered intersections were detected totalling 4099 m in length, which encompasses ca. 26% of the drill core samples. In single drillholes the number of the alteration zones varies from as low as 5 % to as high as 50%. Eleven intersections were longer than 50 m, the longest one being 172 m in OL-KR12 at a depth of 509 - 681 m.

To describe the grade of alteration, two different types of alteration were distinguished, a fracture-controlled type and a pervasive (or disseminated) type (Figs. 6-1 to 6-6). The fracture-controlled alteration indicates that hydrothermal fluids have passed through the rock along planar features and alteration is restricted to incipient fractures or narrow zones adjacent to them. This subtype seems to consist of in situ or autochthonous minerals, but in some cases also quite thick possibly allochthonous kaolinite fillings have been observed. The pervasive alteration indicates the strongest type of alteration, which occurs pervasively or disseminated in the rock in addition to the common location in the fractures. Only in a few cases, is the pervasive occurrence of alteration not observed to occur in fracture fillings, or altered fractures are just very few in number.

The study of hydrothermal alteration zones suggests an extended and complex history of sequential events (Gehör, in press). Different alteration events indicated by specific minerals or mineral assemblages have significant overlap so that the alteration zones of the younger minerals often replace the older ones. The following is a short and generalised description of hydrothermal processes.

Hydrothermal fluids tend to move upward and outward from their source at depth. Porous and permeable host rocks (those containing lots of interconnected pore spaces) allow this to happen more readily.Some types of clayey rocks, like shale or slate, are extremely impermeable. A layer or unit of these impermeable rocks are able to act as a barrier to the fluid circulation or remarkably reduce the percolation of the hydrothermal fluids which, generates overpressure and subsequent hydraulic fracturing in rocks, thus

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enabling hydrothermal fluids and gas to circulate along the conduits formed during these events.A well-developed fracture system and fault zones together constitute the passages for fluids to circulate and serve as favourable target zones for alteration phenomena and precipitation. An extensive open space fracturing is present and characterises the bedrock volume, where the density of hydrothermal fluids conduits had visibly increased. The development of new alteration products and precipitation of new generations of fracture minerals along the fracture walls has predominantly taken place in this kind of hydrothermally crushed zones. In the long run these precipitates have blocked the passage of the circulating fluids through these conduits.

For the present modelling work the following hydrothermal alteration mineral assemblages were separated in core logging:

sulphides (mainly pyrrhotite and pyrite, sporadically sphalerite and galena) ± quartz

illite

kaolinite

calcite

The list is also a simplified and rough age order from oldest alteration events to youngest ones. Undoubtly, all these events have occurred repeatedly from time to time and therefore there are no absolute age data on these alteration events. The cyclic nature at Olkiluoto indicates a complicated evolution, in which the alteration events have partially recycled the earlier alteration products either as solid or in soluble form, as is described in detail in Gehör (2005). The order of appearance of the three alteration phases above is based on geological observations and must be understood as relative.

Sulphides usually occur together with quartz as silicification in ore forming processes. It seems that most pyrrhotite (FeS) has been mobilised and already enriched in ductile tectonic processes showing occurrences from dissemination to veinlets and breccia-like networks (Figs. 6-1 and 6-2). Pyrite (FeS2) occurs in some amount together with pyrrhotite but more often as vein stockworks and fracture infillings. Usually the sulphides are associated with other minerals, such as calcite or clay minerals.

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Figure 6-1. Silicification and breccia-type pyrite in sheared mica gneiss. OL-KR22, ca.

390 m.

Figure 6-2. Silicification and mobilised pyrrhotite and pyrite forming breccia and

veins. OL-KR24, ca. 240 m.

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All greenish, soft clay-type material is classified as illite1 (K, H)Al2(Si, Al)4O10(OH)2 -

xH2O although it is known to occur together with a variety of other minerals such as the smectite group, chlorite, montmorillonite and so on (Gehör, in press). In thin section, it is impossible to separate those clay mineral mixtures from each other. Illite and fine-grained muscovite or sericite are mineralogically similar, except for grain size and textural appearance, however, the mode of occurrence of illite or illite-looking material shows clear replacement of older silicate minerals, often plagioclase (Figs 6-3 and 6-4). A lot of X-ray diffraction work is required to distinguish and identify the different mica and clay species, but technically they have same impact as soft soap-like mass which may volumetrically form 5 - 10% of the rock at Olkiluoto, locally even higher (Gehör et al. 2004).

Kaolinite Al2Si2O5(OH)4 forms extremely fine-grained, pure white, soft and powdery masses and coverings on fracture surfaces (Figs 6-5, 6-6 and 6-7). In several places it is found to associate with fine-grained calcite, which is identifiable only with dilute hydrochloric acid.

In addition to the three alteration processes, carbonatisation is a widespread feature, which is observed primarily in the fracture infillings or as stockworks, but it has randomly altered the rock itself. More data is required for characterising the definite presence of calcite and the grade of carbonatisation. Therefore in this paper the occurrence of carbonatisation is described merely on the basis of the observations made from fractures.

1 Illite and kaolinite are typically accompanied by phases of smectite group (1/2Ca,Na)0.7(Al,Mg,Fe)4(Si,Al)8O20(OH)47nH2O) and chlorite group (Fe, Mg, Al)6(Si,Al)4O10(OH)8

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Figure 6-3. Slickensided illite. OL-KR4, ca.760 m.

Figure 6-4. Strong pervasive illitisation. OL-KR1, 526.20 m.

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Figure 6-5. Strong pervasive kaolinisation, OL-KR4, ca. 525 m.

Figure 6-6. Fracture-controlled kaolinite. OL-KR24, ca. 32 m.

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Figure 6-7. Advanced kaolinisation in drill core sample OL-KR24 drill core length of

24 m. A red circle surrounds a typical cluster of white kaolinite spots.

6.2 Kaolinisation2

The kaolinitic alteration zones constitute numerous spots and lenses at irregular intervals. These have thickness from tens of centimetres to tens of metres in drill core transverses. The most intensively kaolinitised zones of the surficial slice, which the ONKALO tunnel has penetrated this far, come out as strongly weathered and softened sections. The kaolinitised zones contain illite on slickensides and as fracture fillings. For this reason all the zones where kaolinite occurs as a major phase (not as single clay phase) are chosen to this group. Kaolinite occurs in spots, either as a single phase, or together with illite and has typically corroded the framework of rock structure (Figs. 6-5, 6-6 and 6-7). Besides that, kaolinite forms powdery, disseminated white coatings that may well have thicknesses of several millimetres. It usually forms soft fillings, which are loosely attached to the host rock.

The kaolinitised sections are located effectively in an upper slice of the bedrock, varying in thickness from 100 – 200 metres measured form the surface. Kaolinite appears to be an important constituent of the rocks, forming 5 - 30% or locally even more of the volume. In the alteration model (Fig. 6-8), the kaolinitised wedge becomes deeper in northern part of the target area, where the present data (especially the data from the drill core OL-KR13), implies that the base of kaolinitised block reaches the

2 called argillisation in ore-related alteraration

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depth of 250 metres. The drill core data reveals numerous disconnected zones at greater depth, but their position remains unclear based on the current drill core data.

Figure 6-7. Kaolinitised sections are located in the uppermost part of the study area. a)

a view towards the NE, b) a view towards the NW. Yellow = pervasive kaolinitisation,

orange = fracture-controlled kaolinisation.

a)

b)

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6.3 Sulphidisation

Sulphidisation, which in this analysis is regarded as the distribution of pyrrhotite dissemination and the occurrence of pyritic stockworks (Figs. 6-1 and 6-2), covers considerable dimensions of the bedrock. The pyrrhotite dissemination is effectively connected with mica gneisses and migmatites and it has a particular affinity with graphitic occurrences. The distribution of the pyritic fracture infillings and hair dykes are excluded from this approach for clarifying the otherwise complicated three-dimensional spatial position of the alteration zones.

Sulphidised wall rocks, usually migmatites, contain several percent of disseminated pyrrhotite, which also occurs in the fractures of those zones. The thicknesses of this type of zones are from centimetres to several metres. Pyrrhotite is the main sulphide phase in graphitic fracture infillings.

The sulphidisation reaches the greatest depth in the SW-edge of the modelled bedrock volume (Fig. 6-9). The drillholes OL-KR7, OL-KR10 and OL-KR30 reveal the thickest section in the of the sulphidised bedrock volume. These drillholes indicate the lower limit for the zone reach at the depth of -250 to -300 metres. The available drillhole data from the SE edge of the modelled volume suggests the lower level of the sulphidised zone to shallower depth; the base adjusts at the level of -50 m in the SE section and becomes deeper in the NE section, where it has been recognised to reach the level of -150 to -200 metres. Similarly to the kaolinisation there are numerous disconnected patches outside the modelled sulphidisation block. Due to the inadequate drillhole information of that bedrock volume, successful modelling work is not possible with the currently available data.

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Figure 6-8. Sulphides are located in uppermost part of the model volume following

roughly the lithological trend (slightly dipping to the SE). a) a view towards the SE, b)

a view towards the NE. Red = pervasive sulphidisation, light red = fracture-controlled

sulphidisation.

a)

b)

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6.4 Illitisation

Illite forms alteration zones, which are green, transparent, soap-like mass or it forms grey to green waxy or powdered coverings in fracture plains. The bedrock volume at the site model includes discrete illitised zones, a principal part of which is concentrated in an alteration block, located in northern part of the modelled volume (Fig. 6-10). In fact the drillhole data indicate that the block that outlines the illitised bedrock appears to enclose the eastern repository panel. Illitised zones have characteristically thickness from 5 to 20 meters in drill core transverses. At the zones where the rock has experienced advanced illitisation, illite has replaced most of the previous minerals, locally into a grade that the preceding texture of the rock is hardly discernible any longer. In ultimate illitisation the rock has adapted a totally new chemical composition and has approached the equilibration with new environment, which has been the chemical state generated in fluid-rock interaction. This progress has typically resulted to a poorer quality in mechanical stability of the bedrock. The hydrothermal illitic alteration represents a more energetic process than the kaolinitic alteration does and therefore it is presumed to have more deep-seated influence to the host rock.

Illite may occur as single alteration product, but generally it is associated with calcite and sulphide precipitates and with the other clays, like members of kaolinite-group, smectite-group and chlorite-group. Figure 6-11 from drill core sample OL-KR8 illustrates the occurrence of the illitic zones and their relation to the other hydrothermal features in the bedrock.

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Figure 6-9. Domains of pervasive (dark blue) and fracture-controlled (cyan)

illitisation. a) a view towards the NW, b) a view towards the SE.

a)

b)

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6.5 Carbonatisation

The occurrence of calcite as infillings in the fracture walls and as planar and irregular veinlets (stockworks) is a special feature of the drillhole transverses. These are typically features, which have only a minor affect on the rock; so far there is hardly any evidence of penetrative carbonatisation of the bedrock itself. Instead calcite may have an important role in hydrothermal derived fractures and zones of brittle deformation and, similarly, calcite precipitates are widely observed in the matrix of breccia fragments and in thick clay fracture infillings. The fluid inclusion study of the fracture calcites has demonstrated that calcite precipitation has taken place in the temperature interval starting from 300oC and ending at temperatures less than 100oC (Fig. 6-12).

The hydrothermal fluid circulation appears to have episodes of neutralisation of the acidic fluid and thus enabled the episodic precipitation of calcite since the earliest stages of the hydrothermal activity. Calcite-precipitation appears to be a characteristic process in the closing phases of the particular fluid circulation episodes, as is supported by the remarks that calcite widely covers the older hydrothermally generated fractures infillings in all levels of the drilled bedrock volume.

There is evidence that the distribution and density of calcitic fracture sets is elevated in the zones where hydrothermal fluid flow has chemically and physically reworked the bedrock (Fig. 6-11). Correspondingly with the three other alteration processes, carbonatisation has a significant role in alteration events and on the whole the total volume of calcite in the hydrothermally altered zones appears to be significant. In relation with kaolinisation and illitisation, the reaction kinetics for calcite precipitation-dissolution reactions are known to be rapid and for that reason calcite apparently has hold up equilibration with the prevailing chemical potential and thus it may well have had several phases of precipitation and dissolution during the evolution of fluid flow. The precipitation of calcite has inevitably continued until present, whenever the ground water system reached the level of calcite saturation.

The grade of carbonatisation has been estimated by mapping the frequency and thickness of the calcitic fractures in the drillholes. When the recurring calcite-filled fractures are combined into zones, the carbonatisated sequences in this scheme appear to be located in the same positions as the other alteration types. The cutting lengths of the fracture-connected calcitic zones vary from few a metres to tens of metres.

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Figure 6-11. Drillhole sample OL-KR8. The fracture mineralogy of the drill core

sample demonstrates the occurrence of the main clay types, sulphides and calcite; the

thickness of the fracture infilling and the percentage, which is covered by the infilling

substance are given in separate columns. Calcite fracture infillings and the calcite

related to the vein stockworks are found to be a common associate in the hydrothermal

alteration zones.

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0

50

100

150

200

250

300

350

-50 -45 -40 -35 -30 -25 -20 -15 -10 -5 0

Tm

EQ3

EQ5

EQ8

EQ20

EQ27

Blyth et al

EQ25

EQ21

Figure 6-12. Homogenisation (Th) and melting temperature (Tm) measurements from

the fluid inclusions in fracture calcites of the Olkiluoto site. For a detailed description

of the sample locations and their properties the reader is referred to Blyth et al (1998)

and Gehör et al (2002).

6.6 Evaluation of implications to construction

There are three main factors controlled by hydrothermal alteration, which may be of great importance for the underground construction of the ONKALO facility. In addition to these, the role of carbonatisation and the presence of carbonate vein stockworks are in general of concern in evaluation.

Hydrothermal alteration affects the chemical and mechanical characteristics and stability of the host rock:

Mechanical strength of the altered rock mass is likely to be significantly reduced compared to the unaffected rock masses.

Chemical modification due to the hydrothermal re-equilibration is strong in the ultimately altered zones. Currently the whole-rock compositions of the altered zones are not known, but on the basis of the compositions of the alteration products, the most essential compounds, which may have been mobilised in these processes, are the oxides of alkaline earths and alkalines, particularly CaO, MgO, K2O and Na2O, and likewise SiO2, Al2O3, FeO, P2O5, U2O, ThO2, CO2, S, Cl, F. By all accounts also the REE-signatures of the altered zones were modified during hydrothermal episodes. The contents of these compounds in unaltered and altered bedrock volumes and their mutual proportions ought to provide essential indication of the grade of alteration, thus offering an intuitive understanding of the thermal and

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chemical factors and their gradients at the particular bedrock volume The concentrations of carbon dioxide and sulphur in the fracture phases and alteration paragenesis is of special importance as their capability for relatively rapid reactivity in oxidising and hydrous circumstances and their solution-dissolution actions may have an influence on the U- and Th-mobilities. Typical equations for the sulphur containing phases might be the reactions 1o to 3o, which, are expected to elevate the acidity of the matrix waters and, in that respect, the capability of overall dissolution of ions in circulating terrestrial water and in matrix waters increases. Particularly, the dissolution of sulphides and calcite is presumed to accelerate the growth of porosity and hence decrease the strength of the bedrock. The presence of calcium carbonate in certain zones diminishes the acidifying effect of the equations 1o-3o.Wherever CaCO3 is available, it provides a pH-buffer against sudden pH drops. On the other hand, if the alteration zones are taken strictly as closed systems, in conditions where calcite is not present or has been consumed (equation 3o), the sole addition of CO2 to water could also lower the water pH according to equation 4o.

1° 4 FeS2 + 15 O2 + 14 H2O 4 Fe (OH)3 + 8 H2SO4

2° 2FeS2 + 7O2 + 2H2O 2FeSO4 + 2H2SO4

3° CaCO3 (s) + H+ = HCO3- + Ca2+

4° CO2 + H2O H2CO3 H+ + H+ + HCO3-

The clay minerals considered as illite by the naked eye observations actually contains smectites, among which, XRD-identified montmorillonites have been reported (Gehör, in press). The swelling properties of these clay infillings have not been tested this far, but if the clays turn out to contain members, which have expansive lattice types, their connection to long–term safety is to be evaluated.

The field evidence attained from outcrop and trench mappings imply that the hydrothermally reworked bedrock is extensively damaged due to surficial and subsurficial weathering. Strongly weathered zones, cropping out in the site area, may be the result of interaction between porous rocks (soft and loose kaolinite-illite-calcite pods left after hydrothermal alteration) and meteoric water, which brings soluble agents close to surface (Posiva 2005). In particular, those intersections in tunnel driving, that crosscut the hydrothermally modified weathered bedrock, are the one which first require tunnel lining and rock re-enforcement, as their mechanical stability is most in all probability reduced compared to the unaffected rock mass.

More detailed investigations of the effects of hydrothermal alteration of the rock mechanical characteristics of the rock mass will be carried out in the near future.

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6.7 Correlation to the bedrock in Finland in general

Magmatic intrusions are obvious heat sources for geothermal fields. In the site area the rapakivi-related intrusions and the later magmatic events seem to be in response to the provision of the thermal energy that accelerated the fluid circulation and chemical reactions at their halo volumes.

Hydrothermal alteration may take place as large-scale regional alteration (connection with retrogressive metamorphism) or as a local, intense alteration, which strongly affects the rocks and changes the mineralogy and geochemistry. The alteration in the Olkiluoto area is considered to belong to the latter type. The descriptions with the intention of local hydrothermal alteration are characteristically those, which are linked to ore-related hydrothermal alteration, like the hydrothermally derived ore deposits Typical examples of these are information concerning mines, e.g., the Pyhäsalmi deposit and numerous other volcanic-hosted massive sulphide deposits, the reports of ore deposits at the contact zones of intrusions and particularly the descriptions of the gold deposits around Finland and Fennoscandia.

The type of alteration observed in the Olkiluoto area has not been described from the analogous lithological relationships in Finnish bedrock. The nuclear waste disposal site studies in Finland have revealed that the low temperature alteration of the country rock has in various degrees affected the bedrock . However the alteration in any of the studied sites is comparable to the Olkiluoto site. For instance the site studies in Loviisa-Hästholmen (Gehör et al 2000) and Kuhmo-Romuvaara (Gehör et al 1996a) have implied distinctive alteration characteristics for both. Although these two have a lot of similarities to Olkiluoto, especially in relation with the fracture infillings, there are differences as well, such as concerning the frequency of sulphidic fracture planes, which is remarkably fewer than in Olkiluoto. A major difference is that the bedrock itself in Romuvaara and in Hästholmen has not hydrated to form illite and kaolinite, although these phases are present in fracture fillings. On the other hand, the bedrock in Hästholmen has suffered from advanced oxidation, which in Olkiluoto is observed only in restricted bedrock volume. The particular alteration feature in Romuvaara, correspondingly, is the occurrence of zeolites, which are found to be also present in Olkiluoto fracture fillings but of minor importance.

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7 BRITTLE DEFORMATION MODEL

7.1 Description of brittle deformation

Faults usually show evidence of the most recent increment of slip and the displacement can often be inferred, for example, from the offset of lithological layering, crosscutting veins and older fractures. From the perspective of more detailed analysis of faults, the orientation of the fault planes and associated slip striation (slickenlines and fibrous growth of minerals) on the fault surfaces provide important tools for the characterisation of the faulting and proper fault-slip analysis, assuming that the slip striation corresponds to the formation of the fault and not to the most recent increment (an assumption, which is not likely to be valid in complexly deformed areas where reactivation of older deformation zones is probable). By proper kinematic analysis using the fault plane and slip striation orientations, kinematically compatible sets of faults can be identified and classified into groups. Plain fault plane orientations do not provide the proper tools for the identification of the cogenetic faults, as different orientations of faults may still be kinematically compatible. In the current modelling effort, a very simple classification of faults is made on the basis of the orientation of slip striation, which is likely to indicate cogenetic formation of the faults. It should be emphasised though, that this approach does not exclude the possibility that highly varying slip-striation orientations may have been formed in the same faulting (deformation) phase. Possible slip-compatibility will be validated later by proper kinematic analysis.

In the following, we focus on the preliminary results of the analysis of fault-related structures within the Olkiluoto model volume, as revealed by the relationships encountered in the access tunnel, using supporting evidence from the drillholes. Recent studies of the structural evolution of the Olkiluoto bedrock have shown the obvious statistical similarity between the orientation of the regional, composite, pervasive foliation and the slickensided fracture surfaces, measured from the drillholes. One explanation for this relationship is that faults appear to have exploited the planes of weakness imposed by the pervasive foliation. Thus, the products of ductile deformation seem to be important precursors for subsequent brittle deformation. However, many brittle fault structures are not controlled by any older deformation elements.

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A) B)

Figure 7-1. A. Stereogram showing foliation plane orientations (dip direction/dip)

measured from drillholes/core samples OL-KR1 – OL-KR33, Olkiluoto (N = 9500,

lower hemisphere equal area projection). B. Fault plane orientations (dip direction/dip)

measured from the same samples/holes (N = 1655). Schmidt lower hemisphere, equal

area projection. Concentrations % of total per 1% area.

The most common population of fault planes dips gently to the SE (Fig. 7-1B), but statistical evaluation of fault plane orientations does not provide any useable basis for further subdivision of those structures. On the contrary, fault slip directions are widely variable (Fig. 7-2A) and the number of cogenetic phases of brittle faulting or individual sets of faults with identical characteristics of separation will be rather large and the final system of brittle faults intersecting the central part of the Olkiluoto study site will be rather complex. Detailed analysis of fault-slip data shows that more than 20 significant groups of kinematically alike brittle faults can be detected from the site. Evaluation of their real impact on the bedrock structure is a challenging exercise and, for that reason, first phase modelling is based on a result of simplified, generalised classification of fault-slip data.

Tentatively, five groups of brittle faults are isolated from the total amount of brittle faults (fault-slip direction maxima A, B, C, D and E in Fig. 7-2). Figures 7-3 and 7-4 show the orientations of the five fault-slip groups and the orientations of the fault planes, from which the fault-slip orientations have been measured. Fault-slip directions are subhorizontal, N-S trending for group A, gently NE or SW plunging for group B, gently SSE plunging for group C, gently ENE plunging for group D and gently SE plunging for group E. Variation in the fault-slip orientation is limited to 10 – 20 degrees from the most typical slip direction, but fault planes can vary without limitations around that lineation. Thus various concave and convex structures around the fault-slip vector direction are possible. In all of the groups, most of the fault planes dip gently to the SE (Fig. 7-3 and 7-4). In fault groups A and B there are also fault planes that dip steeply to the E and SE, respectively.

In the following sections, the characteristics of the observed and interpreted fault zones are described in detail and the results are evaluated against previous modelling efforts. It should be noted that this is the very first (and preliminary) attempt to classify and model

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zones based on their geological properties and therefore the model will evolve, as more detailed analysis of the collected data is carried out. Proper kinematic analysis, for example, is likely to increase our knowledge of the genetics of the zones and will therefore provide clearer constraints on the extent and properties of the faults. Also, the effect of secondary shear fractures (Riedel fractures) within fault zones and the overall internal structure of a fault will be considered in more detail in future modelling efforts as these are likely to have implications on the mechanical and hydrological properties of the faults.

Figure 7-2. A. Stereogram showing all the fault slip directions (separation vector)

measured from drill core samples OL-KR1 – OL-KR33 and five direction maxima (N =

1699). Schmidt lower hemisphere, equal area projection. Concentrations % of total per

1% area.

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A)

B)

C)

Figure 7-3. Fault-slip (left) orientations (trend/plunge) and corresponding fault plane

(right) orientations (dip/direction/dip). A) Fault group A (N = 245), B) fault group B

(N = 370) and C) fault group C (N = 354). Schmidt lower hemisphere, equal area

projection. Concentrations % of total per 1% area.

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A)

B)

Figure 7-4. Fault-slip (left) orientations (trend/plunge) and corresponding fault plane

(right) orientations (dip/direction/dip). A) Fault group D (N= 96) and B) fault group E

(N = 118). Schmidt lower hemisphere, equal area projection. Concentrations % of total

per 1% area.

7.2 3D model

7.2.1 Interpreted brittle fault zones

The brittle fault intersections observed in drillholes were connected from drillhole to drillhole using the fault-slip directions as a guide as described in Chapter 3-5 (assuming that single fault planes within a fault zone are subparallel to the orientation of the main fault). The resulting brittle fault zones (BFZ) are presented in Figs. 7-3 to 7-7 and described in detail in Appendix 3. The constructed faults were checked against other data, such as charge potential, VSP etc. In this phase of the modelling, the model includes 98 interpreted fault zones (BFZ001 - BFZ097 and BFZ103). However, it should be noted that the results are tentative and the model will evolve, as more data become available. In this phase, the modelled 98 fault zones cover 116 (i.e. ca. 93%) of 125 brittle fault intersections observed in the drillholes.

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The interpreted fault zones have been classified into four confidence groups in terms of their orientation

3: very low (confidence value 0), low (1), medium (2) and high (3). The confidence values are based on number and orientation of slickensided fracture surfaces in one intersection, number of intersections and supporting geophysics (Tables 7-1 to 7-4).

The confidence of the orientation of a zone is assessed by the number of intersections within that zone and by the correlation of the orientation of the intersections to each other. As an example, if a zone is interpreted as including two intersections, and their mutual correlation (estimation on the fit of the orientations) is estimated to be good, the geological confidence is then assigned a value of 2 (Table 7-2). The interpreted zone also has a good correlation with a charged potential anomaly and therefore it is also assigned a geophysical confidence of 2 (Table 7-3). Combining these two values, the overall confidence of the zone has then a value of 3 (Table 7-4), i.e. it has a high confidence. As the emphasis in this model is on the geological evidence, geophysical anomalies can only increase the confidence of an interpreted zone. If an interpreted zone consists only of one intersection, then its geological confidence is assessed using Table 7-1, where the internal correlation of the orientation of slickensides is estimated; as an example, if a zone is interpreted as consisting of a single intersection which has 3 fractures with slickensided surfaces of which 2 are parallel, the intersection therefore has a good correlation with respect to slickenside orientations. From Table 7-2, a value of 1 can be assigned for the geological confidence. Assuming that there are no observed geophysical anomalies correlating with the zone, the zone has then the overall confidence of 1, i.e. low confidence.

Table 7-1. Slickenside orientation in one intersection

Orientation

Number of

slickensides

No parallelism 2 parallel 3 or more parallel

0 No correlation No correlation No correlation 1 No correlation No correlation No correlation

2-3 Poor correlation Good correlation Good correlation 4 or more Poor correlation Good correlation Good correlation

Table 7-2. Geological confidence

Number of intersections

Orientation (from

Table 7-1)

1 2 3 or more

No correlation 0 0 0 Poor correlation 0 1 2 Good correlation 1 2 3

3 The confidence assessment is related only the orientation (and therefore, to the position) of an interpreted fault zone and is therefore, assessment of the confidence of the overall interpretation. No assessment is performed on the quality of the applied data.

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Table 7-3. Geophysical confidence

Confidence VSP Charge potential Sampo

0 No correlation No correlation No correlation 1 Poor correlation Poor correlation Poor correlation 2 Good correlation Good correlation Good correlation 3 - - -

Table 7-4. Overall confidence in orientation

Geology Geophysics

0 1 2

0 0 0 0 1 1 2 3 2 2 3 3 3 3 3 3

Most of the modelled fault zones are present only in one drillhole and, consequently, have a confidence value of 0 or 1 (65 fault zones). 25 fault zones are of medium confidence and 8 have a confidence value of 3.

Figure 7-5. Fault zones of fault group A. View from the SW.

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Figure 7-6. Fault zones of fault group B. View from the SW.

Figure 7-7. Fault zones of fault group C. View from the SW.

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Figure 7-8. Fault zones of fault group D. View from the SW.

Figure 7-9. Fault zones of fault group E. View from the SW.

All the modelled fault zones are shown in Fig. 7-10. N-S trending vertical cross-section showing the modelled fault zones together with the modelled lithologies is presented in Fig. 7-11. More N-S and E-W trending vertical cross-sections are presented in Appendix 4.

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Figure 7-10. Brittle deformation model of the Olkiluoto study site. View from the SW.

Figure 7-11. N-S trending vertical section, y = 1525600. View from the E.

Pegmatitic granite

Diabase

Diatexitic gneiss

TGG gneiss

Veined gneiss

LEGEND

Brittle deformationzone

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Description of selected structures with high confidence (confidence value = 3)

Brittle fault zone OL-BFZ002

DIMENSIONS (X/Y/Z) 646 m/1054 m/306 m

DIP DIRECTION/DIP 180°/17°

FAULT VECTOR ORIENTATION 180°/14°

FAULT GROUP A

SENSE-OF-MOVEMENT Normal

CONFIDENCE 3

INTERSECTIONS OL-KR1 610.30-619.20 m

OL-KR19 464.75-465.32 m

OL-KR19 476.67-477.93 m

Single fault planes at OL-KR6 440.82-451.11 m

Single fault planes at OL-KR2 540.82-547.13 m

OL-BFZ002 is a brittle fault zone with an average dip direction/dip of 180°/17° and a mean fault vector trend/plunge of 180°/14° (Fig. 7-12). The sense-of-shear of the fault is normal, i.e. the hanging wall block has moved down the dip of the fault plane. The zone has been correlated into five different drillhole intersections based on observed fault plane orientations in drillholes and on observed VSP reflectors. The zone intersects drillholes Ol-KR1, OL-KR19, OL-KR6 and OL-KR2 at the drillhole length-intervals indicated in the tabulated data above. The zone is modelled to intersect drillhole KR19 at two different length-intervals, depicting the splaying of the fault zone into two separated fault planes.

Geological properties of drillhole intersections

OL-KR1, 610.30-619.20 m

In drillhole OL-KR1 at 613-618 m, the veined gneiss and the pegmatitic granite are strongly altered and fractured (Blomqvist et al. 1992). In many places the rock has been mangled into clayey material, mostly consisting of chlorite, and this material also fills the fractures. These fractures have in places opened and the rock has been altered, mainly through sericitisation, saussuritisation, silicification and albitisation. In places, the silicification and albitisation have closed the fractures, and these fracture veins have later been deformed with injection of calcite in various phases. The above altered and fractured parts have later been thoroughly illitised, after which slickensided fracture surfaces, breccias, and abundant filled fractures and cavities have been formed. A total of 21 fracture fillings are detected and they are classified into five groups according to decreasing temperature and age (Blomqvist et al. 1992). The two oldest groups are hydrothermal (T <300°C) and the fracture infillings are characterised by muscovite-greisen fractures, silicified microbreccias, albite veins and quartz veins. The younger hydrothermal group is characterised by clay minerals, especially illite, crystallised on chlorite shear planes and fractures. Other typical fracture infillings include pyrrhotite, baryte, laumontite-leonhardite, analsime, adular and fluorite. Pyrite veins, calcite-

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chamosite breccias and infillings of the third group cut the two previous groups. The fourth group is characterised by clay minerals with formation temperatures between 150°C and 40°C. Plagioclase is altered to kaolinite. The youngest group consists of monomineralic calcite infillings, or breccias with anatase on the walls of minor cavities.

OL-KR19, 464.75-465.32 m

The intersection is composed of diatexitic gneiss and contains a few old and welded, calcite- and pyrite-bearing fractures. The intersection consists of a total 10 fractures, which have scattered dips and dip directions. Four slickensided fracture surfaces are also observed, with a scattered orientation of striation.

OL-KR19, 476.67-477.93 m

The intersection is composed of veined gneiss and contains a few old and welded fractures with calcite fillings. The intersection also contains 5 slickensided fracture surfaces, which have a subhorizontal fault plane and fault vectors plunging subhorizontally towards the SW. The rock in the intersection is evenly fractured. A fracture at the depth 477.93 m has kaoline filling.

OL-KR2, 540.82-547.13 m

The zone is correlated to single fault planes in drillhole OL-KR2 at the drillhole length of 540.82-547.13 m. The interval contains two slickensided fractures with a subhorizontal orientation and fault vectors plunging towards the S.

OL-KR6, 440.82-451.11 m

The zone is correlated to single fault planes in drillhole OL-KR6 at the depth of 440.82-451.11 m; the interval contains five slickensided fractures with a subhorizontal orientation and fault vectors plunging towards the S.

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Figure 7-12. A) Brittle fault zone OL-BFZ002 viewed from the east, B) and from above.

a)

OL-KR29

OL-KR6

b)

OL-KR29

OL-KR6

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Brittle fault zone OL-BFZ005

DIMENSIONS (X/Y/Z) 681 m/286 m/467 m

DIP DIRECTION/DIP 167°/28°

FAULT VECTOR ORIENTATION 181°/25°

FAULT GROUP A

SENSE-OF-MOVEMENT Reverse or normal, contradictory

CONFIDENCE 3

INTERSECTIONS OL-KR13 318.80-325.00 m

OL-KR14 445.00-449.08 m

OL-KR15 449.62-456.00 m

OL-KR19 155.17-156.98 m

OL-KR21 275.77-281.00 m

Single fault planes at OL-KR7 577.41-586.35 m

OL-BFZ005 is a brittle fault zone with an average dip direction/dip of 167°/28° and a mean fault vector trend/plunge of 181°/25°. The sense-of-shear of the fault either reverse or normal, i.e. the hanging wall block has moved either down the dip of the fault plane or uup the dip. The kinematic data of the sense-of-movement is not consistent, and accordingly no resolution can be given on the absolute direction of movement. The zone has been correlated into six different drillhole intersections (Fig. 7-13) based on observed fault plane orientations in drillholes and on observed VSP reflectors. The zone intersects drillholes OL-KR13, OL-KR14, OL-KR15, OL-KR19, OL-KR21 and OL-KR7 at the drillhole lengths indicated in the tabulated data above.

Geological properties of drillhole intersections

OL-KR13, 318.80-325.00 m

The intersection of the fault zone in drillhole OL-KR13 is composed of TGG gneiss and contains 14 fractures, with an approximate fracture frequency of 2-3 fractures/m. These fractures have a random direction with moderate to steep dip. The intersection has also 5 fractures with slickensided surfaces, which have two main dip directions towards the E and S with a gentle to steep dip. The fault vectors have also two main directions – towards the E and S (corresponding to group A faults), with a gentle dip. The rock in the intersection is strongly foliated.

OL-KR14, 445.00-449.08 m

The intersection is composed mainly of veined gneiss, but in the end of the intersection there are also sections of mafic gneiss and mica gneiss. The intersection contains 28 fractures, which have a dip/dip direction maximum towards the SE with a moderate dip. The average fracture frequency in the intersection is 7 fractures/m. The central part of the intersection contains two sections (446.40-446.83 m and 447.68-448.13 m) of intensely fractured and partly crushed rock. The latter section contains slightly altered feldspars with white- to green- coloured alteration products and it also has grey clay

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fillings. The majority of the fractures (16) in the intersection have a slickenside surface with two different fault vector orientation maxima, one towards the NE and the other towards the SE. The striations have a moderate plunge. Seven of these slickensided fracture surfaces indicate reverse movement. Mechanical fracturing has occurred during the drilling.

OL-KR15, 449.62-456.00 m

The intersection is composed of mica gneiss and contains a few old and welded calcite-bearing fractures. The fractures are randomly orientated with horizontal to moderate dip. The intersection contains 53 fractureswith a more fractured part at drillhole length of 449.85-451.95 m having 36 fractures. Five fractures have slickensided surfaces with a fault vector trend of NE-SW with moderate plunge. Some fractures contain dark, unidentified clay mineral. Mechanical fracturing has occurred during the drilling.

OL-KR19, 155.17-156.98 m

The intersection is composed of veined gneiss and contains old and welded calcite-bearing fractures, which have been reactivated later. The intersection contains 20 fractures with an average fracture frequency of 10 fractures/m. The fractures have a random dip/ dip direction and the intersection has an even distribution of fractures . Most of the fractures show signs of water conductivity, indicated by kaolinite infillings. Mechanical fracturing has occurred during the drilling.

OL-KR21, 275.77-281.00 m

The intersection consists mainly of intensely banded veined gneiss that has been slightly altered to kaolinite and epidote, and short sections of pegmatitic granite containing small garnets. The intersection contains 31 fractures of which 5 have slickensided surfaces. One set of fractures is parallel to the foliation, with a dip direction/dip of 173°/30°. The slickensided fracture surfaces have fault vector orientations in a NNE-SSW direction plunging towards the north at 40°. The fractures have kaolinite and epidote fillings.

OL-KR7, 577.41-586.35 m

The zone is correlated to single fault planes in drillhole OL-KR7 at 577.41-586.35 m. drillhole length interval contains five slickensided fracture surfaces with a moderate dip towards the S-SSE and fault vectors plunging gently towards the S-SSW.

114

Figure 7-13. A) Brittle fault zone OL-BFZ005 viewed from the east, B) and from above.

a)

b)

115

Brittle fault zone OL-BFZ028

DIMENSIONS (X/Y/Z) 42 m/402 m/300 m

DIP DIRECTION/DIP 269°/82°

FAULT VECTOR ORIENTATION 187°/11°

FAULT GROUP A

SENSE-OF-MOVEMENT Right-reverse

CONFIDENCE 3

INTERSECTIONS OL-KR13 362.75-374.46 m

OL-BFZ028 is a brittle fault zone with an average dip direction/dip of 269°/82° and a mean fault vector plunge/trend of 187°/11°. The sense-of-shear of the fault is right-reverse, i.e. the hanging wall block has moved up-the-dip of the fault plane. The zone has been correlated into one drillhole intersection (Fig. 7-14) based on observed fault plane orientations in drillhole and on observed VSP reflectors.

Geological properties of drillhole intersections

OL-KR13, 362.75-374.46 m (connected to BFZ092)

The intersection of the zone in OL-KR13 is mainly composed of foliated TGG gneiss and one section of quartz gneiss at 372.12-373.30 m. The intersection contains signs of palaeoshearing with old welded fractures with greyish matrix and calcite infillings. The intersection contains 51 fractures with an average fracture frequency of 4 fractures/m. The fractures are randomly oriented with steep dips. The intersection has 11 fractures with slickenside surfaces, which are randomly orientated (moderate dip). At drillhole length of 363.23-363.70 m, the drill core is crushed, corresponding most likely to the core of the fault.

116

Figure 7-14. A) Brittle fault zone OL-BFZ028 viewed from the east, B) and from above.

a)

b)

117

Brittle fault zone OL-BFZ060

DIMENSIONS (X/Y/Z) 360 m/130 m/180 m

DIP DIRECTION/DIP 130°/34°

FAULT VECTOR ORIENTATION 223°/12°

FAULT GROUP B

SENSE-OF-MOVEMENT Normal

CONFIDENCE 3

INTERSECTIONS OL-KR22 188.45-200.50 m

OL-KR28 170.21-178.30 m

OL-BFZ060 is a brittle fault zone with an average dip direction/dip of 130°/34° and a mean fault vector trend/plunge of 223°/12°. The sense-of-shear of the fault is normal, i.e. the hanging wall block has moved down the dip of the fault plane. The zone has been correlated into two drillhole intersections in OL-KR22 and OL-KR28 based on observed fault plane orientations in the drillhole and on observed charge potential connections (Fig. 7-15).

Geological properties of drillhole intersections

OL-KR22, 188.45-200.50 m

This intersection is composed of diatexitic gneiss with a slightly banded texture and contains 79 fractures and has an average fracture frequency of 6-7 fractures/m. At least 10 of these fractures have slickensided surfaces. Some old and healed fractures with calcite infillings occur in the beginning of this intersection. The orientations of the fractures are variable, but one clear fracture set parallel to the foliation can be distinguished, having a dip direction/dip of 150°/20°. The slickensided fracture surfaces have nearly horizontal fault vectors and most are NE-SW trending but two E-W trending also occur. Most of the fractures have calcite and pyrite fillings. Some mechanical fracturing of the old and healed fractures may have occurred during the drillings.

OL-KR28, 170.21-178.30 m

The intersection consists mainly of veined gneiss with short sections of pegmatitic granite and mica gneiss. There are approximately 7 fractures/m at 170.21-173.50, two of them being fractures with slickensided surfaces. They seem to be formed in palaeofractures, which may have been reactivated. Old and welded fractures with biotite, pyrite and calcite fillings can be observed. At 172.65-172.70 m the drill core is crushed, corresponding likely to the core of the fault. At 173.50-174.00 m, old welded calcite-bearing fractures occur in the mica gneiss. At 174.12-174.90 m, slickensided fracture surfaces with dip direction towards the NE occur. Pegmatitic granite containing a few fractures in random orientations and with calcite fillings occur at 174.90-175.85 m. In the veined gneiss, red-stained, round K-feldspar crystals also occur; in some places the K-feldspars are also sericitised.

118

Figure 7-15. a) Brittle fault zone BFZ-060 viewed from the east, b) and from above.

a)

b)

119

Brittle fault zone OL-BFZ079

DIMENSIONS (X/Y/Z) 407 m/245 m/270 m

DIP DIRECTION/DIP 161°/27°

FAULT VECTOR ORIENTATION 107°/30°

FAULT GROUP C

SENSE-OF-MOVEMENT Left-normal

CONFIDENCE 3

INTERSECTIONS OL-KR5 269.45-270.68 m

OL-BFZ079 is a brittle fault zone with an average dip direction/dip of 161°/27° and a mean fault vector trend/plunge of 107°/30°. The sense-of-shear of the fault is left-normal, i.e. the hanging wall block has moved down the dip of the fault plane. The zone has been correlated into one drillhole intersection (Fig. 7-16), based on observed fault plane orientations in drillhole and additionally on observed charge potential connections.

Geological properties of drillhole intersections

OL-KR5, 269.45-270.68 m

The intersection is a very intensively fractured section in the veined gneiss. Strong shearing in narrow seams can be observed; in addition, kaolinitisation and illitisation have occurred in the intersection. All the observed fractures are subparallel with each other and concordant to the shearing. In the intersection, fractures with slickensided, stepped surfaces with subhorizontal orientation and gently SE-plunging fault vectors can be observed. In WellCAD-image, 1 - 2 open fractures can be seen.

120

Figure 7-16. a) Brittle fault zone BFZ-079 viewed from the east, b) and from above.

a)

b)

121

Brittle fault zone OL-BFZ092

DIMENSIONS (X/Y/Z) 360 m/480 m/210 m

DIP DIRECTION/DIP 111°/38°

FAULT VECTOR ORIENTATION 142°/32°

FAULT GROUP E

SENSE-OF-MOVEMENT Right-reverse

CONFIDENCE 3

INTERSECTIONS OL-KR13 362.75-374.46 m

OL-KR19 209.86-211.53 m

OL-KR20 177.60-181.05 m

OL-BFZ092 is a brittle fault zone with an average dip direction/dip of 111°/38° and a mean fault vector trend/plunge of 142°/32°. The sense-of-shear of the fault is righ-reverse, i.e. the hanging wall block has moved down the dip of the fault plane. The zone has been correlated into three drillhole intersections based on observed fault plane orientations in the drillholes (Fig. 7-17). The zone intersects drillholes OL-KR13, OL-KR19 and OL-KR20 at the intervals indicated above.

Geological properties of drillhole intersections

OL-KR13, 362.75-374.46 m (connected to BFZ028)

The intersection of the zone in OL-KR13 consists mainly of foliated TGG gneiss and one section of quartz gneiss at drillhole length of 372.12-373.30 m. The intersection contains signs of paleoshearing with old welded fractures having a greyish matrix and calcite infillings. The intersection contains 51 fractures with an average fracture frequency of 4 fractures/m. The fractures have a random direction with steep dip. The intersection has 11 fractures with slickenside surfaces, which are randomly orientated (moderate dip). At 363.23-363.70 m the drill core is crushed, thus most probably corresponding to the core of the fault.

OL-KR19, 209.86-211.53 m

The intersection consists of veined gneiss and contains a few old, welded, calcite-bearing fractures, which have been partly reactivated later. The intersection has an average fracture frequency of 7 fractures/m, with a total of 14 fractures. The orientations of the fractures are quite scattered. Four fractures with slickenside surfaces can also be observed. They have a moderate dip towards the SE and fault vectors plunging gently towards the E-SE. Some of the slickensides seem have formed in paleofractures, which have been reactivated later.

OL-KR20, 177.60-181.05 m

The intersection consists of pegmatitic granite and contains a few old and welded fractures with white calcite fillings. The intersection contains a total of 29 fractures, the

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average fracture frequency of the intersection being approximately 8 fractures/m. The dip directions of the fractures vary between the E and SE with dips from almost horizontal to moderate. The intersection contains one slickensided surface at along-the-hole depth of 181.05 m, with a SE-trending, moderately plunging fault vector. Some of the fractures are concordant with the foliation. The intersection is evenly fractured.

Figure 7-17. a) Brittle fault zone BFZ-092 viewed from the east, b) and from above.

a)

b)

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Brittle fault zone OL-BFZ093

DIMENSIONS (X/Y/Z) 540 m/320m/750 m

DIP DIRECTION/DIP 139°/29°

FAULT VECTOR ORIENTATION 152°/26°

FAULT GROUP E

SENSE-OF-MOVEMENT Right-normal

CONFIDENCE 3

INTERSECTIONS OL-KR4 791.00-792.00 m

OL-KR7 689.90-692.00 m

OL-KR29 745.70-747.30 m

OL-BFZ093 is a brittle fault zone with an average dip direction/dip of 139°/29° and a mean fault vector trend/plunge of 152°/26°. The sense-of-shear of the fault is right-normal, i.e. the hanging wall block has moved down the dip of the fault plane. The zone has been correlated into three drillhole intersections (Fig. 7-18) based on observed fault plane orientations in drillholes. The zone intersects drillholes OL-KR4, OL-KR7 and OL-KR29 at the intervals presented above.

Geological properties of drillhole intersections

OL-KR4, 791.00-792.00 m

The intersection consists of sheared mica gneiss, which is visible in the whole intersection but especially at the contact of pegmatitic granite. The mica gneiss is strongly altered, i.e. chloritised and illitised. The drill core in the intersection is totally crushed and contains at least 13 fractures. Due to the crushed nature of the core, no orientations of the fractures can be determined. Most of the fractures have smooth surfaces.

OL-KR7, 689.90-692.00 m

At the drillhole length of 689.90-692.00 m in OL-KR7, the rock is completely crushed and split. The intersection is located within a mica-rich migmatitic gneiss inside an intact pegmatitic granite section. Above the crushed section, there is ca. 5 m and below ca. 3 m of unfractured pegmatitic granite. Fault gouge can be observed in the intersection in the form of clay. The intersection contains 34 fractures and the average fracture frequency is 16 fractures/m.

OL-KR29, 745.70-747.30 m

The intersection consists of diatexitic gneiss and contains plenty of old and welded fractures with calcite fillings. The intersection has 18 fractures and an average fracture frequency of 11 fractures/m. The fractures dip towards the N or S with a shallow dip. The intersection contains 5 fractures with slickensided fracture surfaces, three of which

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have a fault vector direction towards the N or S-SE with a moderate plunge. The fault planes dip gently towards the SE.

Figure 7-18. a) Brittle fault zone BFZ-093 viewed from the east, b) and from above.

a)

b)

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7.2.2 Observed brittle fault or joint zones

The model also includes three fault or joint zones, which have been observed in the investigation trenches and in the ONKALO access tunnel, and which have a confirmed orientation and properties (Fig. 7-19).

Figure 7-19. Observed fault or joint zones in the ONKALO area.

Brittle fault zone OL-BFZ100

DIMENSIONS (X/Y/Z) 37 m/3240m/100 m

DIP DIRECTION/DIP 090-120°/55-70°

FAULT VECTOR ORIENTATION 040°/20°

FAULT GROUP B

SENSE-OF-MOVEMENT Strike-slip, small component of normal dip -slip

CONFIDENCE 3

INTERSECTIONS OL-KR25 94.45-97.30 m

OL-KR26 95.80-98.25 m

ONK-PH1 151.64-154.32 m

OL-TK7 P8 3.47-4.00 m

ONKALO 128.50-129.30 m

ONKALO 521.50-523.00 m

ONKALO 900.20-906.40 m

OL-TK11 C20-S25

Weatheredzone

”Storagehall fault”

Subhorizontalzone

126

Fault zone OL-BFZ100 (the ’storage hall fault’) was first observed in the geological mapping of trenches OL-TK7 and OL-TK11 (Fig. 7-20). Later, it was also found in drillholes OL-KR25, OL-KR26 and ONK-PH1 and in the ONKALO access tunnel (Fig. 7-21). It can also be seen in the seismic refraction data as a zone of lowered P-wave velocity (Vp 4000 – 4500 m/s). OL-BFZ100 is a brittle fault zone with dip direction/dip varying from 090-120°/55-70° and a mean fault vector trend/plunge of 040°/20°. The sense-of-shear of the fault is sinistral strike-slip, with a small component of normal dip-slip movement, i.e. the hanging wall block has moved subhorizontally down the dip of the fault plane.

Geological properties of the intersections

OL-TK11, mapping sections C20-S25

The eastern part of the investigation trench is intersected by a continuous fracture zone, which can be defined as a brittle fault based on the observed kinematic indicators (Fig. 7-19). The trace length of the fault is approximately 50 metres and it has an average corresponding trace direction of 015°. The average dip direction/dip of the fault plane is 110°/65°. The continuity of the fault outside the trench area is unknown but the visible part of the fault runs through mapping sections C20 and S25. The fault splays into two different fault planes in the southern part of the investigation trench but the continuation of the secondary fault plane is also unknown. The fault consists of a clearly definable core and transition zone; the core has a varying width of 0.15 to 2 metres and has in places strongly developed schistose fabric with associated slickensided surfaces. Quartz, pyrite, chalcopyrite, graphite, galena and talc mineralisations can be observed within the fault core. Pyrite mineralisation occurs within cavities associated with quartz-filled tension veins. Where the fault splays into two different planes, the rock is strongly broken by intensive fracturing.

The transition zone forms an area where the fracture density is higher than in the rest of the excavated area. The width of the transition zone varies and cannot be explicitly measured, as it seems to continue outside the trench area on the eastern side of the fault core. Nevertheless, on the western side of the fault, the transitional area with higher fracture density has a varying width of 2 to 6 metres. In addition to the higher fracture density, the transition zone is also characterised by long, planar and vertical synthetic and antithetic secondary Riedel-fractures (R- and R’-fractures, respectively)

The fault shows sinistral sense of movement by numerous kinematic indicators. In the core of the fault, in sections O24 and P24, quartz-filled tension veins show clear sinistral vergeance in a horizontal plane. The fault also crosscuts an older, east-west striking ductile shear zone, which shows sinistral deflection towards the fault core. Based on the crosscutting relationship and the amount of deflection of the older shear zone it can be estimated that within the fault the sinistral horizontal movement has been at least 2 metres. Sinistral sense of shear is also supported by the existence of planar secondary Riedel shear fractures or R-fractures, which form an approximate angle of 15 to 25 degrees (trace of 160-170°) to the fault core, or the P-shear plane. Planar R’-

127

fractures, which are less developed than the R-fractures, have an approximate angle of 5-15 degrees (trace of 110-120°) to the main fault plane.

OL-TK7, mapping section P8, 3.47-4.00 m

The fault zone in OL-TK7 is a brittle fault intersection with calcite- and chlorite-coated fractures having an approximate dip direction/dip of ca. 085°/75°.

OL-KR25, 94.45-97.30 m

The intersection consists of veined gneiss. The intersection contains old and welded fractures where pyrite and some calcite are present as fillings. These old fractures have been partly reopened during drilling. The rock in the intersection has a well-developed foliation and the fracturing is concordant to it. All the fractures have a NE-SW direction and a moderate dip. The intersection contains 21 joints, and the average fracture frequency is 7 fractures/m. The rock is weathered, crushed and altered at 96.35-96.66 m. Some mechanical fracturing has occurred during the drillings.

OL-KR26, 95.80-98.25 m

The intersection consists of diatexitic gneiss and contains old and welded fractures where calcite is present. These old fractures have been partly reactivated later. The fractures seem to have a random direction but no certainty on the orientations could be established because of a lack of an OPTV image and oriented core. The intersection contains 28 fractures with and average fracture frequency of 11 fractures/m. The rock is most fractured in the section 97.24-97.64 m, which has 14 fractures, i.e. the fracture frequency is 35 fractures/m. This section probably represents the core of the fault. Some mechanical fracturing has occurred in the core during the drilling.

ONK-PH1, 151.64-154.32 m

The intersection consists of heterogeneous and altered pegmatitic granite with biotite-rich schlieren; the K-feldspars are mainly altered into chlorite and sericite. The majority of the fractures in the intersection contain chlorite and some have a light greenish clay filling. The intersection contains 34 fractures, corresponding to an average fracture frequency of 12 fractures/m. A few old and welded fractures with calcite fillings can be observed. 3 fractures with slickensided surface are present but due to a lack of OPTV image and an oriented core, no directions could be measured. Some of the fractures are, however, parallel to foliation. Mechanical fracturing has occurred during the drilling.

ONKALO, chainage 128.50-129.30 m

The intersection consists of veined gneiss and the fault intersection is visible across the whole tunnel and has a trace length of approximately 15-20 metres. The fault plane has an average dip direction/dip of 115°/70° and it crosscuts the foliation. The width of the zone at the tunnel roof is approximately 4 metres, but in the lower part of the tunnel, fault planes combine into an intersection with a width of 20 cm. Calcite-filled tension veins can be observed. The fault vector of the zone has a trend/plunge of 044°/11° and

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is visible in some of the slickensided fractures with striated and stepped characteristics. The slickensided fracture surfaces and tension veins indicate sinistral strike-slip type of movement with a small component of normal-dip-slip sense-of-movement.

The fault has a thin core of a width of 5-10 cm, composed of crushed rock with rock pieces up to 20 mm in diameter, and grey-greenish clay/silt. The core can be defined as fault breccia, as 70-80% of the material consists of rock pieces. In places the core material shows the development of strong tectonic fabric.

Within the fault pyrite, chalcopyrite, galena and graphite mineralisation are common. Chalcopyrite seems to be associated with calcite-filled fractures/tension veins.

ONKALO, chainage 521.50-523.00 m

The intersection, consisting mainly of veined gneiss, contains approximately ten slickensided fracture surfaces with a well-developed lineation. The core of the fault is approximately 5-25 cm in width and consists of fault breccia, with crushed rock pieces and material varying from clay fraction up to 4 cm in diameter. The core also contains unidentified greyish black clay. Within the core, lenses approximately 5-35 cm wide can be observed; they have a dip direction/dip of 284°/89° and 098°/86°. There are also some fractures with calcite and pyrite fillings.

The fault plane has an average dip direction/dip of 284°/89° and corresponding fault vector orientation of 012°/14°.

ONKALO, chainage 900.20-906.40

The fault zone consists of two nearly vertical main faults (with a separation of ca. 5 m between them) that cut through the tunnel and many smaller vertical slickensided fracture surfaces that join the main faults. The faults have 0.5-4 cm thick fillings of pyrite, calcite, clay, graphite, and chlorite. The rock is very densely fractured between the main faults and many fractures both parallel to the foliation and randomly orientated are present. The rock is highly crushed and altered in the vicinity of the main faults and therefore the displacement is hard to observe. On the basis of bent foliation and striations on the fault plane, the fault seems to be dextral in the right tunnel wall.

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Figure 7-20. Brittle fault zone OL-BFZ100 in investigation trench OL-TK11 (Mattila et

al., in prep). Photo by Matti Talikka, Geological Survey of Finland.

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Figure 7-21. a) Brittle fault zone BFZ-100 viewed from the east, b) and from above.

a)

b)

131

Brittle fault zone OL-BFZ101

DIMENSIONS (X/Y/Z) 70 m /24 m/14 m

DIP DIRECTION/DIP 116°/11°

FAULT VECTOR ORIENTATION

FAULT GROUP

SENSE-OF-MOVEMENT

CONFIDENCE 3

INTERSECTIONS ONK-PH1 98.05 – 99.76 m

OL-PR5 4.24 – 4.64 m

OL-PR6 5.55 – 6.00m

OL-PR7 756 – 8.09 m

OL-PR8 11.90 – 12.30 m

OL-PP40 17.85 – 18.53 m

OL-PP41 27.10 – 27.89 m

ONKALO 67.56 – 68.23 m

The ground penetrating radar (GPR) survey performed in investigation trench OL-TK7 indicated a subhorizontal fracture (fault?) zone (OL-BFZ101) between mapping sections P13 and P17 (Sutinen 2003). In OL-TK7, the zone can be seen as a gently dipping surface parallel to the foliation (Paulamäki 2005b). This fracture zone is intersected by several short drillholes: OL-PR5, OL-PR6, OL-PR7, OL-PR8, OL-PP41 and, probably, OL-PP40. The feature detected using GPR and the short drillholes is correlated with a clay-structured (RiV) zone at 98.05-99.76 m in pilot drillhole ONK-PH1, in which fractures with 2 – 40 mm thick infillings of grey clay mineral powder, together with some illite and kaolinite, have been detected. The rock in this drillhole section is strongly to completely weathered with core loss of more than 1.05 m and the rods dropped several times during the drilling (Niinimäki 2004). This fracture zone is observed in the ONKALO access tunnel at 67.56 – 68.23 m.

Brittle joint zone OL-BJZ102

DIMENSIONS (X/Y/Z) 314 m/379 m/111 m

DIP DIRECTION/DIP 110-170°/ca. 40-60°/

FAULT VECTOR ORIENTATION

FAULT GROUP

SENSE-OF-MOVEMENT Sinistral strike-slip

CONFIDENCE 3

INTERSECTIONS OL-KR25 122.00-122.11 m

ONK-PH2 118.50-121.31 m

ONKALO 240.00- 282.00 m

ONKALO 449.70-453.30 m

OL-TK4 P48-49, P58-59

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The weathered zone OL-BJZ102 (Fig. 7-17) has been modelled on the basis of seismic P-velocities, charge potential survey, and observations in investigation trench OL-TK4, in drillhole ONK-PH2 and in the ONKALO access tunnel. The zone appears as strongly weathered, altered and fractured section in PH2 at 118.50-121.31 m, corresponding to 253.09-256.90 m in the access tunnel, and it is connected to about 16 m wide weathered and fractured zone in mapping sections P58 and P59 in OL-TK4 ca. 10 m north of the access tunnel profile (see Paulamäki 2005a) (Fig. 7-22A). The rock in both sections is strongly broken mainly along the foliation planes. Feldspars in the granite veins are altered to sericite, saussurite, kaolinite and probably illite. The mica gneiss mesosome is sericitised, chloritised and kaolinitised. In PH2, the feldspar is strongly altered to kaolinite, illite and other clay minerals. The strongly weathered section in mapping sections P48-P49 in TK4 is also connected to this zone. In the beginning of section P48, there is 1.3 m wide zone, in which the mica gneiss is completely weathered to greenish clayey material. The zone is present in the ONKALO access tunnel chainages 240-282 m (Fig. 7-20B) and 449.70-453.30 m, where it is a sheared and altered zone, the clearest alterations being visible in the kaolinisation of feldspar grains and chloritisation of biotite. In the latter intersection, the rock is intensively kaolinitised, and in the centre of this intersection there is a strongly sheared zone, with a width of 30-100 mm. The dip direction/dip of shearing is 158°/56°, which is same as the orientation of the foliation. The surrounding rock is also pervasively kaolinitised.

Figure 7-22. A) Weathered zone OL-BJZ102 in mapping section P58 in investigation

trench OL-TK4. B) OL-BJZ102 in the ONKALO access tunnel, chainage 280 m. Photos

by Seppo Paulamäki, Geological Survey of Finland (A) and Kimmo Kemppainen,

Posiva Oy (B).

A

B

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7.2.3 Possible brittle fault zones

In addition, the model includes two zones (OL-BFZ098 and OL-BFZ099; Fig. 7-23) interpreted on the basis of charge potential measurements in drillholes and also observed as highly fractured intersections in drill cores. However, these may not represent fracture zones, since they are simply zones of higher electrical conductivity, which can reflect the effect of groundwater and/or graphite and sulphide mineralisations. Nevertheless, the geophysical anomalies of these two zones are so evident that, because of need for conservatism, their properties should be carefully assessed in respect to long-term safety. In the volume of these zones, several of the fault zones shown in Figs. 7-5 to 7-10 occur and, consequently, the zones are thought to represent the combined effect of brittle faulting and associated fracturing and mineralisations of conductive minerals. This kind of behaviour of brittle faults is typical in nature: fault zones are often segmented and connected in a step-like manner by fracture networks, and as such, fault zones are discontinuous and non-planar (cf. Milnes et al. in prep. and references therein).

Figure 7-23. Two possible fault zones OL-BFZ098 and OL-BFZ099 interpreted on the

basis of charge potential survey in drillholes.

BFZ098

BFZ099

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7.3 Correlation to previous bedrock model

The previous bedrock model (Vaittinen et al. 2003) contains 140 directly observed structures. Most of the structures (121) have only one drillhole intersection, and they have a code containing the drillhole identification code (KR01, KR02, etc.), a sequence number from top to bottom and a descriptive attribute ‘R’ (fracturing), ‘H’ (hydraulic conductivity), or ‘RH’ (both). Those structures (19), which have been correlated from one drillhole to another or from one drillhole to the surface are called ‘R’-structures, ‘H’ -structures or ‘RH’ –structures. In total the model contains 94 fractured structures and 68 hydraulic structures.

The definitions of structural intersections in the previous bedrock model are based on fracture frequency, hydraulic conductivity, and mapped fracturing class. The orientation of structures is mostly based on hydraulic responses between the drillholes or on oriented fractures determined either from core samples or optical drillhole images. Some structures have been oriented using the seismic and drillhole radar measurements. As described in Chapters 2.1.2 and 7.1, the definition of the structural intersections in the present model is based on expert judgement and not on any specific fracture frequency and the orientation is determined on the basis of kinematic data of the slickensided fracture surfaces (faults).

Table 7-5 shows the interpreted brittle fault zones and their orientation of the present model, which have a correspondence in the previous bedrock model . Although a certain correspondence can be found between the two models in terms of the location of the brittle structures, the orientations of the structures in most case do not match.

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Table 7-5. Interpreted brittle fault zones and their orientation of the Olkiluoto site area model v. 0, which have a spatial correspondence in the previous bedrock model 2003/1.

Site area model v.0 Dip direction/dip

(°)

Bedrock model

2003/1

Dip direction/dip

(°)OL-BFZ001 224/11 KR06_12R 000/00 OL-BFZ002 180/17 RH21, RH9, KR02_7R 165/19, 141/49,

170/40 OL-BFZ004 210/17 R2 (KR19_7R) 174-183/68 OL-BFZ005 167/28 KR15_4R 090/60 OL-BFZ006 235/45 RH20C 115/24 OL-BFZ007 108/33 KR19B_3RH - OL-BFZ008 107/10 RH26 (KR13_2RH) 137/20 OL-BFZ009 173/26 KR21_3R - OL-BFZ010 190/50 R10A 155/41 OL-BFZ011 095/15 RH24 139/33-63 OL-BFZ016 205/23 KR08_11R 315/30 OL-BFZ018 150/36 RH19A

KR22_4RH 000/03 -

OL-BFZ026 179/53 KR01_6R 180/40 OL-BFZ027 180/31 ? OL-BFZ028 269/82 KR13_8R 090/70 OL-BFZ038 174/28 RH9 (KR20_5R) 141/49 OL-BFZ040 155/37 RH26 137/20 OL-BFZ042 129/35 KR13_10R 140/75 OL-BFZ045 140/37 KR13_9R 130/70 OL-BFZ047 154/19 KR19B_4H - OL-BFZ049 090/20 KR06_12R 000/00 OL-BFZ050 112/50 R78 (KR17_3R) 115/38 OL-BFZ051 105/08 RH19B (KR04_2RH)

R24B (KR08_8R) 180/23 150/40

OL-BFZ052 170/44 KR15_4R 090/60 OL-BFZ059 140/47 KR22_4RH - OL-BFZ060 130/34 KR22_5R - OL-BFZ062 142/35 RH21 (KR05_8R) 165/19 OL-BFZ064 158/40 R21 (KR02_8RH) 165/19 OL-BFZ065 099/38 KR19_12R 120/30 OL-BFZ067 120/36 RH26 (KR12_2R) 137/20 OL-BFZ072 143/41 RH20C (KR13_6R) 115/24 OL-BFZ073 150/47 RH20A (KR07_3RH) 137/18 OL-BFZ074 043/51 RH19A (KR08_3RH) 000/03 OL-BFZ075 172/32 KR15_4R 090/60 OL-BFZ076 148/36 KR13_10R 140/75 OL-BFZ077 170/45 R56 (KR07_9R) 191/59 OL-BFZ079 161/27 RH9 (KR05_5R) 141/49 OL-BFZ084 182/64 R10A (KR03_3R) 155/41 OL-BFZ085 185/58 KR01_2RH (RH11_ALT,

RH20_ALT) 135/45

OL-BFZ086 141/37 R78 (KR17_3R) 115/38 OL-BFZ092 111/38 KR13_8R

KR20_3R 090/70 150/40

OL-BFZ093 139/29 RH21 (KR07_10R) 165/19 OL-BFZ094 117/74 KR12_15R - OL-BFZ095 093/13 KR19_4R 170/30 OL-BFZ096 244/85 KR12_5R 245/60

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7.4 Correlation to ONKALO area model version 0

In the ONKALO area model, the faults have been divided into three main fault groups: 1) subhorizontal faults with fault vector plunging gently towards the SSW or NNE, 2) vertical to subhorizontal faults with fault vector plunging gently towards the NE or SW, and 3) subhorizontal faults with fault vector plunging gently towards the ESE. The orientation data, 1700 fault planes and fault striation orientations, and sense-of-shear of the faults, is the same as in the present model. The basic difference between the two models is that in the ONKALO area model, the modelled structures can be both brittle fault intersections and individual faults, whereas in the Olkiluoto site area model, in principal, only the brittle fault or joint intersections have been modelled.

The ONKALO area model contains 38 faults or fault zones. In addition, the model includes three observed fault or fracture zones and two possible zones, interpreted on the basis of charge potential survey in drillholes, and these are also included in the present model.

7.5 Intersections with ONKALO underground rock characterisation facility

Only a few modelled fault or joint zones intersect the access tunnel of the underground rock characterisation facility (ONKALO) (Fig. 7-24). The zones, which intersect the access tunnel, are listed in Table 7-6.

Figure 7-24. Modelled brittle fault and joint zones in the vicinity the ONKALO access

tunnel. View from the W.

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Table 7-6. Intersections of the modelled brittle fault zones (BFZ) and joint zones (BJZ) in the access tunnel of the ONKALO underground rock characterisation facility.

Fault zone Chainage (m) Dip direction/dip (°) OL-BFZ016 2840-2860 205/23 OL-BFZ018 970-980 150/36 OL-BFZ034 1715-1725 165/89 OL-BFZ043 2145-2150, 3955-3960 115/78 OL-BFZ051 958-964 105/08 OL-BFZ059 595-605 140/47 OL-BFZ077 3575-3585 170/45 OL-BFZ088 1425-1430 073/24 OL-BFZ100 123.5-124.5, 521.5-532, 901-903 090-120/55-70 OL-BFZ101 67-67.5 116/11 OL-BJZ102 240-282, 449-453 110-170/40-60

7.6 Evaluation of implications for construction

The modelled zones represent either joint cluster or brittle fault zones, i.e. the rock mass within the modelled zones has lost its internal cohesion on certain surfaces due to brittle deformation. Accordingly, the modelled zones and their intersections with the ONKALO underground rock characterisation facility are potential places where the rock mass is likely to be more fractured than the surrounding host rock and therefore these zones may cause difficulties for the construction (as rock enforcement may be necessary and the excavation process may be slowed down). Water conductivity of the zones, which is not assessed in this model, may be high in certain tunnel intersections of the zones and this may also cause additional difficulties for the construction. The properties of the modelled zones and their effects on the construction needs to be carefully assessed zone-specifically, but it must be emphasised that natural brittle deformation products, e.g. faults, are always in nature discontinuous and non-planar and therefore prediction of the properties of the modelled zones, based only on the current model, always contains uncertainty. Brittle faults typically have so called ‘fault damage zones’ or ‘transition zones’ which are areas of higher fracture intensity around the core, or the most deformed part of the fault, and extend several meters away from the core. Consequently, the effective width and the implication for construction of a modelled zone may in reality be much wider than can be seen in the modelled solids. Therefore the drilling of pilot holes within the tunnel perimeter should be favoured as these provide detailed information on the properties of intersected zones and may effectively change decisions concerning construction, tunnel design and safety aspects as the uncertainty on the properties of brittle zones is greatly reduced.

The effect of brittle deformation zones on construction will depend on the orientation of the zones. This is an important factor, which needs to be taken into account. Zones cross-cutting the tunnel perimeter at a low angle have long intersections with the tunnel (e.g. tens of metres – several excavation rounds) and are much more likely to cause more problems than zones crosscutting at a high angle. Estimated orientations of zones modelled to intersect the ONKALO tunnel are presented in Table 7-6.

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7.7 Lineament map

A new lineament interpretation of the Olkiluoto area was presented in 2005 (Korhonen et al. 2005). A lineament is a straight or curved feature, which can be seen, e.g., in topographic maps, air photos or aeromagnetic maps. Lineaments can indicate a geological feature, for example a shear or fault structure but not necessarily. The interpretations data in this case comprises both geophysical and topographic data. The geophysical data included magnetic and electromagnetic (EM) data from aerogeophysical surveys, magnetic, EM, and seismic data from ground surveys, and acoustic data from a marine survey. The topographic data was composed of two digital elevation models and 5-metre elevation contours. The digital elevation models used were the 25-metre pixel-size National Land Survey (NLS) digital elevation model (DEM) of Finland and a detailed DEM of the Olkiluoto island.

The lineament interpretation was performed in three phases according to the methodologies developed by the Swedish Nuclear Fuel and Waste Management Co (SKB) and described in the method descriptions SKB MD 120.001 (Metodbeskrivning för lineamentstolkning baserad på topografiska data) and SKB MD 211.003 (Metodbeskrivning för tolkning av flyggeofysiska data). In the first phase, each method-specific data set was interpreted separately. In the next phase, those method-specific lineaments that describe the same linear feature were coordinated. Finally, the coordinated lineaments assumed to describe the same linear feature were linked into a single lineament. The method-specific lineament interpretation has a total of 1334 lineaments, which dropped to 998 lineaments in the coordinated lineament interpretation phase. The final lineament interpretation of the Olkiluoto study site has 609 linked lineaments (Fig. 7-23).

All the modelled brittle fault zones and the brittle and semi-brittle fault and joint intersections observed in the investigation trenches have been checked against the lineament data but the correlation has been rather poor. Not a single modelled fault zone could have been connected to the interpreted lineaments. Moreover, from 34 method specific or linked lineaments intersecting the investigation trenches, only 13 intersect the trenches at places with observed brittle fault or joint intersection. Using the observed fault or joint orientation in the trenches, these 13 lineaments were modelled in 3D to check, if they could be connected to the brittele joint or fault intersections in the drillholes. The results were very contradictory and no lineaments could be positively connected to drillholes. The results indicate that most of the interpreted lineaments, at least within the Olkiluoto site area, may be some features other than the brittle fault zones. Thus, at this phase of the modelling, the interpreted lineaments have not been incorporated into the brittle deformation model. In the future, the lineaments should be thoroughly analysed, e.g., by targeted drilling, trenching, validated geophysics, and so on.

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1520000

1520000

1525000

1525000

1530000

1530000

67

90

000

67

90

000

67

95

000

67

95

000

0 1 2 3 4 5

km

Linked lineaments

Medium uncertainty (1.5 - 2.5)

Low uncertainty (< 1.5)

High uncertainty (> 2.5)

Figure 7-25. Linked lineaments classified by their uncertainties (Korhonen et al. 2005).

140

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8 SELECTED FRACTURE STATISTICS

8.1 Surface fractures (outcrops and trenches)

A total of 7628 fractures have been measured from outcrops and from nine 400 - 800 m long and 1 - 5 m wide investigation trenches (OL-TK1 – OL-TK9). The distribution of all the fracture orientations measured is shown in Fig. 8-1 as Schmidt equal area, lower hemisphere projection. The fracture data has not been corrected for orientation sampling bias. Fractures striking parallel or sub-parallel to the foliation (see Fig. 5-3) are dominant but the dips are variable. However, two main maxima can be seen (157/37° and 172/82°) but also fractures dipping steeply in the opposite direction are common (Fig. 8-2A). Another fracture cluster is formed by fractures striking approximately N-S and dipping steeply to the west or east. Figures 8-2 and 8-3 show the orientation of fractures by rock types. The distribution of fractures is rather similar in all rock types, except in the diatexite, where the fractures are more widely distributed compared to the other rock types. The diatexites are located in the area, where the ductile D4 deformation with ca. NNE-SSW trend dominates (see Chapter 5.1) and this can be clearly seen in the fracture orientation. In addition, N-S striking fractures are more pronounced in the TGG gneisses.

The vast majority of the measured fractures show no indications of fault movement. However, a few N-S or NW-SE striking faults have been observed with a displacement of 1-11 cm (Paulamäki & Koistinen 1991, Paulamäki 2005a, Engström 2006.)

A) B)

Figure 8-1. Orientation of fractures (dip direction/dip) in outcrops and investigation

trenches OL-TK1 – OL-TK9 (N = 7593). A) contoured strereogram, B) pole stereogram

(Schmidt equal area, lower hemisphere projection). 5° declination not added.

142

A)

C)

A)

B)

C)

Figure 8-2. Orientation of fractures (dip direction/dip) by rock types in outcrops and

investigation trenches OL-TK1 – OL-TK9. A) Veined gneisses (N = 2186), B) mica

gneisses (N = 1695) and C) tonalitic-granodioritic-granitic gneisses (N = 1446).

Contoured stereograms and pole stereograms (Schmidt equal area, lower hemisphere

projection). 5° declination not added.

143

A)

B)

Figure 8-3. Orientation of fractures (dip direction/dip) by rock types in outcrops and

investigation trenches OL-TK1 – OL-TK9. A) Diatexites (N= 799), B) pegmatitic

granites (N = 1396). Contoured stereograms and pole stereograms (Schmidt equal

area, lower hemisphere projection). 5° declination not added.

The main fracture directions of 1703 recorded fractures from the tonalitic-granodioritic-granitic gneiss and pegmatitic granite in the Ulkopää cape area are NNE-SSW, SSE-NNW and E-W (Sacklén 1994), which correspond well with the orientations determined from the outcrops and the investigation trenches.

During mapping of the outcrops and investigation trenches OL-TK1 – OL-TK7 fractures with an observed trace length of 1 m were mapped, while in investigation trenches TK8 and TK9 all the fractures were mapped. The mean fracture trace length of the measured fractures is 1.78 m. The mean length of the fractures is 1.52 m in the veined gneiss, 1.85 m in the diatexite, 1.67 m in the mica gneiss, 2.22 m in the tonalitic-granodioritic-granitic gneiss, and 1.82 m in the pegmatitic granite. However, due to narrow investigation trenches and the small area of the outcrops, almost two-thirds of the fractures are only partly visible. The percentage of fractures with both ends visible is 37%, while the percentages of singly- and doubly-truncated fractures are 36.2% and 26.8%, respectively. Consequently, the length distribution is badly biased and only a

144

few fractures reach a length of tens of metres or even several metres (Fig. 8-4). Only 0.3% of the mapped fractures have a trace length equal to or more than 10 m, with the longest observed fracture having a trace length of 30 m. Fractures with a trace length equal to or more than 10 m mostly (73%) strike N-S, NNW-SSE or NW-SE.

In terms of the shape of the fractures, they are either straight (51.4%), undulating (38.4%) or curved (10.2%). The fractures are tight (44.4%), open (23.9%), filled (1.9%) or some combination of these three fracture characteristics (29.8%). The fracture filling minerals include chlorite, hematite, carbonate, epidote, mica, kaolinite, pyrite and clay minerals (illite).

Fracture trace lengths

0

500

1000

1500

2000

<0

.5

0.5 1

1.5 2

2.5 3

3.5 4

4.5 5

5.5 6

6.5 7

7.5 8

8.5 9

9.5 10

Trace length (m)

Nu

mb

er o

f fr

actu

res

Figure 8-4. Distribution of fracture trace lengths in outcrops and investigation trenches

TK1-TK9.The range values 0.5 = 0.5-0.99, 1 = 1.00-1.49, 1.5 = 1.50-1.99 etc. Note that

the percentage of fractures with both ends visible is only 37%, while the percentage of

singly- or doubly-truncated fractures is 63%.

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8.2 Fractures in the ONKALO access tunnel

The distribution of all fracture orientations measured in the ONKALO access tunnel chainage 25-990 m is shown in Fig. 8-5. The fracture data has not been corrected for orientation sampling bias. Horizontal or sub-horizontal, southeast-dipping fractures dominate. Another fracture cluster is formed by fractures, which strike approximately N-S and dip steeply to the east or west.

Figure 8-5. Orientation of fractures (dip direction/dip) in the ONKALO access tunnel

chainage 25-990 m (N = 14995). Contoured strereogram, Schmidt equal area, lower

hemisphere projection.

The distribution of the fracture trace lengths in the ONKALO access tunnel is presented in Fig. 8-6. Although the dimensions of the tunnel (height 4.5 m, width 5.5 m) are larger than the investigation trenches and many of the outcrops, the distribution is rather similar to that of the outcrops and trenches shown in Fig. 8-4.

146

Facture trace length, ONKALO tunnel

0

500

1000

1500

2000

2500

0.2

5

1.2

5

2.2

5

3.2

5

4.2

5

5.2

5

6.2

5

7.2

5

8.2

5

9.2

5

10

.3

Trace length (m)

Nu

mb

er

of

fractu

res

Figure 8-6. Distribution of fracture trace lengths in ONKALO access tunnel chainage

0-985 m. 90% of the fractures are visible in their full length.

8.3 Fractures in drillholes

A total of 32 172 fractures have been measured using drillhole wall imagery. Figure 8-7 combines the fracture orientation measurements in drillholes OL-KR1 – OL-KR33. Work was done in 2005 as a part of the structural mapping of Olkiluoto drill cores (see

chapter 2.1.2). All the fracture data is collected into the fracture database and extensive statistical fractures analyses will be carried out at a later date. For drillhole fracture data a correction of sampling bias, caused by one-dimensional sampling in the three-dimensional fracture system (Terzaghi 1965), has been used.

Horizontal fractures or fractures dipping gently (0 - 40º) to the S or SSE following the strike of the foliation (see Fig 5.3) dominate in the fracture data (a maximum in 155/27°). The fracture distribution is strongly influenced by the common foliation strike especially in migmatites, which are mostly foliated. Rare steeply dipping fractures, especially a N-S striking population, appear therefore more visibly in unfoliated TGG gneisses, mafic gneisses, quartzitic gneisses and pegmatitic granites. For instance in TGG sections this maximum is 086/87°. These fractures are also common in surface data (see Fig. 8-1). Also some signs of a weak maximum of steeply dipping E-W striking fractures can be seen. Because of the usually steep dip of the drillholes and a common drilling direction nearly perpendicular to the foliation plane, a strong bias can be assumed accentuating the foliation caused maximum and decreasing the sub-vertical ones.

147

A) B)

C) D)

E) F)

G)

Figure 8-7. Orientation of fractures (dip direction/dip) in drillholes KR1-KR33. A)

veined gneisses (N = 13365), B) diatexites (N = 9008), C) mica gneisses (N = 2004), D)

tonalitic-granodioritic-granitic gneisses (N = 1273), E) quartz gneisses (N = 410), F)

mafic gneisses (N = 452), G) pegmatitic granites (N = 5293). Contoured stereograms

(Schmidt equal area, lower hemisphere projection) with Terzaghi corrections.

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8.4 Statistical modelling of fractures

A statistical model of fractures based on the fracture data from investigation trenches OL-TK7 and OL-TK11, drillholes OL-KR24 and ONK-PH1 and ONKALO chainage PL0 – 140 m has been created by Tuominen et al. (2006) for DFN modelling of the ONK-PH2 area. Fractures were assigned to three sets based on their orientation: a sub-horizontal set dipping towards the southeast, and two vertical sets with N-S and E-W strike. Mean orientations of sets are 139/18°, 089/89° and 177/86°, the first of which has clearly the smallest dispersion. For each set the size distribution and intensity were defined. Influence of data source and geological settings like effects of rock types and deformation zones were analysed. The DFN parameters were defined for migmatites and excluded fractures within any deformation zone. The work of Tuominen et al. (2006) was a first attempt to statistically describe fracture data mapped from ONKALO, boreholes and investigation trenches. Resulting parameters are presented in Table 8-1.

Tuominen et al. (2006) showed that the match between simulated and observed properties of fracture sets is rather reasonable for surface and ONKALO data, but the intensity of fracturing in drillhole data is underestimated. According to Tuominen et al. this fact should be studied in the future.

Table 8-1. Summary of simulation parameters in (Tuominen et al. 2006).

P32 r min kr

Dipdir = 139

Set 1 Dip = 18 0,87 0,52 3,33Disp. 7,9

Dipdir = 89

Set 2 Dip = 89 0,47 0,22 3,11Disp. 16,7

Dipdir = 177

Set 3 Dip = 86 0,45 0,47 3,5Disp. 16,6

DFN parameters in Tuominen et al. (2006) were defined only based on the orientation and frequency data. An example of the simulated fracture map is presented in Figure 8-8. (Tuominen et al. 2006). In further studies, also other parameters e.g. fracture termination, fracture fillings and kinematical data, should be applied. An example of the simulated fracture map is presented in Figure 8-8. (Tuominen et al. 2006).

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Figure 8-8. Trace map of a 20 m x 20 m area of OL-TK11 (a) and trace map of 20 m x

20 m sampling trace plane from the simulation (b). (Tuominen et al. 2006).

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9 EVALUATION OF UNCERTAINTIES

Uncertainties of the lithological and ductile deformation models

One of the main uncertainties in the lithological 2D model is the incomplete coverage of available data. The bedrock is rather poorly exposed, which causes difficulties in determination of the location of lithological boundaries. In the central investigation area with only a few outcrops, the outcrop mapping has been supplemented by the results from deep and shallow drillholes and ten investigation trenches and interpretations of the geophysical investigations. However, the contacts between the rock types are visible only occasionally, and, thus, the bedrock map is largely an interpretation, which combines the direct observations of the rock types and their contacts in outcrops, investigation trenches and in drillholes with the interpretation of the geophysical investigations and the tectonic structure of the area.

During the site investigations, a number of different geologists have carried out the outcrop and trench mappings at Olkiluoto. Since the outcrop data is largely descriptive in character and based on interpretations of individual geologists, it is rather heterogeneous. Moreover, the naming practice of the rock types during the early mappings in 1988 and 1991 was different from that adopted later in the drill core studies. Although the nomenclature has recently been co-ordinated (see Kärki & Paulamäki 2006), uncertainties may still exist, especially regarding the naming of different migmatite types. The gneisses and migmatites of Olkiluoto form a transition series and it is not possible to define any clear contacts between the rock types as the change from one type to another takes place gradually. An artificial border between the gneisses and migmatites has been set at 10% or 20% of granitic leucosome. Within the migmatites the proportion of the leucosome varies from about 10% to more than 80%.

Although lithological data from 33 drillholes have been available in preparing the 3D lithological model, they are, however, rather limited and the distance between the drillholes is great. Consequently, there are considerable uncertainties concerning the geometry and extension of the various rock units at depth. Uncertainties remain, especially, concerning the size and extension of the pegmatitic granites. In the lithological model, the granite pegmatite sections in drillholes more than 10 metres in length have been distinguished as separate units. In addition, the pegmatite sections less than 10 m in length, if separated only by short sections of migmatitic mica gneiss, are combined into larger units. It is quite certain that the granite pegmatites are not as continuous and coherent as modelled and do not necessarily characterise the actual form of the veins, but rather volumes of rock mass where granite pegmatite veins are more common than outside these units.

The complexity of the ductile deformation is an important source of uncertainty in the bedrock modelling. The bedrock has been interpreted to be subject to five successive ductile deformational phases. The actual measuring of the various ductile deformation structures (foliation, folds, lineations etc.) can be rather exact, although errors certainly occur, for instance, in the measurement of dip values. The complexity of the

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deformation leads to difficulties in determining the occurrence of the different lithologies occurring at the surface or at depth.

The effects of foldings, especially during D3, have not been visualised in the 3D lithological model, except in the case of veined gneiss/diatexite contact (see Chapter 4.6) but an assumption was made that between drillholes the foliation is rather constant over large distances and lithological correlations from drillhole to drillhole and from the drillhole to surface can be made in accordance with foliation measurements. Thus, the current model must be seen as a simplified representation of probable complex geological structures. Although we have rather a good understanding of the larger-scale folding in the site area, presenting it in 3D is difficult because of the lack of proper larger-scale marker horizons. The migmatites, which in the present lithological model form the main volume of the rock mass, have been divided into different migmatite types. Their use in the modelling is uncertain, however, , because the classification is based solely on visual inspection of rock types in outcrops and drill cores by a number of individuals independently. More detailed petrological and lithogeochemical studies of the drill core samples have shown that the metasedimentary and metavolcanic rocks of Olkiluoto can be subdivided into four different series (Chapter 4.2). This new classification of the migmatitic mica gneisses may provide the way to incorporate the folding into the lithological model. However, the data of the distribution of these series are, presently, far too scanty to be used in the modelling.

Uncertainties of the brittle deformation model

In general, one importante source of uncertainty in geological modelling is the low number of drillholes, their uneven distribution and the distances between the drillholes. In Olkiluoto, the ONKALO area is well covered with drillholes and therefore also the confidence of the model is higher in the area; nevertheless, in the modelled area, there are still few "white areas", where the drillhole density is very low and, similarly, also the confidence of the model. In addition, in places where there are no drillholes, deterministic modelling is impossible due to lack of proper data and, as a consequense, these areas are likely to be underrepresented by geological features in the model. Another cause of uncertainty is the quite uniform drilling orientation that causes bias, as it masks the occurrence of possible N-S trending features. Modelling of the brittle phase of deformation has two types of uncertainty. The first one is measurement-related problem, i.e. how to identify and measure brittle elements and their kinematic features (e.g., fractures, slickensides, fault slip direction, sense of slip direction) correctly and the second one is data analysis-related or conceptual uncertainty.

Modelling tasks need a large amount of oriented data from drill core samples. The insufficient amount of oriented core and in places core losses together with the increasing need of accurate orientation data on kinematic elements and fractures at depth promoted the substantial use of drillhole TV. The analysis of the TV imagery carries basically the same uncertainties as the drill core sample by using the same deviation data. The other uncertainties are disturbances or inadequate quality of TV imagery and sometimes the difficulty to identify properly the planar features of the imagery. In the imagery analysis the core sample is also checked if available to

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compensate, for example, for the low quality of the TV imagery and to minimise the errors in interpretations of planar elements.

Data analysis-related and conceptual uncertainties regarding the brittle deformation modelling are, e.g.:

Orientation of the fault zones Length and down-dip extent of the zones Strong spatial variation in properties (width, fracturing, hydraulic conductivity) within the same modelled brittle fault zone Large number of modelled zones intersected by only one drillhole and presented as rectangular bodies, extending about 50-300 m from the drillholes Surface exposure of the fault zones Termination of the fault zones (in the present model, almost all the modelled zones are presented as individual zones) Lack of possible N-S and NW-SE-striking fault zones, which may exist between the parallel drillholes

There are large uncertainties in the orientation of the modelled zones, since the orientation of most of the zones is based on a few striated fault surfaces assumed to reflect the orientation of the zone. In some zones the orientation is determined by just one or two faults. Regarding the certainty of the orientation, 8 zones have a high confidence, 25 a medium confidence and 70 a low or very low confidence. As the orientation of the modelled fault zones is mostly based solely on the kinematic data, errors in the data may have a big impact on the orientation of the zone. Moreover, even if the data are correct, there can be several different fault orientations in one intersection making also other interpretations of the orientation of the whole fault zone possible.

Both the horizontal and down-dip continuities of the modelled fault zones are uncertain. Although 33 drillholes have been drilled at the site area, it is, however, a rather small number considering the dimensions of the area, and the distances between the drillholes are quite large. This causes uncertainties in connecting the individual brittle fault and joint intersections in one drillhole to another over large distances. This has led to a large number of zones extending only about 50-300 from the drillhole. It is possible to estimate the length of the fault from the maximum displacement of the fault (see, e.g., Kim & Sanderson 2005) but it cannot be used at Olkiluoto, because at the moment only the fault and fault vector orientations and the sense-of-shear are known. However, it should be bare in mind that the rather small lengths are not necessarily incorrect but the fault zones may really be that short as noticed in areas with many drillholes occurring close to each other.

Because of the general flatness of the outcrops, there are uncertainties in measuring the dip of fractures accurately. At the very least, the horizontal or subhorizontal fractures are underrepresented in the surface fracture data. There are considerable uncertainties in the distribution of the fracture trace lengths, since generally only about one-third of the measured fractures in the outcrops and investigation trenches can be seen in their full length.

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Uncertainties exist regarding the relationship between the surface fracture data and the drill core data. There are, for example, differences in the distribution of fracture sets. For example, ca. N-S striking fracture set, which is one of the two main fracture sets in the outcrops, is commonly only poorly represented in the drill core fracture data, probably due to unfavourable orientation of the drillholes. In the previous phase of the site investigations, the outcrop data and the drillhole data were combined and a correction method was used to reduce the bias by compensating for the under-represented fractures (see Paulamäki & Paananen 1996).

Although most of the modelled fault zones strike E-W or NE-SW, i.e., follow the general trend of the ductile deformation, the existence of N-S and NW-SE striking zones cannot be overruled. The N-S striking fractures form a very distinct fracture cluster in the outcrop data and all the brittle faults observed on outcrops strike either N-S or NW-SE. Moreover, NW-SE trending lineaments are very common in the Olkiluoto area.

The hydrothermal alteration model is the first serious outcome of the site area. The alteration study benefited data collected in the pilot study from deep drill holes OL-KR1 to OL-KR33. The visual assessment of the alteration was supported by the preparation of a small number of thin sections. At the moment, the mapping method is one of the main limitations and uncertainties of the alteration study, because it is mineralogically too simple. For example, all greenish, soft clay-type material is classified as illite, although it is known to occur together with a variety of other minerals, such as those of the smectite group, chlorite, montmorillonite, etc. In thin sections, it was impossible to separate the above minerals from each other or illite from fine-grained muscovite or sericite; however, the mode of occurrence of illite or illite-looking material shows clear replacement of older silicate minerals, often plagioclase. Considerable instrumental analysis work would be required to distinguish and identify different mica and clay species, but technically any of these minerals may have same impact, as they are present as a soft, soap-like mass, which may form 5 - 10% by volume of the rock at Olkiluoto, locally even more. Kaolinite forms very fine-grained, pure white, soft and powdery masses and coverings. In some places it could be mixed up with fine-grained calcite, which, however, can be identified by using dilute hydrochloric acid. The configuration and the number of the drillholes limit especially the evaluation of the size of the illitic body and its continuation to the NE and E.

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10 SUMMARY

The geological model of the Olkiluoto site area is composed of four submodels: the lithological model, the ductile deformation model, the brittle deformation model and the alteration model. The lithological model gives the properties of definite rock units that can be defined on the basis the migmatite structures, textures and modal compositions. The ductile deformation model describes and models the products of polyphase ductile deformation, which makes it possible to define the dimensions and geometrical properties of individual lithological units determined in the lithological model. The ductile deformation structures are important precursors for the subsequent brittle deformation. The brittle deformation model describes the products of multiple phases of brittle deformation.

The rocks of Olkiluoto can be divided into two major classes: 1) high-grade metamorphic rocks including various migmatitic gneisses, tonalitic-granodioritic-granitic gneisses, mica gneisses, quartz gneisses, and mafic gneisses, 2) igneous rocks including pegmatitic granites and diabase dykes. The migmatitic gneisses can further be divided into three subgroups in terms of the type of migmatite structure: veined gneisses, stromatic gneisses and diatexitic gneisses, the last mentioned representing distinct end members in a transition system of gneisses and migmatitic gneisses. The change from rather homogeneous gneisses to migmatitic gneiss variants and between the migmatitic gneisses takes place gradually, so that it is not possible to define any natural borders between the end members. Thus, an artificial border between the homogeneous gneisses and migmatitic gneisses has been set at 10% or 20% of the leucosome. The veined gneisses account for 43% of the volume of the Olkiluoto site area, the stromatic gneisses for 0.4% and the diatexitic gneisses for 21%. The granite pegmatites make up 20% of the bedrock, the tonalitic-granodioritic-granitic gneisses 8%, mica gneisses 7% and the mafic gneisses 1%.

Based on whole rock chemical analyses, the supracrustal rocks can be divided into four distinct series: the T series, S series, P series and mafic or ultramafic, probably volcanogenic gneisses. In addition, pegmatitic granites and diabases form groups of their own. Rocks of the T, S and P series are estimated to make up 42-46%, 7-12% and 26-28%, respectively, of the volume of central part of the island of Olkiluoto and the various pegmatitic granites about 20%. The T series include mica gneisses and migmatitic gneisses with less than 60% SiO2 and quartz gneisses with more than 75%

SiO2, representing clay mineral-rich pelitic materials and greywacke-type impure sandstones, respectively. The members of the S series, characterised by their high calcium concentration, have originated from calcareous sedimentary materials. The P series, which is mainly composed tonalitic-granodioritic-granitic gneisses, is characterized by its high P2O5 concentrations that exceed 0.3%. The comparison of the chemical compositions of the different series indicate that the origin of the protolith for the P-type gneisses most likely include mixing of the volcanic and turbiditic components and subsequent physical and chemical enrichment processes.

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On the basis of refolding and crosscutting relationships, the supracrustal rocks have been subject to polyphased ductile deformation, made up of five stages. The main deformation phase D2 is characterised by intense thrust related folding and abundant leucosome production. Shear related structures have been observed as the most important D2 elements in certain zones. In deformation phase D3 the earlier structures were zonally refolded or rotated. Zones dominated by ductile D3 shears and folds were formed, and often, e.g., the S2 foliation was reoriented parallel to the F3 axial plane (S3).Simultaneously with D3 deformation a new granitic leucosome intruded parallel to the F3 axial planes. Subsequently the D3 and earlier elements were again re-deformed in the deformation phase D4, which produced more open F4 folds with axial planes trending ca. NNE -SSW. Due to D4 deformation, the S2/3 composite structures are zonally reoriented towards the trend of F4 axial plane. The latest ductile structures to be identified are the very open F5 folds, the fold axes plunging gently to the ESE and axial planes to the SSW.

In 3D modeling of the lithological units, an assumption has been made, on the basis of measurements in outcrops, investigation trenches and drill cores, that the pervasive, composite foliation produced as a result a polyphase ductile deformation has a rather constant attitude in the site area. Consequently, the strike and dip of the foliation has been used as a guide, through which the lithologies have been correlated between the drillholes and from the surface to the drillholes. The lithological modelling mainly comprises modelling of the tonalitic-granodioritic-granitic gneisses and the pegmatitic granites. In addition the contact zone of the diatexitic gneisses and veined gneisses has been modelled as well as the narrow diabase dykes. The veined gneisses form the main volume of the model area. The tonalitic-granodioritic-granitic gneiss and pegmatitic granite intersections in drillholes more than ca. 10 metres in thickness have been distinguished as separate units. Furthermore, adjacent pegmatitic granite sections less than 10 m in length, separated by short sections of homogeneous or migmatitic gneisses were combined into larger units with the assumption that the gneisses represent inclusions within the pegmatitic granite. The lithological model includes 17 units of tonalitic-granodioritic-granitic gneisses, 35 units of pegmatitic granite, 6 diabase units and one unit of diatexitic gneiss.

The bedrock in the Olkiluoto site has been subject to extensive hydrothermal alteration, linked to the phases of magmatic activity. The alteration has taken place at reasonably low temperature conditions, the estimated temperature interval being from slightly over 300oC to less than 100oC. Typically, high permeability zones were created and these zones appear to have repeatedly acted as pathways for the periodic thermal fluid circulation. Two types of mode of occurrence can be observed in hydrothermal alteration processes: 1) pervasive (dissemination) alteration and 2) fracture-controlled (veinlet) alteration. Kaolinisation and sulphidisation are the most prominent alteration events at the site model area. Sulphides are located in the uppermost part of the model volume following roughly the lithological trend (slightly dipping to the SE). Kaolinite is located also in the uppermost part, but the orientation is opposite to the main lithological trend (slightly dipping to the N). The third main alteration event, illitisation, appears to form a dome-like body located north of the ONKALO access tunnel and penetrating the eastern repository panel. Calcite occurs as fracture infillings and as stockwork vein sets in the same bedrock volume as the other three hydrothermal

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alteration zones and at least part of that is understood to present carbonatisation, which, however, has not affected the rock itself. The continuance of the alteration-affected bedrock downwards from the drillhole sounded bedrock volume is probable. The lower surfaces for the modelled alteration volumes given in this paper are to be taken as the cut-out, which is based on the present drillhole information, and other available geo-analytical records received so far.

The bedrock at the ultimately hydrothermally altered volumes has suffered strong chemical and physical modification and the most essential compounds, which may have mobilised in these processes, are the oxides of alkaline earths and alkalines and likewise SiO2, Al2O3, FeO, P2O5, U2O, ThO2, CO2, S, Cl, F. The contents of these compounds in unaltered and altered bedrock volumes and their mutual proportions are potential markers of the grade of alteration. The increased concentrations of CO2 and the compounds of sulphur are anticipated to have an influence on the acidity of ground and matrix water conditions and subsequently to the solution- dissolution behaviour of some of the critical elements at the zones.

About 1700 fault planes and fault-slip striation orientations, and sense-of-shear of the faults were measured from drillholes KR1-KR33. On the basis of the statistical analysis of the orientation of the slip striations , faults have tentatively been divided into five main fault groups: A, B, C, D and E . It is assumed that the faults with the same slip striation orientation are cogenetic. Slip striation directions are subhorizontal, N-S trending for group A, gently NE or SW plunging for group B, gently SSE plunging for group C, gently ENE plunging for group D and gently SE plunging for group E. In addition to fault data, sections of increased fracturing in the drill cores and ONKALO tunnel were mapped and subdivided into brittle joint intersections (BJI) and brittle fault intersections (BFI). The BFI intersections were modelled as brittle fault zones, the orientation of which was determined on the basis of the above kinematic data. On the basis of drillhole data, 98 fault zones from the site area were interpreted and modelled in 3D. In addition, the model includes three fault or fracture zones observed both at the surface and in the ONKALO access tunnel, as well as two possible zones, interpreted on the basis of charge potential survey in drillholes.

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11 FUTURE ACTIVITIES

As was stated in the preceding chapters, the modelling results contain uncertainties related to the accuracy of size, location and characteristic parameters of the modelled units. The modelling of geological features is basically an iterative, dynamic process, where continuous processing of the data yields new ideas and concepts, which may be implemented into the updated versions of the geological model. Therefore this version of the model is a baseline (i.e. version 0) for the future modelling and for the characterisation of the geology and will be refined and updated as new data is acquired. Consequently, the so-called prediction-outcome studies of the tunnel are an important tool for evaluating modelling methodologies and the uncertainties of the models.

Several aspects of the current site model need to be improved and refined for the next versions:

Ductile deformation needs to be extended in to three-dimensional model in order to provide information on the degree of intensity, type and orientation of foliation in the deeper parts of the ONKALO facility. As was stated in the preceding chapters, foliation has significant implications to the rock mechanical properties of the bedrock. In future more attention need to be paid for defining foliation characteristics for forthcoming tunnel sections. There is also necessity for evaluation of foliation significance for constructing tunnel in certain direction through the foliation plane. Also, a more definitive analysis of the foliation data and data on other ductile deformation features needs to be carried out, following the established methodology of structural analysis.

The effects of different lithologies in respect to the type and quality of fracturing and foliation need to be evaluated in more detailed manner in future modelling work. Also, the importance of the tunnel orientation to the above-mentioned properties will be more closely assessed. In the geological models of the ONKALO area, special attention will be paid to the units, which are located close to, or within, the ONKALO facilities.

The rock mechanical characteristics of the hydrothermally altered and weathered zones needs to be investigated in more detailed, since these are likely to have important implications for ONKALO construction. Possible correspondences between the effects of alteration in different lithologies, and the products of ductile deformation and brittle deformation need to be evaluated in the course of future modellings.

The specific internal characteristics of modelled brittle fault zones need to be presented, although it must be recognized that the characteristics of faults are typically highly variable and discontinuous and therefore the descriptions of particular intersections are not necessarily applicable to the fault as a whole. A highly crushed intersection of a fault at one intersection may transform into a single shear fracture at another intersection (adding to the heterogeneity of the rock mass and limitations of the modelling work).

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The deepened understanding of the relationships between the different modelled kinematic groups of faults needs to be attained (for example, by proper kinematic analysis and age determinations), for instance, the age relationships. Only by understanding the deformation history and mode of formation of the brittle faults can a reliable model be presented, because this knowledge provides constraints on the location, geometry and extent of the faults. The basic problem with this concept is data coverage – drill core data provides only punctual information, whereas the ONKALO tunnel will increase our knowledge enormously as the brittle zones are successively intersected.

The zone of influence which accompanies any fault, often referred to as the ‘damage zone’ or ‘transition zone’, i.e. the zone of increased fracturing, alteration and water conductivity around the fault core, is an important feature of the fault zones in relation to construction and long-term safety. Work is currently going on, firstly to define the term ‘influence zone’ and secondly to characterize it by means of geological and geophysical methods. The results of this work will greatly enhance our knowledge of the properties of the brittle deformation zones and therefore increase the quality and accuracy of the model.

The resolution of the stochastic approach for characterising fracturing will be increased in bedrock volumes where the methods of deterministic modelling are not applicable. Single fractures are generally too small to be described deterministically and therefore extensive statistical analysis of fracture data will be implemented in the future models.

The SITE model will be updated every 2-3 years, as new data is acquired from drillings, trenches and the ONKALO access tunnel. The update frequency will be coordinated through the Olkiluoto Modelling Task Force (OMTF). Prior to the update, a decision on the data freeze needs to be done in order to keep a balance between the decided deadlines and the acquisition of new data.

In the next modelling period, an important process is the continuous assessment of hydrological, hydrogeochemical and rock mechanical data from the perspective of geological data - the results will be then used as an important tool in the development of the geological model and building of separate integrated models (hydrogeological model, rock mechanics model and hydrogeochemical model).

All the above-mentioned issues will be addressed in the course of future modelling activities, with the acquisition of new data and the development of concepts based on the geological history and the style and type of deformation. As was stated in Chapter 1, the results and conclusions of the modelling reports necessarily reflect the current understanding of the site-specific geological features and, as a consequence, the amount of information provided in these reports will increase and will be more specifically focussed on the needs of the end-users of the model, i.e. layout-design and long-term safety.

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APPENDICES

Appendix 1: Hierarchical classification procedure for deformation zone intersections at Olkiluoto

Appendix 2: Deformation zone intersections in drillhole OL-KR25 (Table 1)

Appendix 2: Measured kinematic data from drillhole OL-KR25 (Table 2)

Appendix 2: WellCAD-table of drillhole OL-KR25 (Table 3)

Appendix 3: Description of the modelled deformation zones

Appendix 4: Vertical and horizontal cross-sections of the modelled deformation zones and lithologies

174

175 APPENDIX 1

Table 1. Hierarchical classification procedure for deformation zone intersections at Olkiluoto (Milnes et al., in prep.)

Designation of a given intersection at Olkiluoto:

The intersection shows intensive deformation, clearly more intensive than the wall rock on either side.

Designation: Deformation zone intersection

The intersection is characterized by features which indicate that the deformation took place under low PT conditions, lower than those under which the wall rock was

formed.

Designation: Low-grade deformation zone intersection

The intersection shows cohesionless or low-cohesive

deformation products: gouge, breccia, fractured rock and their

partially mineralized equivalents

Designation: Brittle

deformation zone intersection

(often called “fracture zone” intersection in earlier reports)

The intersection shows no clearsigns of lateral

movement

Designation: Joint zone

intersection

(BJI )

The intersection shows clear signs

of lateral movement

Designation: Fault zone

intersection

(BFI)

The intersection shows cohesive

deformation products:

cataclasites,peseudotachylite,

welded crush rocks, etc.

(typically massive and structureless)

Designation: Semi-brittle

deformation zone,

or semi-brittle

fault zone,

intersection

(SFI)

The intersection shows cohesive

deformation products: mylonites,

phyllonites, etc. (typically strongly

foliated)

Designation: Low-grade

ductile

deformation zone,

or ductile shear

zone, intersection

(DSI)

The intersection is characterized by features which

indicate that the deformation took place under high

PT conditions,similar to those under which the wall rock was

formed, showing cohesive

deformation products (e.g.

blastomylonites)

Designation: High-grade

ductile

deformation zone

intersection

(HGI)

APPENDIX 2 176

In table 1, descriptions of the mapped deformation zone intersections from drillhole OL-KR25 are presented as an example of the type of data produced during the structural geological mapping campaign mentioned in the preceding text. The descriptions are presented together with information of the intersection identification code, along-the-hole length of the intersection, type of intersection (classified according to the system presented in appendix 1), geologist who performed the mapping and mapping date.

In table 2, the kinematic data mapped from drillhole OL-KR25 is shown as another example of the type of data produced during the structural geological mapping campaign. The column DRILLHOLE refers to the mapped drillhole, DEPTH to along-the-hole depth of a mapped fracture, SAMPLE to fracture orientations measured from oriented drillcore, IMAGE to fracture orientations measured from WellCAD-image, DISPLACEMENT VECTOR to the orientation of measured slip-linear, U to the sense-of-movement of the slip-linear in respect to horizontal plane, E in respect to NS-striking vertical plane and S in respect to EW-striking vertical plane. CERTAINTY refers to the estimated confindence of the sense-of-movement where 1=certain, 2=uncertain and 3=very uncertain. In the DESCRIPTION column the quality of the fracture surface is described with abbreviations which refer to striated surfaces (STRIA), planar surfaces (PLAN), undulating surfaces (UNDU), irregular surfaces (IRREG), concave or convex surfaces (CONC), grooved surfaces (GROV). In addition, stepped surfaces are described with the abbreviation STEP and observed pressure shadow growth of minerals is described with PSGR. SOURCE-column indicates which of the fracture orientation measurements, either SAMPLE or IMAGE, is used in the measurement of the orientation of the slip-linear (DISPLACEMENT VECTOR).

APPENDIX 2 177

Table 1. Deformation zone intersections in drillhole OL-KR25

INTERSECTION DRILLHOLE FROM TO TYPE DESCRIPTION GEOLOGIST DATE

OL_KR25_BJI_8095_8655 OL-KR25 80.95 86.55 BJI

The intersection contains mostly veined gneiss and some diatexitic gneiss parts. The rock is heterogeneous and lacks any clear foliation in the beginning (81-85 m). The fractures are not paralell to the foliation. The intersection contains 32 fracture with an average fracture frequency of 5-8 fractures / m. Three of the fractures have signs of water conductivity (82.20, 85.39 & 86.30) and contain green and greyish clay mineral infillings. Two fracture sets occur; one horizontal and one nearly vertical with a W-E trend. A few old and welded fractures with pyrite and calcite are present. Some mechanical fracturing has occured during the drillings.

Jon Engström, GSF

7.6.2005

OL_KR25_BJI_9445_9730 OL-KR25 94.45 97.30 BJI

The intersection is composed of veined gneiss. The intersection contains old and welded fractures where pyrite and some calcite are present. These old fractures has partly been reopened during drilling. The rock has a clear foliation and the fracturing follows it. All the fractures have a NE-SW direction and a moderate dip. The intersection contains 21 fractures, with an average fracture frequency of 7 fractures / m. The rock is weathered, crushed and altered in section 96.35-96.66. The section also exhibits clear signs of water conductivity. Some mechanical fracturing has occured during the drillings.

Jon Engström, GSF

7.6.2005

OL_KR25_BJI_14970_15415 OL-KR25 149.70 154.15 BJI

The rock in the intersection is mostly composed of veined gneiss, with diatexitic gneiss in the beginning and quartz gneiss in the end. The fractures are randomly orientated and partly follow the foliation. Mostly they have a moderate dip and E-W direction. The intersection contains 41 fractures, with an average of 6-8 fractures / m. The rock is more fractured at interval 151.80-153.00 m, with 20 fractures. This section ends in the contact between the veined gneiss and quartz gneiss. A few old and welded fractures with calcite are present, some of them has been probably reopened later. The intersection contains no water conductivity signs. Some mechanical fracturing has occured during the drilling.

Jon Engström, GSF

7.6.2005

OL_KR25_BFI_16459_17200 OL-KR25 164.59 172.00 BFI

The rock in the intersection is mostly composed of diatextitci gneiss, with some small sections of veined gneiss and quartz gneiss in the beginning. The texture of the rock is irregular and no clear foliation can be observed. The fractures are randomly orientated with a nearly horizontal dip. The intersection contains 47 fractures, with an average fracture frequency of 4-7 fractures/m. It also contains 10 fractures with slickensided surfaces. The lineation on the slickenside surface has a trend varying from NW to NE, with variable plunge. The slickenside surface mostly show a R,L,L movement. A few old and welded fractures with calcite are present. Three of the fractures have signs of water conductivity (171.23, 171.30 & 171.41). Some mechanical fracturing has occured during the drilling.

Jon Engström, GSF

7.6.2005

APPENDIX 2 178

OL_KR25_BFI_21650_22205 OL-KR25 216.50 222.05 BFI

The rock in this intersection is heterogeneous and is composed of small veined gneiss, diatexitic gneiss, pegmatitic granite and mafic gneiss sections. On a large scale the rock is diatexitic gneiss. Only in the sections with veined gneiss has the rock a clear foliation and fractures parallel to it. The intersection has a total of 52 fractures at a frequency of 9 fractures / m. 11 of the fractures have slickensided surfaces. The lineations on the slickensides occur in two directions; plunging towards east and nearly horizontal with N-S trend. At 217.70-218 m the rock is crushed at shows signs of water conductivity (greyish clay infillings), at this section the rock has probably been partly mechanically chrushed.

Jon Engström, GSF

7.6.2005

OL_KR25_BFI_34700_35225 OL-KR25 347.00 352.25 BFI

The intersection contains mostly veined gneiss and a diatexitic gneiss part. The rock is mostly clearly foliated but the diatexitic gneiss part in section 348.92-349.75 is heterogenous and irregular. The intersection contains 50 fractures, with an average frequency of 7-11 fractures/m. The fractures in the intersection have a nearly horizontal dip but their orientation varies. The rock is more fractured in the section between 350.50-351.70, which contains 22 fractures. The rock in this section shows minor signs of semi-brittle shearing, with some cataclastic features and alteration of the feldspars. It also contains some calcite filled healead fractures. This fractured section also exhibits some water conducting fractures in the beginning of it, with grey clay infillings. The intersection also contains several slickenside surfaces, but no directions or movements could be observed. The horizontal nature of the fracturing in this section can partly probably be explained by the effect of drilling.

Jon Engström, GSF

7.6.2005

OL_KR25_BJI_36931_37320 OL-KR25 369.31 373.20 BJI

The intersection is composed of diatexitic gneiss and veined gneiss. The diatexitic gneiss section (369.70-371.75) in the rock is strongly altered, containing feldspars which are altered to albite (yellow-greenish coloured). This section also contains thick (max 5 cm) calcite bearing water conductive fractures (20 fractures). The neosomes in the veined gneiss exhibit a green soft unidentified mineral. The veined gneiss contains only a few fractures. The fractures are randomly orientated, usually with a nearly horizontal dip. At 370.75 m there is 10 cm of core loss and the wellcad picture shows in this part a large fracture/cavity (this part contains small calcite crystals). This fracture/cavity also shows a clear peak in the flow rate table. Some mechanical fracturing has occured during the drillings.

Jon Engström, GSF

7.6.2005

OL_KR25_BJI_48960_49540 OL-KR25 489.60 495.40 BJI

The dominating rock type in the intersection is veined gneiss with short sections of diatexitic gneiss and pegmatitic granite. The intersection contains old and welded fractures where calcite are present. Some of these fractures have been reactivated later. Most of the fractures in the intersection have calcite or/and kaolinite fillings and some of them show signs of water conductivity. The fractures exhibit an E-W trend, with horizontal to moderate dip towards south. The intersection contains ca 50 jfracture, with a frequency of of 3-13 fractures/m. The most fractured part (490.40-490.90, 491.20-492.00 & 493.50-494.00) of the rock also shows signs of water conductivity. Some mechanical fracturing has occured during the drillings.

Jon Engström, GSF

7.6.2005

APPENDIX 2 179

OL_KR25_BJI_56510_56882 OL-KR25 565.10 568.82 BJI

Veined gneiss which exhibits few neosomes. The rock contain old and healed fractures with calcite fillings. Some "younger" fractures are probably old fractures that have been reopened either naturally or mechanicaly during the drilling. The fractures are partly parallel to the foliation but other directions also occur. No directions have been measured because of absent Wellcad picture. At 566.07 and 566.10 there are two water conducting fractures with some grey clay infilling.The most fractured section at 568.50-568.70 m, also shows some water conducting fractures. This most fractured section contains 7 fractures/20 cm, average being 5-8 fractures/m. The drilling had small impact on the core sample.

Jon Engström, GSF

7.6.2005

OL_KR25_BFI_57155_57800 OL-KR25 571.55 578.00 BFI

The intersection is composed of veined gneiss and pegmatitc granite. Pegmatitic granite sections have old, welded calcite bearing fractures. Fractures exhibit dip direction towards NW with a nearly horizontal dip. The intersection contains 8 slickenside surfaces, but the orientation of the striation varies. Some of the fractures are water conducting. These fractures contain kaolinite and grayish clay infillings. The intersection contains ca 40 fractures, with 13 fractures/0.7 m (576.21-576.91). Some mechanical fracturing has occured during the drillings.

Jon Engström, GSF

7.6.2005

APPENDIX 2 180

Table 2. Measured kinematic data from drillhole OL-KR25

DRILLHOLE DEPTH SAMPLE IMAGE DISPLACEMENT VECTOR SENSE-OF-MOVEMENT CERTAINTY DESCRIPTION SOURCE

(m) Dip dir. dip Dip dir. dip Plunge Trend U E S

OL-KR25 69.20 no data no data 250 74 27 322 L L R 3 STRIA,PSGR IMAGE

OL-KR25 72.33 no data no data 94 23 47 113 R R L 3 PSGR,UNDU,IRREG,STRIA IMAGE

OL-KR25 74.03 no data no data 117 39 9 182 L R N 2 STRIA IMAGE

OL-KR25 74.34 no data no data 99 44 32 41 R R L 3 STRIA,PSGR IMAGE

OL-KR25 74.37 no data no data 96 39 25 41 N L L 2 STRIA,PSGR IMAGE

OL-KR25 78.75 no data no data 178 32 38 192 L L R 2 STRIA,PSGR IMAGE

OL-KR25 86.13 no data no data 152 44 47 137 L L R 2 STRIA,CONC IMAGE

OL-KR25 108.37 no data no data 279 77 24 349 R N L 3 STRIA,GROV,PSGR IMAGE

OL-KR25 114.80 no data no data 200 41 42 244 R L R 2 PSGR IMAGE

OL-KR25 118.75 no data no data 158 25 26 114 R R L 2 PSGR,STRIA IMAGE

OL-KR25 122.77 156 59 185 61 55 161 L L N 2 GROV,PSGR IMAGE

OL-KR25 129.30 no data no data 146 56 17 216 R L R 2 PSGR,STRIA,IRREG IMAGE

OL-KR25 133.64 136 55 142 53 45 94 R R L 2 PSGR,STRIA,PLAN IMAGE

OL-KR25 145.05 186 39 189 40 0 93 R N L 2 PSGR,STRIA,PLAN IMAGE

OL-KR25 158.62 113 20 155 29 42 120 L L R 2 PSGR,PLAN IMAGE

OL-KR25 161.24 no data no data 131 46 57 119 R R L 1 GROV,STEP,UNDU IMAGE

OL-KR25 164.11 no data no data 93 55 56 48 R L L 3 PLAN,GROV,STRIA IMAGE

OL-KR25 165.86 61 41 114 1 37 10 R L L 3 PLAN,STRIA,STEP,GROV SAMPLE

OL-KR25 165.99 no data no data 111 13 18 8 R L L 3 UNDU,STRIA,GROV SAMPLE

OL-KR25 167.73 231 79 237 73 19 305 R R R 2 STRIA,UNDU IMAGE

OL-KR25 168.92 no data no data 220 48 40 277 R L L 3 STRIA,UNDU,GROV IMAGE

OL-KR25 169.22 no data no data 228 23 19 296 R L L 3 STRIA,CONC,STEP IMAGE

OL-KR25 169.50 95 31 126 20 13 37 L R R 2 IRREG,STRIA SAMPLE

OL-KR25 169.61 no data no data 139 33 15 54 L R L 3 CONC,STRIA IMAGE

OL-KR25 186.55 196 64 152 37 44 104 R R L 2 PLAN,STRIA,GROV IMAGE

OL-KR25 193.49 51 21 103 16 20 74 L L L 3 PLAN,STRIA SAMPLE

OL-KR25 193.52 65 16 81 14 13 95 N N L 3 UNDU,STRIA IMAGE

OL-KR25 196.42 75 26 103 27 31 78 R N L 3 PLAN,STRIA,GROV IMAGE

OL-KR25 206.64 no data no data 117 62 30 32 L R R 3 UNDU,STRIA,GROV IMAGE

OL-KR25 206.97 no data no data 113 35 29 95 N L R 2 CONC,GROV,STRIA IMAGE

OL-KR25 208.49 no data no data 150 28 31 125 L L R 1 PLAN,GROV,STRIA IMAGE

OL-KR25 209.83 no data no data 28 33 31 331 L R L 3 UNDU,GROV,STRIA,STEP IMAGE

OL-KR25 216.79 56 51 103 51 3 6 R L R 2 PLAN,STRIA IMAGE

OL-KR25 218.07 no data no data 98 59 28 95 N L L 3 PLAN,STRIA IMAGE

OL-KR25 218.21 no data no data 127 33 33 74 L R R 3 CONC,STRIA IMAGE

OL-KR25 218.70 no data no data 155 44 45 136 L L R 3 PLAN,STEP,PSGR,STRIA IMAGE

OL-KR25 220.96 no data no data 86 31 5 190 L L R 3 STRIA,PSGR IMAGE

OL-KR25 224.54 no data no data 88 49 19 17 R R L 1 IRREG IMAGE

OL-KR25 228.74 no data no data 168 40 45 325 R R L 2 PSGR,IRREG,STEP IMAGE

OL-KR25 228.85 no data no data 137 33 42 118 L L R 2 CONC,UNDU,PSGR IMAGE

OL-KR25 228.88 120 35 118 41 34 79 R N L 2 PSGR,STEP IMAGE

OL-KR25 237.33 186 59 165 67 5 79 L R L 2 STRIA,PSGR IMAGE

OL-KR25 241.02 no data no data 183 49 13 259 L R L 2 STRIA,PSGR IMAGE

OL-KR25 274.51 no data no data 277 19 0 16 N R R 2 STRIA,PSGR IMAGE

OL-KR25 281.66 328 60 332 48 47 9 L L L 3 STRIA,PSGR,PLAN IMAGE

APPENDIX 2 181

OL-KR25 288.97 136 30 150 25 27 192 L R R 3 STRIA,STEP IMAGE

OL-KR25 351.48 no data no data 263 14 7 192 L L L 3 STRIA,PSGR IMAGE

OL-KR25 365.93 289 19 260 20 2 11 R R L 2 PLAN,STRIA SAMPLE

OL-KR25 372.95 no data no data 120 23 20 110 R R R 2 IRREG,STRIA IMAGE

OL-KR25 376.82 127 20 142 31 25 121 N R L 3 PLAN,STRIA,GROV IMAGE

OL-KR25 402.40 174 63 151 48 60 148 R R L 3 PLAN,STEP,STRIA SAMPLE

OL-KR25 402.48 156 33 164 29 33 187 R L N 3 UNDU,STRIA,GROV SAMPLE

OL-KR25 402.77 157 48 150 41 33 222 R L L 3 UNDU,STEP SAMPLE

OL-KR25 406.51 146 39 156 30 25 217 R L L 2 CONC,STRIA,GROV SAMPLE

OL-KR25 410.18 2 17 66 7 7 49 L L R 3 UNDU,STRIA SAMPLE

OL-KR25 456.05 170 48 167 45 50 128 N R L 3 PLAN,PSGR IMAGE

OL-KR25 485.09 no data no data 145 20 40 178 R L N 3 IRREG,STEP,STRIA,PSGR IMAGE

OL-KR25 485.13 no data no data 146 20 24 176 R L N 3 CONC,STEP,STRIA,PSGR IMAGE

OL-KR25 493.77 no data no data 106 31 35 139 R L R 2 PSGR, UNDU IMAGE

OL-KR25 521.60 172 33 no data no data 42 196 N R N 2 STRIA, PLAN SAMPLE

OL-KR25 556.34 no data no data 190 23 26 194 N R L 2 IRREG, STRIA, PSGR IMAGE

OL-KR25 556.43 191 38 186 27 35 231 L R N 3 CONC, STRIA, PSGR IMAGE

OL-KR25 571.73 no data no data 189 26 30 241 L R R 3 CONC, STRIA, PSGR IMAGE

OL-KR25 572.04 no data no data 188 46 45 179 N R N 3 UNDU, STRIA, PSGR IMAGE

OL-KR25 572.08 no data no data 205 25 27 239 L R R 3 IRREG, STRIA, PSGR IMAGE

OL-KR25 577.74 no data no data 321 8 18 311 N R N 2 UNDU, STRIA, PSGR IMAGE

OL-KR25 579.82 no data no data 217 27 1 129 no data no data no data no data STRIA, IRREG IMAGE

OL-KR25 583.53 39 47 38 40 17 111 L L N 3 UNDU, STRIA IMAGE

OL-KR25 587.12 66 17 143 27 3 354 L L R 3 PSGR, CONC, STEP SAMPLE

OL-KR25 600.95 162 39 no data no data 48 130 N L R 2 PLAN, STRIA SAMPLE

OL-KR25 601.05 146 40 no data no data 48 145 N L R 2 UNDU, STRIA, PSGR SAMPLE

OL-KR25 604.24 265 53 no data no data 48 225 no data no data no data no data PLAN SAMPLE

Lithology:

Fractures:

Tonalitic-granodioritic-granitic gneiss

Mica gneiss

Pegmatite/Pegmatitic granite

Diatexitic gneiss

Veined gneiss

Open Tight Filled Filled slick. Clay filled Grain filled

Ri: Ri III Ri IV Ri V

Core loss: Core loss interval Length of core loss due to drilling Length of core loss due to fracturing

Pervasive Fracture fillingsAlteration:

KR25

Zone intersections: Ductile shear zone Semibrittle fault zone Brittle joint zone Brittle fault zone

Diameter: 75.7 mm Azim./Tilt: 43.4/70.1 x/y/z (m): 6792079.94/1526000.00/8.02Length: 604.87 m

Cond. fractures

0 90

LogK2m

-10 -3m/s

Fracture T

-10 -3m2/s

Flow 2/0.25m 7.-8.1.2004

1 1e+006ml/h

Fractures ml/h

1 1e+006ml/h

Hydrology

Brittle

join

t zone

Brittle

fault z

one

Sem

ibrittle

fault z

one

Ductile

shear z

one

Zone

intersections

Kaolin

ite

Illite

Sulp

hid

es

AlterationRi Fractures

0 90

Lith. Foliation

0 90

Foliation orientationCore loss

Fract. freq.

0 201/m

Oriented fractures

0 90

Fracture orientation

Geology

Density

2 3.2g/cm3

Nat. gamma

0 90uR/h

Susceptibility

-10 2001E-5 SI

GeophysicsDepth

1m:200m

45

50

Veinedgneiss

0°0° -6.59

Page 1

Table 3. WellCAD-table of drillhole OL-KR25 182 APPENDIX 2

50

55

60

65

70

75

80

Diatexiticgneiss

180°

0°

180°

180°

0°

180°

-6.74

-6.19

-4.8

-6.13

-5.0

-5.78

-6.23

-6.61

-4.8

-6.78

-6.63

Page 2

183

85

90

95

100

105

110

Pegmatite/Pgranite

Diatexiticgneiss

0°

180°

0°

180°

0°

180°

0°

180°

-6.46

-6.46

-7.19

-7.09

-6.31

-4.8

Page 3

184

115

120

125

130

135

140

Pegmatite/Pgranite

Diatexiticgneiss

0°

180°

0°

180°

-6.75

-5.88

-7.07

Page 4

185

145

150

155

160

165

170

0°

180°

0°

180°

0°

180°

0°

180°

-6.95

Page 5

186

175

180

185

190

195

200

Pegmatite/Pgranite

Diatexiticgneiss

0°

180°

0°

180°

-7.06

Page 6

187

205

210

215

220

225

230

235

0°

180°

0°

180°

0°

180°

0°

180°

Page 7

188

240

245

250

255

260

265

Pegmatite/Pgranite

0°

180°

0°

180°

Page 8

189

270

275

280

285

290

295

Diatexiticgneiss

Micagneiss

0°

180°

0°

180°

0°

180°

0°

180°

Page 9

190

300

305

310

315

320

325

Pegmatite/Pgranite

Micagneiss

Veinedgneiss

Pegmatite/Pgranite

Micagneiss

Pegmatite/Pgranite

0°

180°

0°

0°

180°

0°

Page 10

191

330

335

340

345

350

355

Diatexiticgneiss

Veinedgneiss

180°

0°

180°

180°

0°

180°

-5.63

-5.73

-5.0

-4

-7.19

Page 11

192

360

365

370

375

380

385

390

0°

180°

0°

0°

180°

0°

-7.34

-4.7

-7.68

-8.73

Page 12

193

395

400

405

410

415

420

180°

0°

180°

180°

0°

180°

-7.83

-6.97

-7.54

Page 13

194

425

430

435

440

445

450

Micagneiss

Veinedgneiss

Pegmatite/Pgranite

0°

180°

0°

180°

0°

180°

0°

180°

Page 14

195

455

460

465

470

475

480

Veinedgneiss

Pegmatite/Pgranite

Veinedgneiss

Pegmatite/Pgranite

Veinedgneiss

Pegmatite/Pgranite

Veinedgneiss

0°

180°

0°

180°

Page 15

196

485

490

495

500

505

510

Pegmatite/Pgranite

Veinedgneiss

Tonalitic-gragneiss

Veinedgneiss

0°

180°

0°

180°

0°

180°

0°

180°

-9.14

-8.37

Page 16

197

515

520

525

530

535

540

545

Micagneiss

Pegmatite/Pgranite

0°

180°

0°

180°

-8.07

Page 17

198

550

555

560

565

570

575

g

Tonalitic-gragneiss

Veinedgneiss

Pegmatite/Pgranite

0°

180°

0°

180°

0°

180°

0°

180°

-7.19

Page 18

199

580

585

590

595

600

605

Veinedgneiss

Pegmatite/Pgranite

Micagneiss

0°

180°

0°

180°

Page 19

200

201 APPENDIX 3

ID OL-BFZ001

DIMENSIONS X/Y/Z, m 200/200/41

DESCRIPTION OL_KR6_BFI_50596_50933

Densely-fractured intersection in veined gneiss. Random fracturing wit fractures parallel to and cross-cutting foliation. An older small-scaled microfracturing and -breakage, which is welded. On slickensides graphite-coatings can be seen. One observation on direction vector, FDV = 40°/14°. Drilling-induced splitting of the core sample.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

No other kinematic data.

Gently dipping, planar feature. Dip/dip direction 11/224. Fault vector orientation 14/176.

INTERSECTIONS OL_KR6_BFI_50596_50933

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

0 Very low (0= very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR6: 480.5 – 506 Rp0, 506 – 509.5 Rp1 OL-KR6: 506.88 – 508.85 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR06_12R

UPDATES - version history V 0 FILE Group_a_1.dtm

COMPILATION DATE AND COMPILED BY

12.12.2005 Markku Paananen

APPENDIX 3 202

ID OL-BFZ002

DIMENSIONS X/Y/Z, m 646/1054/306

DESCRIPTION OL_KR1_BFI_61030_61920

In borehole KR1 at 613-618 the veined gneiss and the pegmatitic granite, are strongly altered and fractured (Blomqvist et al. 1992). In many places the rock has been mangled into clayey material, mostly composing of chlorite, and this material also fills the fractures. These fractures have in places opened and the rock has been altered, including sericitization, saussuritization, silicification and albitisation. In places, the silicification and albitisation have closed the fractures, and these fracture veins have later been deformed with injection of calcite in various phases. The above altered and fractured parts have later thoroughly illitized, after which slickensided fractures, breccias, and abundant filled fractures and cavities have been formed. A total of 21 fracture infillings are detected and they are classified into five groups according to decreasing temperature and age (Blomqvist et al. 1992). Two oldest groups are hydrothermal (T <300°C) and the fracture infillings are characterised by muscovite-greisen fractures, silicified microbreccias, albite veins and quartz veins. The younger hydrothermal group is characterised by clay minerals, especially illite, crystallised on chlorite shear planes and fractures. Other typical fracture infillings include pyrrhotite, baryte, laumontite-leonhardite, analsime, adular and fluorite. Pyrite veins, calcite-chamosite breccias and infillings of the third group cut the two previous groups. The fourth group is characterised by clay minerals with formation temperatures between 150°C and 40°C. Plagioclase is altered to kaolinite. The youngest group consists of monomineralic calcite infillings, or breccias with anatase on the walls of minor cavities. The dated calcites indicate crystallisation ages of less than 300 000 years (Blomqvist et al. 1992).

OL_KR19_BFI_46475_46532

The intersection is composed of DTX. The rock contains a few old, welded, calcite and pyrite bearing fractures. The intersection consists 10 fractures. The fractures dip direction and dip is scattered. Four slickenside surfaces are also observed (scattered orientation of striation). Almost every fracture in the intersection is water conductive. At 465.22-465.32 drill core is taken for analysis (by Kivitieto Oy).

OL_KR19_BFI_47667_47793

The intersection is composed of VMGT. The intersection contains a few old, welded fractures with calcite infillings. The intersection contains 5 slickenside fractures. The fractures dip directions are towards SE with almost horizontal plunge. The rock in the intersection is evenly fractured. The fracture at 477.93 shows water conductivity (kaoline infilling).

KINEMATICS OF THE ZONE – IF POSSIBLE

Group A

U = N E = L S = N

Normal fault

APPENDIX 3 203

ORIENTATION/GEOMETRY OF THE ZONE

Gently dipping, planar feature. Dip/dip direction 17/180. Mean fault vector orientation 14/180.

INTERSECTIONS OL_KR1_BFI_61030_61920 OL_KR19_BFI_46475_46532 OL_KR19_BFI_47667_47793 Single fault planes at OL-KR2 540.82 – 547.13 Single fault planes at OL-KR6 440.82 – 451.11

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersections, kinematics, VSP

3 High (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR1: 576.6 – 613.0 Rp0, 613.0 – 618.5 Rp1, 618.5 – 636.45 Rp0 OL-KR1: 613.18 – 617.61 RiIII

OL-KR2: 513.0 – 570.0 Rp0 OL-KR2: 534.41 – 541.67 RiIII, 542.89 – 543.34 RiIII, 543.98 – 544.79 RiIII

OL-KR6: 369.50 – 463.00 Rp0

OL-KR19: 461.48 – 467.10 Rp1, 467.10 – 481.11 Rp0(1) OL-KR19: 464.59 – 465.32 RiIV

COMPARISON TO BEDROCK MODEL 2003/1

RH21, RH9, KR02_7R

UPDATES - version history V 0 FILE Group_a_2.dtm

COMPILATION DATE AND COMPILED BY

12.12.2005 Markku Paananen

APPENDIX 3 204

ID OL-BFZ003

DIMENSIONS X/Y/Z, m 200/250/46

DESCRIPTION OL_KR19_BFI_41236_41462

The intersection is composed of DTX. The intersection contains old, welded fractures with calcite infillings. The intersection contains 14 joints. The fractures dip directions are towards SE with moderate dip. The rock in the intersection is more fractured at 412.36-413.11 (10 fractures). The majority of the fractures (8) in the intersection exhibit a slickenside surface, with the striation direction towards E with almost horizontal plunge. At 413.11-413.20 and 414.62 the fractures show water conductivity (kaoline infilling).

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U = R E = R S = L

Right-normal fault

Moderately dipping, planar feature. Dip/dip direction 38/252. Fault vector orientation 25/179.

INTERSECTIONS OL_KR19_BFI_41236_41462

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

0 Very low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR19: 408.02 – 412.99 Rp0(1), 412.99 – 456.37 Rp0

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_3.dtm

COMPILATION DATE AND COMPILED BY

12.12.2005 Markku Paananen

APPENDIX 3 205

ID OL-BFZ004

DIMENSIONS X/Y/Z, m 300/386/25

DESCRIPTION OL_KR13_BFI_31880_32500

The intersection is composed of GGN. The fractures have a random direction with moderate to steep dip. The intersection contains 14 joints, app. 2-3 fractures per 1 metre. The intersection exhibits 5 slickenside surfaces, which are randomly orientated (moderate dip). Rock is strongly foliated.

OL_KR19_BFI_25335_25982

The intersection is mainly composed of VMGT with a short section of GRPG. The rock contains old, welded, calcite bearing fractures. Here and there the feldspars are altered (sericitized). The intersection contains 58 joints. The fractures are randomly orientated. 5 fractures in the intersection exhibit a slickenside surface, with the striation direction towards SW with moderate plunge. The intersection contains three gouges (rock fragments in dark clay and/or calcite matrix) at 253.60-253.70, 255.05-255.22 and 255.52-256.17. The rock in the intersection is evenly fractured having an average of 10 fractures/m. The fractures at 253.64-255.58 and 259.01-259.63 show signs of water conductivity (kaoline infillings). Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U = N E = R, L S = R, L Contradictory kinematic information

Normal fault

Gently dipping planar feature. Dip/dip direction 17/210. Mean fault vector orientation 23/180.

INTERSECTIONS OL_KR13_BFI_31880_32500 OL_KR19_BFI_25335_25982

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersections, kinematics

1 Low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR13: 248.88 – 345.45 Rp0

OL-KR19: 248.43 – 259.63 Rp1, 259.63 – 262.96 Rp0-1 OL-KR19: 253.64 – 254.00 RiIV, 259.01 – 259.63 RiIV

APPENDIX 3 206

COMPARISON TO BEDROCK MODEL 2003/1

R2 in OL-KR19

UPDATES - version history V 0 FILE Group_a_4.dtm

COMPILATION DATE AND COMPILED BY

12.12.2005 Markku Paananen

APPENDIX 3 207

ID OL-BFZ005

DIMENSIONS X/Y/Z, m 681/268/467

DESCRIPTION OL_KR13_BFI_31880_32500

The intersection is composed of GGN. The fractures have a random direction with moderate to steep dip. The intersection contains 14 joints, app. 2-3 fractures per 1 metre. The intersection exhibits 5 slickenside surfaces, which are randomly orientated (moderate dip). Rock is strongly foliated.

OL_KR14_BFI_44500_44908

The intersection is composed of VMGT and in the latter part of MAFGN and MGN. The intersection contains 28 joints. The fractures dip direction and dip is scattered, with a concentration of fractures showing a dip direction towards SE with a moderate dip. The rock in the intersection has an average of 7 fractures/m. The central part of the intersection contains two sections (446.40-446.83 & 447.68-448.13) of intensely fractured and partly crushed rock. The latter section exhibit slightly altered feldspars (white-green alteration) and it also show signs of water conductivity (grey clay infillings). The majority of the fractures (16) in the intersection exhibit a slickenside surface, with two different striation direction one towards NE and the other towards SE. The striations have a moderate plunge. Seven of these slickenside surfaces indicate a R, L, L movement. Mechanical fracturing has occurred during the drilling.

OL_KR15_BFI_44962_45600

The intersection is composed of MGN. The rock exhibits a few old, welded, calcite bearing fractures. The fractures are randomly orientated with horizontal to moderate dip. The intersection contains 53 joints, with a more fractured part (449.85-451.95) exhibiting 36 fractures. The slickensides (only 5) have striation trend of NE-SW with moderate plunge. Some fractures (at least at 451.25, containing dark, unidentified clay mineral) might act as a water channels, but no water conductive measurements has been carried out in this part of the borehole. Mechanical fracturing has occurred during the drilling.

OL_KR19_BJI_15517_15698

The intersection is composed of VMGT. The rock contains old, welded, calcite bearing fractures, which have been reactivated later. The intersection contains 20 joints (ca. 10 fractures/m). The fractures are randomly orientated. The rock in the intersection is evenly fractured. Most of the fractures show signs of water conductivity (kaoline infillings). Mechanical fracturing has occurred during the drilling.

OL_KR21_BFI_27577_28100

The intersection is mainly composed of intensely banded VMGT that is slightly altered (kaolinitization and epidotisation) and some small sections of GRPG that contain some small garnets. The intersection contains one set of joints parallel to the foliation is present (dip/dip direction 30/173°), 31 joints of which 5 are slickensides. The slickensides have striations in a NNE-SSW direction plunging 40 degrees towards north. The joints have infillings of kaolinite and epidote. No signs of water conductivity are visible.

APPENDIX 3 208

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

Contradictory kinematic information.

Reverse or normal fault

Gently dipping planar feature. Dip/dip direction 28/167. Mean fault vector orientation 25/181.

INTERSECTIONS OL_KR13_BFI_31880_32500 OL_KR14_BFI_44500_44908 OL_KR15_BFI_44962_45600 OL_KR19_BJI_15517_15698 OL_KR21_BFI_27577_28100 Single fault planes at OL-KR7 577.41 – 586.35

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersections, kinematics, VSP

3 High (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR13: 248.88 – 345.45 Rp0

OL-KR14: 415.22 – 447.83, 447.83 – 448.07, 448.07 – 470.03 Rp0 OL-KR14:

OL-KR19: 149.67 – 157.93 Rp0-1 OL-KR19: 155.27 – 155.84 RiIII

OL-KR21: 206.95 – 301.08 Rp0(Rp1)

COMPARISON TO BEDROCK MODEL 2003/1

KR15_4R

UPDATES - version history V 0 FILE Group_a_5.dtm

COMPILATION DATE AND COMPILED BY

12.12.2005 Markku Paananen

APPENDIX 3 209

ID OL-BFZ006

DIMENSIONS X/Y/Z, m 71/71/72

DESCRIPTION OL_KR19_BJI_11400_11568

The intersection is composed of VMGT and GRPG. The rock contains old, welded, calcite and mica bearing fractures. The feldspars in whole intersection are altered (sericitized). The intersection contains 19 joints. The fractures are randomly orientated. The rock in the intersection is more fractured at 114.34-114.75 (9 fractures). In that part there are two gouges (small rock particles in grey clay matrix). Most of the fractures show signs of water conductivity (kaoline infillings). Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

No other kinematic data.

Fault

Moderately dipping planar feature. Dip/dip direction 45/235. Fault vector orientation 17/191.

INTERSECTIONS OL_KR19_BJI_11400_11568

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

0 Very low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR19: 113.47 – 115.10 Rp1-2 OL-KR19: 113.99 – 114.76 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

RH20C

UPDATES - version history V 0 FILE Group_a_6.dtm

COMPILATION DATE AND COMPILED BY

12.12.2005 Markku Paananen

APPENDIX 3 210

ID OL-BFZ007

DIMENSIONS X/Y/Z, m 250/208/140

DESCRIPTION OL_KR19B_BJI_1870_2362

The intersection is MAINLY composed of MGN with short sections of GRPG (22.75-23.10) and VMGT (22.00-22.75 and 23.10-23.62). The intersection contains old, welded, calcite bearing fractures. Some of them have been reactivated later. The intersection contains 45 fractures, which are randomly orientated. Two fractures in the intersection exhibit a slickenside surface, one (at 23.15) with the striation direction towards SE with almost horizontal plunge and another ss-surface (at 23.17), which is shattered. The rock in the intersection is evenly fractured (app. 8 fractures/m). Most of the fractures show signs of water conductivity (kaoline infillings). Mechanical fracturing has occurred during the drilling. At 20.61 there is 0.07 m core loss.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=NE=LS=N

Strike-slip fault

Gently dipping planar feature. Dip/dip direction 33/108. Fault vector orientation 12/175.

INTERSECTIONS OL_KR19B_BJI_1870_2362

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

0 Very low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR19B: 11.05 – 19.43 Rp1, 19.43 – 19.58 Rp2, 19.58 – 19.61 Rp3, 19.61 – 20.17 Rp1, 20.17 – 20.41 Rp1-2, 20.41 – 24.08 Rp1

OL-KR19B: 19.25 – 20.67 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR19B_3RH

UPDATES - version history V 0 FILE Group_a_7.dtm

COMPILATION DATE AND COMPILED BY

12.12.2005 Markku Paananen

APPENDIX 3 211

ID OL-BFZ008

DIMENSIONS X/Y/Z, m 155/106/116

DESCRIPTION OL_KR13_BJI_3385_4604

Intersection is composed of DTX with short section of QUAR. Some of the feldspars have been slightly altered to epidote. The DTX intersection contains old and welded fractures where calcite is present. These old fractures have partly been reactivate later. There are two fracture sets, one horizontal and one vertical with a N-S trend. The intersection contains 93 joints. Most of the fractures are water conductive. Some mechanical fracturing has occurred during the drillings. Core loss in depth of 35.34 (5 cm) and 41.90 (12 cm).

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

No other kinematic data

Fault

Gently dipping planar feature. Dip/dip direction 10/107. Fault vector orientation 20/193.

INTERSECTIONS OL_KR13_BJI_3385_4604

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

0 Very low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR13: 21.03 – 38.35 Rp0(Rp1), 38.35 – 43.90 Rp0-1, 43.90 – 49.27 Rp0

COMPARISON TO BEDROCK MODEL 2003/1

KR13_2RH

UPDATES - version history V 0 FILE Group_a_8.dtm

COMPILATION DATE AND COMPILED BY

12.12.2005 Markku Paananen

APPENDIX 3 212

ID OL-BFZ009

DIMENSIONS X/Y/Z, m 260/470/225

DESCRIPTION OL_KR21_BFI_20484_22070

The rock in the intersection is mostly composed of VMGT that is moderately kaolinitised, epidotised and sericitised at places, at 216-218 m a section of coarse grained GRPG occurs. The intersection contains 88 joints that are quite randomly orientated but one set parallel to the foliation can be distinguished (dip/dip direction 21/180). 9 joints are slickensides with striations in a N-S direction usually plunging about 40 degrees towards north. The movement has often been LLR handed. The joints often have infillings of kaolinite and calcite. Some show signs of water conductivity and have thick greyish clay infillings.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=LE=RS=R

Normal fault

Gently dipping planar feature. Dip/dip direction 26/173. Fault vector orientation 32/192.

INTERSECTIONS OL_KR21_BFI_20484_22070 Single fault plane at OL-KR19 89.58 m.

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersections, kinematics

1 Low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR21: 206.95 – 301.08 Rp0(Rp1) OL-KR21: 205.06 – 206.95 RiIII

OL-KR19: 66.30 – 93.50 Rp0-1 COMPARISON TO BEDROCK MODEL 2003/1

KR21_3

UPDATES - version history V 0 FILE Group_a_9.dtm

COMPILATION DATE AND COMPILED BY

12.12.2005 Markku Paananen

APPENDIX 3 213

ID OL-BFZ010

DIMENSIONS X/Y/Z, m 150/140/165

DESCRIPTION OL_KR3_BFI_15820_16275

Pegmatite containing voluminous mica-rich parts, around, which the rock has slipped and plenty of slickensides were born. Slight alteration, some pyrite on fracture surfaces and sporadic illite-coatings.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

No other kinematic data

Normal or reverse fault

Moderately dipping planar feature. Dip/dip direction 50/190. Fault vector orientation 42/175.

INTERSECTIONS OL_KR3_BFI_15820_16275

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

0 Very low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR3: 68.05 – 246.10 Rp0 OL-KR3: 158.97 – 161.69 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

R10A

UPDATES - version history V 0 FILE Group_a_10.dtm

COMPILATION DATE AND COMPILED BY

12.12.2005 Markku Paananen

APPENDIX 3 214

ID OL-BFZ011

DIMENSIONS X/Y/Z, m 100/191/0.4

DESCRIPTION OL_KR9_BFI_14733_14956

Veined gneiss and a crosscutting narrow pegmatite. Fractured, slickensides, sulphide-fillings and porosity. Fractures are quite parallel. Drilling has an effect on splitting of sample. TV image displays no open fractures. A real breakage.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

No other kinematic data

Fault

Subhorizontal planar feature. Dip/dip direction 15/095. Fault vector orientation 6/009.

INTERSECTIONS OL_KR9_BFI_14733_14956

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

0 Very low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

RH24

UPDATES - version history V 0 FILE Group_a_11.dtm

COMPILATION DATE AND COMPILED BY

12.12.2005 Markku Paananen

APPENDIX 3 215

ID OL-BFZ012

DIMENSIONS X/Y/Z, m 300/261/194

DESCRIPTION OL_KR27_BFI_8450_9650 The intersection contains mostly VMGT and short sections of GRPG (88.03-88.75 & 91.77-92.40) and a grey-red, fine-medium grained, sheared rock that resembles VMGT (86.31-88.03 & 92.80-94.25). The VMGT is greenish in colour, due to probable illite alteration. The GRPG exhibits a red oxidation (palaeo) mineral. The intersection is strongly altered and shows a palaeo shearing which probably later has been reactivated. The rock is partly porous, because of mineral leaching. The rock exhibits in one joint a black mineral (goethite?) and a few gouges with unidentified clay minerals. The intersection contains some slickenside surfaces but no directions can be observed. Water flowing has been determined in following joints 84.60, 86.40, 88.00, 89.80, 92.75 & 95.50. The fractures mostly follow the foliation in VMGT, but the grey-red, fine- to medium-grained rock have several fracture directions. The intersection also contains old, randomly oriented "welded" fractures; fractures are welded by calcite. The drilling has partly crushed the rock.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

No other kinematic data

Fault

Subhorizontal planar feature. Dip/dip direction 53/128. Fault vector orientation 32/176.

INTERSECTIONS OL_KR27_BFI_8450_9650

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

0 Very low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR27: 84.07 – 86.36 Rp1(Rp2), 86.36 – 86.66 Rp2-3, 86.66 – 90.77 Rp2, 90.77 – 91.20 Rp2-3, 91.20 – 92.41 Rp2, 92.41 – 95.68 Rp2-3 OL-KR27: 86.31 – 86.66 RiV, 86.66 – 88.61 RiIII, 89.77 – 90.14 RiIV, 90.14 – 93.15 RiIII, 93.15 – 94.22 RiIV, 94.22 – 94.85 RiIII, 94.85 – 95.07 RiIV, 95.07 – 95.48 RiIII, 95.48 – 95.70 RiV

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_12.dtm

COMPILATION DATE AND COMPILED BY

12.12.2005 Markku Paananen

APPENDIX 3 216

ID OL-BFZ013

DIMENSIONS X/Y/Z, m 86/240/224

DESCRIPTION OL_KR27_BFI_12816_12960

K-feldspar porphyric GGGN. The K-feldspar phenocrysts are 0.5-3 cm. The intersection starts (128.56) and ends (129.54) in water conducting fractures, which contains greenish "silt-sand". No alteration observed. The intersection also contains old, randomly oriented "welded" fractures; fractures are welded by calcite. The fractures are randomly orientated.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A U=RE=LS=L

Right-reverse fault

Steeply dipping planar feature. Dip/dip direction 69/080. Fault vector orientation 30/170.

INTERSECTIONS OL_KR27_BFI_12816_12960

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

0 Very low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR27: 128.18 – 130.63 Rp1 OL-KR27: 128.23 – 129.60 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_13.dtm

COMPILATION DATE AND COMPILED BY

12.12.2005 Markku Paananen

APPENDIX 3 217

ID OL-SFZ014

DIMENSIONS X/Y/Z, m 140/400/372

DESCRIPTION OL_KR27_SFI_33385_34842

The intersection contains DTX that is strongly sheared and contains a lot of paleofractures of which some are reactivated and occurred as joints and slickenside surfaces. The rock contains a lot of angular, altered feldspar crystals, which show a cataclastic structure. The diameter of the feldspars is usually a couple of millimetres but crystal up to 4 cm in length are present. On both sides of this intersection there is a 25 m wide zone where the rocks occasionally show some weak signs of semi-brittle deformation. The intersection contains a 3.25 m wide section, which is strongly fractured and faulted (see below).

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

Contradictory kinematic data

Semi-brittle strike-slip fault

Steeply dipping planar feature. Dip/dip direction 70/109. Fault vector orientation 10/350 or 26/177.

INTERSECTIONS OL_KR27_SFI_33385_34842

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

1 Low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR27: 338.31- 344.73 Rp1, 344.73 – 351.96 Rp0-1 OL-KR27: 338.21 – 339.77 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_14.dtm

COMPILATION DATE AND COMPILED BY

13.12.2005 Markku Paananen

APPENDIX 3 218

ID OL-BFZ015

DIMENSIONS X/Y/Z, m 88/201/180

DESCRIPTION OL_KR8_BFI_30393_30675

Chlorite-, calcite- and illite-coated fractures at depth of 303.93 - 304.65 m. In places the feldspars of granitic veins in mica gneiss are greenish due to strong illitization. Quartz vein in the altered and fractured intersection between 304.80 - 305.60 m shows cavities, which are filled by some mineral (quartz?). Many slickensides almost parallel to core sample between 305.60 - 306.00. In the bottom of the intersection there is one water-conductive fracture.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A U=LE=RS=N, R

Left-normal fault

Steeply dipping planar feature. Dip/dip direction 64/92. Mean fault vector orientation 13/011.

INTERSECTIONS OL_KR8_BFI_30393_30675

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

2 Moderate (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR8: 303.93 – 305.97 RiIII OL-KR8: 82.50 – 415.60 Rp0

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_15.dtm

COMPILATION DATE AND COMPILED BY

13.12.2005 Markku Paananen

APPENDIX 3 219

ID OL-BFZ016

DIMENSIONS X/Y/Z, m 352/324/143

DESCRIPTION OL_KR8_BFI_37600_38300

The intersection is composed of DTX, with some short sections of MAFGN. The intersection contains old and welded fractures where calcite is present. These old fractures have partly been reactivated later. The fractures dip direction is towards NE, with moderate to steep dip. The intersection contains 50 joints. The rock is most fractured in section 379.18-379.80, containing 18 fractures. The intersection exhibits 14 slickenside surfaces with a NE-SW striation trend. The movement on surfaces is random. No mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=R, N E=N, R S=L, N

Normal or right-reverse fault

Gently dipping planar feature. Dip/dip direction 23/205. Fault vector orientation 20/008 or 30/176.

INTERSECTIONS OL_KR8_BFI_37600_38300

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

2 Moderate (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR8: 316.77 – 379.21 Rp0, 379.21 – 382.83 Rp0(1), 382.82 – 401.03 Rp0 OL-KR8: 378.46 – 379.76 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR08_11R

UPDATES - version history V 0 FILE Group_a_16.dtm

COMPILATION DATE AND COMPILED BY

13.12.2005 Markku Paananen

APPENDIX 3 220

ID OL-SFZ017

DIMENSIONS X/Y/Z, m 179/461/36

DESCRIPTION OL_KR23_SFI_4030_5966

The upper part of this zone is visible in the last 5 m (40-45m) of KR23B. The intersection contains mostly DTX that at the end gradually gets the typical banded texture of VMGT. The rock is abundant in reddish granite pegmatite neosome. The rock is sheared and deformed in a semi-brittle fashion, a bit weathered, altered (chloritized and kaolinitized) but still cohesive. The rock is cataclastic and contains angular (broken) crystals of feldspar and quartz, the crystals vary in size from a couple of millimetres to 3 cm (mostly 1 cm). The rock is not evenly deformed and some small, undeformed sections occur. The feldspar and quartz grains often lie scattered in a dark greyish or greenish matrix, probably mica. The rock contains many old, healed fractures that give the rock a brecciated look at places. The healed fractures contain mostly pyrite, calcite and a dark greyish green matrix (fault gauge?). Inside this intersection lies the younger and brittle intersection BJI_OL_KR23_04410-05580 (see below).

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=RE=LS=L

Left normal or left reverse fault

Subhorizontal planar feature. Dip/dip direction 9/232. Fault vector orientation 9/181.

INTERSECTIONS OL_KR23_SFI_4030_5966

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

1 Low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR23: 40.30 – 48.24 Rp1, 48.24 – 55.86 Rp2, 55.86 – 60.46 Rp1 OL-KR23: 44.17 – 45.19 RiIII, 47.25 – 55.68 RiIII, RiIV (RiV)

COMPARISON TO BEDROCK MODEL 2003/1

KR23_1R

UPDATES - version history V 0 FILE Group_a_17.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Markku Paananen

APPENDIX 3 221

ID OL-BFZ018

DIMENSIONS X/Y/Z, m 344/161/92

DESCRIPTION OL_KR4_BFI_8154_8239

Tectonic breccia or protocataclastite in which the average diameter of the fragments exceeds 0.5 cm and the proportion of the fault rock is 10 – 15%. Products of pervasive alteration: sulphides, kaolinite and illite. Late stage fractures are often coplanar with ancient mylonitic foliation.

OL_KR22_BJI_14965_15280

This intersection contains DTX with a slightly banded texture at places. The intersection contains 31 fractures and has an average joint density of 10 joints / m. Some old and healed joints with calcite and pyrite occur. There is only one set of joint in this intersection. The joint are parallel to the foliation and have dip/dip directions of about 25/130 degrees. At 151.7 m there is two fractures that conduct water.

OL_KR24_BJI_11255_11620

The intersection is composed of clearly banded VMGT, GRPG and DTX. The intersection contains 36 joints and has an average joint density of 10 joints / m. The fractures are randomly orientated. Between 115.40-116.20 m the GRPG is a bit sheared and porphyric. The GRPG contains old, welded calcite bearing fractures and paleoshears with a fine-grained matrix. This section is also the most densely fractured (17 fractures) and some of these fractures has signs of water conductivity. The typical joint infillings in this section are chlorite and calcite.

OL_KR25_BJI_9445_9730

The intersection is composed of VMGT. The intersection contains old and welded fractures where pyrite and some calcite are present. These old fractures have partly been reopened during drilling. The rock has a clear foliation and the fracturing follow it. All the fractures has a NE-SW direction and a moderate dip. The intersection contains 21 joints, ca. 7 fractures / m. The rock is weathered, crushed and altered in section 96.35-96.66. The section also exhibits clear water conductivity signs. Some mechanical fracturing has occurred during the drillings.

OL_KR28_BFI_17021_17830

Mainly VMGT with short sections of GRPG and MGN. In VMGT (from 170.21 to 173.50) there are about 7 fractures/ 1 metre. Two slickenside surfaces are also observed. They seem to be created into paleofractures which may have been reactivated. There are red feldspar crystals (rounded) in VMGT. Old welded biotite, pyrite and calcite infillings are observed. In some places feldspars are sericitized. 172.65-172.70 crushed drillcore. 173.50- 174.00 MGN with some old welded calcite bearing fractures. 174.00-174.12 several fractures in random directions. In depth of 174.12-174.90 VMGT contains some slickensides (NE orientated). 174.90-175.85 GRPG contains some fractures in random orientation and old welded calcite bearing fractures. 175.85-178.00 VMGT contains only a few fractures in random orientation. In sections of 168.50-171.99 and 172.90-173.16 there are water conductive fractures.

APPENDIX 3 222

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=RE=LS=L

Fault

Moderately dipping planar feature. Dip/dip direction 36/150. Fault vector orientation 24/182.

INTERSECTIONS OL_KR4_BFI_8154_8239 OL_KR22_BJI_14965_15280 OL_KR24_BJI_11255_11620 OL_KR25_BJI_9445_9730 OL_KR28_BFI_17021_17830

BASIS FOR INTERPRETATION

CONFIDENCE

Mise-a-la masse, drillhole intersections

0 Very low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR4: 81.30 – 83.50 Rp2 OL-KR4: 81.41 – 82.61 RiIII

OL-KR22: 113.45 – 152.25 Rp0(Rp1), 152.25 – 165.44 Rp0 OL-KR22: 151.04 – 151.87 RiIII

OL-KR24: 111.93 – 115.03 Rp0-1, 115.03 – 115.85 Rp0, 115.85 – 116.57 Rp0-1 OL-KR24: 115.24 – 115.84 RiIII

OL-KR25: 69.4 – 96.10 Rp0-1, 96.10 – 96.70 Rp1-2, 96.70 – 113.40 Rp0-1 OL-KR25: 96.09 – 96.73 RiIII

OL-KR28: 169.20 – 178.50 Rp1 – (Rp2) OL-KR28: 172.35 – 174.11 RiIII, 172.60 – 173.20 RiIV, 175.50 – 176.60 RiIII, 177.02 – 178.02 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

RH19A KR22_4RH

UPDATES - version history V 0 FILE Group_a_18.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Markku Paananen

APPENDIX 3 223

ID OL-BFZ019

DIMENSIONS X/Y/Z, m 270/332/137

DESCRIPTION OL_KR10_BFI_27147_27159

A set of parallel slickensides, which crosscuts ductile foliation. Presumably slickensides are quite steeply-dipping. On fracture surfaces a slight pyrite coatings.

OL_KR14_BFI_21755_21913

The intersection is composed of VMGT. The fractures seem to mainly be parallel to the foliation, but no certainty could be established because of absent Wellcad picture. The intersection contains 8 joints, with an average of ca. 4 fractures/m. The intersection contains 5 fractures with slickenside surface, but due to the absent Wellcad picture no direction and movement could be established. No signs of water conductivity.

OL_KR25_BFI_34700_35225

The intersection contains mostly VMGT and a DTX part. The rock is mostly clearly foliated but the DTX part in section 348.92-349.75 is heterogenous and irregular. The intersection contains 50 joints, with an average of 7-11 fractures/m. The fractures in the intersection have a nearly horizontal dip and thus there orientation varies. The rock is more fractured in the section between 350.50-351.70; this section contains 22 fractures. The rock in this section shows minor signs of semi-brittle shearing, with some cataclastic features and alteration of the feldspars. It also contains some calcite healed fractures. This fractured section also exhibits some water conducting fractures in the beginning of it, with grey clay infillings. The intersection also contains several slickenside surfaces, but no directions or movements could be observed. The horizontal nature of the fracturing in this section can partly probably be explained by the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=LE=LS=L

Left-normal fault

Gently dipping planar feature. Dip/dip direction 14/263. Fault vector orientation 7/192.

INTERSECTIONS OL_KR10_BFI_27147_27159 OL_KR14_BFI_21755_21913 OL_KR25_BFI_34700_35225

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersections, kinematics, VSP

1 Low (0=very low, 1=low, 2=moderate, 3=high)

APPENDIX 3 224

HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR10: 260.65 – 326.10 Rp0 OL-KR10: 271.41 – 271.82 RiIII

OL-KR14: 184.22 – 292.00 Rp0

OL-KR25: 347.3 – 350.56 Rp0-1, 350.56 – 350.82 Rp2, 350.82 – 351.66 Rp1, 351.66 – 355.70 Rp0-1 OL-KR25: 348.27 – 349.14 RiIII, 350.41 – 351.66 RiIII/RiIV

COMPARISON TO BEDROCK MODEL 2003/1 UPDATES - version history V 0 FILE Group_a_19.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Markku Paananen

APPENDIX 3 225

ID OL-BFZ020

DIMENSIONS X/Y/Z, m 30/210/210

DESCRIPTION OL_KR25_BFI_57155_57800

The intersection is composed of VMGT and GRPG. GRPG sections have old welded calcite bearing fractures. Fractures exhibit dip direction towards NW with a nearly horizontal dip. The intersection contains 8 slickenside surfaces, but the orientation of the striation varies. Some of the fractures are water conducting. These fractures contain kaolinite and greyish clay infillings. The intersection contains ca 40 joints, with 13 fractures/0.7 m (576.21-576.91). Some mechanical fracturing has occurred during the drillings.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=NE=RS=N

Normal fault

Moderately dipping planar feature. Dip/dip direction 46/188. Fault vector orientation 45/179.

INTERSECTIONS OL_KR25_BFI_57155_57800

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

0 Very low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR25: 572.2 – 577.90 Rp0.1 OL-KR25: 576.02 – 576.87 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_20.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Markku Paananen

APPENDIX 3 226

ID OL-BFZ021

DIMENSIONS X/Y/Z, m 100/90/44

DESCRIPTION OL_KR29_BJI_25147_25184

Intersection of slightly altered and weathered VMGT with 9 fractures. Clay mineral infillings. Biotite rich bands and neosome bands. Fractures mainly in direction of foliation. Foliation is dipping gently to SE. Pinite occurs in neosome veins. Weak striation in one fracture face. Set of fractures is water conductive according to flow measurements.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

No other kinematic data

Fault

Gently dipping planar feature. Dip/dip direction 26/133. Fault vector orientation 21/170.

INTERSECTIONS OL_KR29_BJI_25147_25184

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

0 Very low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR29: 251.00 – 252.35 Rp1-2 OL-KR29: 251.22 – 251.78 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_21.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Markku Paananen

APPENDIX 3 227

ID OL-BFZ022

DIMENSIONS X/Y/Z, m 140/151/54

DESCRIPTION 4 single slickensided fractures at OL-KR29 321.1 – 324.8 m

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=R, N, L, R E=L, L, R, L S=N, N, L, L

Fault

Gently dipping planar feature. Dip/dip direction 21/050. Mean fault vector orientation 17/001.

INTERSECTIONS 4 single fault planes at OL-KR29 321.1 – 324.8 m

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

0 Very low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR29: 320.2 – 333.50 Rp1 (Rp2) OL-KR29: 321.14 – 322.14 RiIII, 322.71 – 325.58 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_22.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Markku Paananen

APPENDIX 3 228

ID OL-BFZ023

DIMENSIONS X/Y/Z, m 536/278/232

DESCRIPTION OL_KR29_BFI_53300_54855 The intersection is composed of VMGT and DTX, with some short sections of GRPG. The feldspars are often altered to illite. The rock in the intersection also contains plenty of cordierite (1.5 cm) and some garnet grains (1.0 cm), which are metamorphosed. The intersection contains a few old and welded fractures with calcite and pyrite infillings, especially in the GRPG. Several of the fractures contain kaolinite and illite infillings. Accordingly, a majority of the fractures show signs of water conductivity and some of them also exhibit green-grey clay infillings. There is, however, no indication of water flow in the flow measurements. The intersection exhibits 61 fractures, with a dip direction towards SE and a moderate dip. The rock is more fractured at the following section 543.80-547.12 (37 joints). The intersection exhibit 29 fractures with a slickenside surface, which have a striation direction varying from SE to SW, with a moderate plunge. Some mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=LE=RS=R

Left-normal fault

Moderately dipping planar feature. Dip/dip direction 39/130. Mean fault vector orientation 22/181.

INTERSECTIONS OL_KR29_BFI_53300_54855 Single fault planes at OL-KR7 467.55 – 475.80 m

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersections, kinematics

2 Moderate (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR29: 514 – 536.50 Rp0(Rp1), 536.50 – 543.80 Rp0 (Rp1), 543.80 – 546.40 Rp1 (Rp2), 546.4 – 556.85 Rp0(Rp1) OL-KR29: 543.82 – 546.42 RiIII - RiIV

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_23dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Markku Paananen

APPENDIX 3 229

ID OL-BFZ024

DIMENSIONS X/Y/Z, m 180/124/128

DESCRIPTION OL_KR29_BJI_55676_56035

The intersection is composed of DTX, with a short section of GRPG in the beginning. Some of the feldspars are altered to illite. The intersection contains a few old and welded fractures with calcite infillings. Some of the fractures contain kaolinite and illite infillings. These fractures show signs of water conductivity and some of them (559.86, 559.89 & 559.92) also exhibit green-grey clay infillings. There is, however, no indication of water flow in the flow measurements. The intersection exhibits 32 fractures, with a dip direction towards E and a moderate dip.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=LE=RS=N

Left-normal fault

Moderately dipping planar feature. Dip/dip direction 47/139. Fault vector orientation 15/186.

INTERSECTIONS OL_KR29_BJI_55676_56035

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

0 Very low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR29: 546.4 – 556.85 Rp0(Rp1), 556.85 – 566.20 Rp0-1 OL-KR29: 557.03 – 558.28 RiIII – RiIV

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_24.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Markku Paananen

APPENDIX 3 230

ID OL-BFZ025

DIMENSIONS X/Y/Z, m 121/170/97

DESCRIPTION OL_KR15_BFI_32308_33200

The intersection is composed of VMGT. The plagioclases are slightly altered to sericite/epidote. The intersection contains (330.55-331.05) a quartz vein with sphalerite and chalcopyrite. It also contains a few old and welded fractures with calcite infillings. The intersection contains 53 joints. The fractures dip direction and dip is scattered, with a concentration of fractures showing a dip direction towards SSW with a moderate dip. The fractures are partly parallel to the foliation. The rock in the intersection have an average of 5 fractures/m, with a more intensely fractured part (327.11-330.15) exhibiting 27 fractures. One fracture (327.55) in this part also contains gouge (dark grey clay infilling) but no water conductivity measurement has been carried out in this part of the borehole. The intersection exhibit 13 fractures with a slickenside surface, these have a striation direction from E to S, with a moderate plunge. Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=RE=RS=R

Right-normal fault

Moderately dipping planar feature. Dip/dip direction 32/198. Fault vector orientation 16/189.

INTERSECTIONS OL_KR15_BFI_32308_33200

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

0 Very low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_25.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Markku Paananen

APPENDIX 3 231

ID OL-BFZ026

DIMENSIONS X/Y/Z, m 100/60/79

DESCRIPTION OL_KR1_BFI_53860_53963

Contact between veined gneiss and pegmatite. Strong alteration can be seen as illitization and kaolinisation. Slickensided fractures, grain-filled fractures and open fractures occur in the short range between 539.12 - 539.25 m. Remarkable water-flow anomaly.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=NE=LS=N

Normal fault

Moderately dipping planar feature. Dip/dip direction 53/179. Fault vector orientation 42/190.

INTERSECTIONS OL_KR1_BFI_53860_53963

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics, VSP

1 Low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR1: 527.0 – 575.80 Rp0 OL-KR1: 538.61 – 539.24 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR01_6R

UPDATES - version history V 0 FILE Group_a_26.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Markku Paananen

APPENDIX 3 232

ID OL-BFZ027

DIMENSIONS X/Y/Z, m 203/324/196

DESCRIPTION OL_KR13_BFI_44550_46800

The intersection is mainly composed of VMGT and some sections of GRPG and MGN. The intersection contains 133 fractures of which 45 are slickensides. The VMGT is usually more densely fractured than the other rock types. Old and welded fractures are rare except for the GRPG where paleoshearzones and healed fractures with calcite infillings occur. The fractures in the intersection occur parallel to the foliation (NNE-SSW trend with moderate dips towards SSE). The slickenside surfaces have lineations in random directions but most plunge towards south. At 456-467 m there is signs of water conductivity in many fractures (greyish clay infillings).

OL_KR19_BJI_29561_29755

The intersection is composed of VMGT. The intersection contains 19 joints. The fractures dip directions are towards SE with moderate dip. The rock in the intersection is evenly fractured (ca. 9 fractures/m). At 296.14-297.09 the fractures show signs of water conductivity (kaoline infillings). Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=NE=LS=N

Left-normal fault

Moderately dipping planar feature. Dip/dip direction 31/180. Mean fault vector orientation 21/176.

INTERSECTIONS OL_KR13_BFI_44550_46800 OL_KR19_BJI_29561_29755

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersections, kinematics, VSP

1 Low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR13: 445.21 – 451.69 Rp0, 451.69 – 455.69 Rp0-1, 455.69 – 463.26 Rp0, 463.26 – 463.85 Rp0-1, 463.85 – 490.90 Rp0 OL-KR13: 454.34 – 454.97 RiIII, 457.33 – 459.23 RiIII

OL-KR19: 277.17 – 298.83 Rp0 OL-KR19: 295.61 – 297.34 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR13_10R KR19_8R

UPDATES - version history V 0

APPENDIX 3 233

FILE Group_a_27.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Markku Paananen

APPENDIX 3 234

ID OL-BFZ028

DIMENSIONS X/Y/Z, m 42/401/300

DESCRIPTION OL_KR13_BFI_36275_37446

The intersection is mainly composed of clearly foliated GGN and one section of quartz (372.12-373.30m). The intersection is relatively unfractured but contains signs of paleoshearing with old welded fractures with greyish matrix and calcite infillings. The intersection contains 51 joints, app. 4 fractures per metre. The fractures have a random direction with steep dip. The intersection exhibits 11 slickenside surfaces, which are randomly orientated (moderate dip). At 363.23-363.70 m the drill core is crushed and shows signs of water conductivity.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=L, R E=NS=L, R

Right-reverse fault

Steeply dipping planar feature. Dip/dip direction 82/269. Mean fault vector orientation 187/11.

INTERSECTIONS OL_KR13_BFI_36275_37446

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics, VSP

3 High (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR13: 362.53 – 373.41 Rp1, 373.41 – 391.41 Rp0 OL-KR13: 363.96 – 363.89 RiIV

COMPARISON TO BEDROCK MODEL 2003/1

KR13_8R

UPDATES - version history V 0 FILE Group_a_28.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Markku Paananen

APPENDIX 3 235

ID OL-BFZ029

DIMENSIONS X/Y/Z, m 178/200/92

DESCRIPTION OL_KR20_BFI_44963_45264

The intersection is mainly composed of VMGT with short sections of GRPG (464.20-464.60 and 467.15-468.10). The intersection contains 49 joints. The fractures dip direction and dip are scattered, with a concentration of fractures showing a dip direction towards SE and a moderate dip. Some of the fractures also have a foliation parallel direction. The intersection contains two fractures with slickenside surface. One of these fractures is shattered and another has SE trend with steep plunge. The VMGT in the intersection is evenly fractured, the GRPG section does not contain any fractures. The fractures at 466.35-466.37, 469.04, 469.17-469.19 show signs of water conductivity.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=L, R E=LS=R

Right-normal or left-normal fault

Steeply dipping planar feature. Dip/dip direction 28/81. Mean fault vector orientation 6/175.

INTERSECTIONS OL_KR20_BFI_44963_45264

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

1 Low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR20: 443.80 – 463.20 Rp0

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_29.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Markku Paananen

APPENDIX 3 236

ID OL-BFZ030

DIMENSIONS X/Y/Z, m 97/150/113

DESCRIPTION OL_KR33_BFI_27591_28043

The intersection composed of VMGT and DTX containing 55 fractures, some slickensides. Fracture density is varying inside the intersection and also technical breaking occurs in two 10-15 cm sections. Core loss in two depths (15 cm and 20 cm). Carbonate, kaolinite and illite infillings. Faults in two different directions. Clear pressure shadow carbonates in one fault in drillhole direction. Some old welded fractures. Not clear main directions of fracturing. High content of blueish pinitized cordierite with grain size of 1-10 mm. In appearances of K-feldspar grains also indicators of ductile shear.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=LE=LS=L

Fault

Moderately dipping planar feature. Dip/dip direction 51/117. Mean fault vector orientation 35/169.

INTERSECTIONS OL_KR33_BFI_27591_28043

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

1 Low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR33: 275 – 275.9 Rp1, 275.9 – 276.3 Rp2-3, 276.3 – 279.3 Rp1-2, 279.3 – 286.6 Rp1 (Rp2)

OL-KR33: 275.91 – 276.22 RiV, 276.22 – 280.42 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_30.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Markku Paananen

APPENDIX 3 237

ID OL-BFZ031

DIMENSIONS X/Y/Z, m 97/150/113

DESCRIPTION OL_KR33_BFI_28678_28815

MGN intersection with 27 fractures and also breaks caused by drilling. Couple of fractures slickensides with strong striation. Fractures in different directions but usually dipping to SE like foliation (121/66), more discordance in GRPG section. Kinematic vector around 180/30. Slight alteration, kaolinite.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=LE=LS=R

Left-normal fault

Steeply dipping planar feature. Dip/dip direction 53/107. Mean fault vector orientation 38/180.

INTERSECTIONS OL_KR33_BFI_28678_28815

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

1 Low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR33: 286.6 – 288.25: Rp1-2 OL-KR33: 286.63 – 288.13 RiIV

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_31.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Markku Paananen

APPENDIX 3 238

ID OL-BFZ032

DIMENSIONS X/Y/Z, m 605/479/165

DESCRIPTION OL_KR20_BFI_41059_42445

The intersection is composed of VMGT with a section of GRPG at between 414.20 and 416.40. The rock contains old and welded fractures with calcite infillings. The intersection contains 112 joints. The fractures dip direction is scattered, with a concentration of fractures showing a dip direction towards SE with a moderate dip. The intersection exhibit 34 fractures with a slickenside surface having a striation direction trend from NE to SW, with a moderate plunge. The fractures are mainly parallel to the foliation. The rock in the intersection has an average of 5 fractures/m, with a more intensely fractured part (416.45-417.71) exhibiting 21 fractures. One fracture (417.57) in this part also contains gouge (dark grey clay infilling). Water conductive fractures with kaoline infilling occur at between 420.13 and 420.51. Mechanical fracturing has occurred during the drilling.

OL_KR33_BFI_27591_28043

The intersection composed of VMGT and DTX containing 55 fractures, some slickensides. Fracture density is varying inside the intersection and also technical breaking occurs in two 10-15 cm sections. Core loss in two depths (15 cm and 20 cm). Carbonate, kaolinite and illite infillings. Faults in two different directions. Clear pressure shadow carbonates in one fault in drillhole direction. Some old welded fractures. Not clear main directions of fracturing. High content of blueish pinitized cordierite with grain size of 1-10 mm. In appearances of K-feldspar grains also indicators of ductile shear.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=RE=R,LS=L

Fault

Gently dipping planar feature. Dip/dip direction 19/155. Mean fault vector orientation 25/172 or 5/002.

INTERSECTIONS OL_KR20_BFI_41059_42445 OL_KR33_BFI_27591_28043 OL-KR5 300.23 – 303.11, single fault plane at OL-KR5 300.23

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersections, kinematics

2 Moderate (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

APPENDIX 3 239

IMPLICATIONS TO CONSTRUCTION

OL-KR5: 283.0 – 404.50 Rp0

OL-KR20: 403.5 – 411.5 Rp0, 411.5 – 417.1 Rp0(1), 417.1 – 417.56 Rp1, 417.56 – 417.60 Rp2, 417.60 – 420.13 Rp1, 420.13 – 420.63 Rp2(1), 420.63, 427.5 Rp1

OL-KR20: 416.32 – 418.40 RiIII, 419.27 – 420.13 RiIII, 420.13 – 420.63 RiIV, 423.40 – 423.89 RiIII

OL-KR33: 275 – 275.9 Rp1, 275.9 – 276.3 Rp2-3, 276.3 – 279.3 Rp1-2, 279.3 – 286.6 Rp1 (Rp2)

OL-KR33: 275.91 – 276.22 RiV, 276.22 – 280.42 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR20_5R

UPDATES - version history V 0 FILE Group_a_32.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Markku Paananen

APPENDIX 3 240

ID OL-BFZ033

DIMENSIONS X/Y/Z, m 170/348/143

DESCRIPTION OL_KR2_BFI_47100_47235

Mica-rich veined migmatite displaying ductile shear. In places the sample is strongly illitized and powderised kaolinite can be detected. Fractures are parallel with foliation and often slickensided. Drilling has open some fractures. FDV's are quite parallel, 198º/37º and 200º/14º. No water-conductivity.

OL_KR14_BFI_44500_44908

The intersection is composed of VMGT and in the latter part of MAFGN and MGN. The intersection contains 28 joints. The fractures dip direction and dip is scattered, with a concentration of fractures showing a dip direction towards SE with a moderate dip. The rock in the intersection has an average of 7 fractures/m. The central part of the intersection contains two sections (446.40-446.83 & 447.68-448.13) of intensely fractured and partly crushed rock. The latter section exhibit slightly altered feldspars (white-green alteration) and it also show signs of water conductivity (grey clay infillings). The majority of the fractures (16) in the intersection exhibit a slickenside surface, with two different striation direction one towards NE and the other towards SE. The striations have a moderate plunge. Seven of these slickenside surfaces indicate a R, L, L movement. Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=RE=LS=L

Right-reverse fault

Moderately dipping planar feature. Dip/dip direction 40/65. Mean fault vector orientation 25/199 or 30/003.

INTERSECTIONS OL_KR2_BFI_47100_47235 OL_KR14_BFI_44500_44908

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersections, , kinematics , VSP

2 Moderate (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR2: 52.13 – 503.65: Rp0 (1) OL-KR2: 471.42 – 472.00 RiIII

OL-KR14: 415.22 – 447.83 Rp0, 447.83 – 448.07 Rp1, 448.07 – 470.03 Rp0 OL-KR14: 446.44 – 448.11 RiIII

APPENDIX 3 241

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_33.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Markku Paananen

APPENDIX 3 242

ID OL-BFZ034

DIMENSIONS X/Y/Z, m 166/289/29

DESCRIPTION OL_KR25_BFI_16459_17200

The rock in the intersection is mostly composed of DTX, with some small sections of VMGT and QTZGN in the beginning. The rock is irregular and no clear foliation can be observed. The fractures are randomly orientated with a nearly horizontal dip. The intersection contains 47 joints, with an average of 4-7 fractures/m. It also contains 10 fractures with slickenside surfaces. The lineation on the slickenside surface has a trend varying from NW to NE, with variable plunge. The slickenside surface mostly show a R,L,L movement. A few old and welded fractures with calcite are present. Three of the fractures have signs of water conductivity (171.23, 171.30 & 171.41). Some mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=RE=LS=L

Right-reverse of right-normal fault

Subhorizontal planar feature. Dip/dip direction 7/113. Mean fault vector orientation 42/180 or 28/009.

INTERSECTIONS OL_KR25_BFI_16459_17200 Single fault planes at OL-KR28 179.13 and 183.12.

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersections, kinematics

2 Moderate (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR25: 130.30 – 171.15 Rp0-1, 171.15 – 178.50 Rp0-(Rp1) OL-KR28: 178.50 – 188.00 Rp0-(Rp1)

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_34.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Markku Paananen

APPENDIX 3 243

ID OL-BFZ035

DIMENSIONS X/Y/Z, m 50/1.4/50

DESCRIPTION OL_KR31_BJI_4070_4400

The intersection is composed of DTX. The intersection contains 44 fractures and a few old, welded, calcite and pyrite bearing fractures. The fractures are randomly orientated with moderate dip. The central part of the intersection (41.00-42.10) is badly crushed. In this section there is also 15 cm core loss. These grey clay bearing fractures have acted as a water channel according to the water conducting measurements. Some mechanical fracturing has occurred during the drillings

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A

U=NE=RS=N

Normal fault

Vertical planar feature. Dip/dip direction 89/165. Fault vector orientation 33/179.

INTERSECTIONS OL_KR31_BJI_4070_4400

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersection, kinematics

0 Very low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR31: 40.10 – 48.80 Rp1-2 OL-KR31: 40.80 – 43.20 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE Group_a_35.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Markku Paananen

APPENDIX 3 244

ID OL-BFZ036

DIMENSIONS X/Y/Z, m 170/348/143

DESCRIPTION OL_KR14_BFI_46985_47623

The rock in the intersection is mainly composed of VMGT and some sections of massive GRPG. The intersection contains 26 joints. The fractures are showing a dip direction towards ENE with a moderate dip. The rock in the intersection has an average of ca. 4 fractures/m. The intersection exhibit 8 fractures with a slickenside surface, these have a striation direction towards NE, with a moderate plunge. Three of these slickenside surfaces indicate a L, R, R movement. No signs of water conductivity.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group B

U=LE=RS=R

Left-normal fault

Moderately dipping planar feature. Dip/dip direction 40/118. Mean fault vector orientation 12/030.

INTERSECTIONS OL_KR14_BFI_46985_47623

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics, VSP

1 Low (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR14: 448.07 – 470.03 Rp0, 470.03 – 471.39 Rp0(Rp1), 471.39 – 514.10 Rp0

COMPARISON TO BEDROCK MODEL 2003/1

-

UPDATES - version history V 0 FILE Group_b_34.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Markku Paananen

APPENDIX 3 245

ID OL-BFZ037

DIMENSIONS 849 m in E-W-direction 262 m in N-S-direction

DESCRIPTION OL_KR5_BFI_40580_40962

Densely-fractured intersection in veined gneiss. Part of the fractures are parallel to foliation and part of them are cross-cutting foliation and the core in low angle. There is an older small-scale breakage, which is welded. The intersection of these two fracture orientations has obviously gathered fluids, because it seems to be remarkably altered compared to its surroundings, for example, strong pervasive kaolinization can be noticed. Drilling has an effect on splitting the core sample. TV image shows this section to be very modestly broken.

OL_KR19_BFI_48461_48892

The intersection is composed of GRPG and VMGT. The intersection contains a few old, welded fractures with calcite infillings. Some of them have reactivated later. The intersection contains 24 fractures (randomly orientated). 14 fractures in the intersection exhibit a slickenside surface, with the random striation direction. The rock in the intersection is evenly fractured (about 3 fractures/m). Almost half of the fractures are water conductive (kaoline infilling). Mechanical fracturing has occurred during the drilling.

OL_KR33_BFI_27591_28043

The intersection composed of VMGT and DTX containing 55 fractures, some slickensides. Fracture density is varying inside the intersection and also technical breaking occurs in two 10-15 cm sections. Core loss in two depths (15 cm and 20 cm). Carbonate, kaolinite and illite infillings. Faults in two different directions. Clear pressure shadow carbonates in one fault in drill hole direction. Some old welded fractures. Not clear main directions of fracturing. High content of blueish pinitized cordierite with grain size of 1-10 mm. In appearances of K-feldspar grains also indicators of ductile shear.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=LE=LS=L

Left-normal fault

Average dip/dip direction in KR19 095/21 and in KR33 45/098. Mean fault vector orientation 16/209 and 14/039.

INTERSECTIONS OL_KR5_BFI_40580_40962 OL_KR19_BFI_48461_48892 OL_KR33_BFI_27591_28043

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

2 Moderate (1=low, 2=moderate, 3=high)

APPENDIX 3 246

HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR33 275.91-276.22 m RiV, 276.22-280.42 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_b_1.dtm

COMPILATION DATE AND COMPILED BY

13.12.2005 Seppo Paulamäki

APPENDIX 3 247

ID OL-BFZ038

DIMENSIONS 598 m in E-W-direction 265 m in N-S-direction

DESCRIPTION OL_KR20_BFI_41059_42445

The intersection is composed of VMGT with a section of GRPG at between 414.20 and 416.40. The rock contains old and welded fractures with calcite infillings. The intersection contains 112 joints. The fractures dip direction is scattered, with a concentration of fractures showing a dip direction towards SE with a moderate dip. The intersection exhibit 34 fractures with a slickensided surface having a striation direction trend from NE to SW, with a moderate plunge. The fractures are mainly parallel to the foliation. The rock in the intersection has an average of 5 fractures/m, with a more intensely fractured part (416.45-417.71) exhibiting 21 fractures. One fracture (417.57) in this part also contains gouge (dark grey clay infilling). Water conductive fractures with kaolinite infilling occur at between 420.13 and 420.51. Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=LE=RS=R

Left-normal fault

Average dip/dip direction 28/174. Mean fault vector orientations 14/039 and 12/208.

INTERSECTIONS OL_KR20_BFI_41059_42445

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

2 Moderate (1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

416.32-418.40 m RiIII 419.27-420.13 m RiIII 423.40-423.89 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR20_5R (RH9)

UPDATES - version history V 0 FILE group_b_4.dtm

COMPILATION DATE AND COMPILED BY

13.12.2005 Seppo Paulamäki

APPENDIX 3 248

ID OL-BFZ039

DIMENSIONS 536 m in NE-SW-direction 362 m in NW-SE-direction

DESCRIPTION OL_KR29_BFI_53300_54855

The intersection is composed of VMGT and DTX, with some short sections of GRPG. The feldspars are often altered to illite. The rock in the intersection also contains plenty of cordierite (1.5 cm) and some garnet grains (1.0 cm), which are metamorphosed. The intersection contains a few old and welded fractures with calcite and pyrite infillings, especially in the GRPG. Several of the fractures contain kaolinite and illite infillings. Accordingly, a majority of the fractures show signs of water conductivity and some of them also exhibit green-grey clay infillings. There is, however, no indication of water flow in the flow measurements. The intersection exhibits 61 fractures, with a dip direction towards SE and a moderate dip. The rock is more fractured at the following section 543.80-547.12 (37 joints). The intersection exhibit 29 fractures with a slickenside surface, which have a striation direction varying from SE to SW, with a moderate plunge. Some mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=L(R) E=R(L)S=L

Right-/left-reverse? fault

Average dip/dip direction 40/130. Mean fault vector orientation 16/212.

INTERSECTIONS OL_KR29_BFI_53300_54855 Single fault plane in OL-KR7 at 473.92 m

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

2 Moderate (1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

The borehole did not exist in 2003.

UPDATES - version history V 0 FILE group_b_5.dtm

COMPILATION DATE AND COMPILED BY

13.12.2005 Seppo Paulamäki

APPENDIX 3 249

ID OL-BFZ040

DIMENSIONS 363 m in NE-SW-direction 295 m in NW-SE-direction

DESCRIPTION OL_KR3_BJI_4630_4880

Mica gneiss shows slightly elevated fracturing. In fact, the intersection shows 2 - 3 short (20 - 30 cm) sets of parallel fractures. Some of fractures are slickensides.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=RE=LS=L

Right-normal fault

Average dip/dip direction 37/155. Mean fault vector orientation 14/225.

INTERSECTIONS OL_KR3_BJI_4630_4880

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics, charge potential

2 (1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

RH26

UPDATES - version history V 0 FILE group_b_6.dtm

COMPILATION DATE AND COMPILED BY

13.12.2005 Seppo Paulamäki

APPENDIX 3 250

ID OL-BFZ041

DIMENSIONS 300 m in NE-SW-direction 300 m in NW-SE-direction

DESCRIPTION OL_KR13_BFI_16378_17647

The intersection is composed of DTX. A few old, "welded" fractures with calcite infilling occur. Some of the welded fractures have reactivated later. The dip directions of the fractures are randomly orientated. Intersection contains several slickensides, which have trends of NW-SE and NE-SW with almost vertical dip. The fractures have no signs of water conductivity.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=RE=RS=L/R/N?

Right-normal fault

Average dip/dip direction 41/153. Mean fault vector orientation 07/211.

INTERSECTIONS OL_KR13_BFI_16378_17647

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics

2 (1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_b_7.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Seppo Paulamäki

APPENDIX 3 251

ID OL-BFZ042

DIMENSIONS 375 m in NE-SW-direction 276 m in NW-SE-direction

DESCRIPTION OL_KR13_BFI_44550_46800

The intersection is mainly composed of VGN, and some sections of PGR and MGN. The intersection contains 133 fractures of which 45 are slickensides. The VMGT is usually more densely fractured than the other rock types. Old and welded fractures are rare except in the PGR where palaeoshearzones and healed fractures with calcite infillings occur. The fractures in the intersection are parallel to the foliation (NNE-SSW trend with moderate dips towards SSE). The slickenside surfaces have lineations in random directions but most plunge towards south. At 456-467 m there are signs of water conductivity in many fractures (greyish clay infillings).

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=LE=RS=R

Left-normal fault

Average dip/dip direction 35/129. Mean fault vector orientation 20/204.

INTERSECTIONS OL_KR13_BFI_44550_46800

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics

1 (1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

451.04-451.84 m RiIII 454.34-454.97 m RiIII 457.33-459.23 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR13_10R

UPDATES - version history V 0 FILE group_b_8.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Seppo Paulamäki

APPENDIX 3 252

ID OL-BFZ043

DIMENSIONS 250 m in N-S-direction 250 m in E-W-direction

DESCRIPTION OL_KR10_DSI_26900_27540

Strongly-foliated rock with a very fine-grained almost glassy groundmass. In the section, short brittle fault set exists.

OL_KR10_BFI_27147_27159

A set of parallel slickensides, which cross-cuts ductile foliation. Presumably slickensides are quite steeply-dipping. On fracture surfaces a slight pyrite-coatings.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=LE=RS=R

Left-normal fault

Average dip/dip direction 78/115. Mean fault vector orientation 21/028.

INTERSECTIONS OL_KR10_BFI_27147_27159

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics

2 (1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

271.41-271.82 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_b_9.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Seppo Paulamäki

APPENDIX 3 253

ID OL-BFZ044

DIMENSIONS 150 m in NE-SW-direction 150 m in NW-SE-direction

DESCRIPTION OL_KR19_BFI_9945_10309

The intersection is composed of VGN. The rock contains a few old, welded, calcite bearing fractures, witch have been reactivated later. The intersection consists about 3-4 fractures/ 1 metre (19 fractures altogether). The fractures dip direction and dip is scattered. Four slickensided surfaces are also observed (SW orientated). Some of them seem to be created into palaeofractures, which may have been reactivated. In section of 102.28-102.52 there are water conductive fractures (three fractures). In some places feldspars are sericitized.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=LE=RS=R

Left-normal fault

Average dip/dip direction 37/146. Mean fault vector orientation 03/224.

INTERSECTIONS OL_KR19_BFI_9945_10309

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics

1 (1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

271.41-271.82 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_b_10.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Seppo Paulamäki

APPENDIX 3 254

ID OL-BFZ045

DIMENSIONS 548 m in NE-SW-direction 100 m in NW-SE-direction

DESCRIPTION OL_KR13_BFI_40941_42389

The intersection is mainly composed of strongly foliated (sheared) VGN, at 420.85-421.67 there is a section of PGR. The intersection is unevenly fractured and at 409.79-410.50 m the rock is intensely fractured (16/m) and 10 cm core loss has occurred, at this place the rock is water conductive. The intersection contains 66 fractures, of which 15 are slickensides. Only a few old and welded fractures with calcite infillings are present. The fractures are parallel to the foliation (NE-SW trend with moderate dips towards SE). Most slickensided surfaces have nearly horizontal lineations in random directions. At 363.23-363.70 m the drill core is crushed and shows signs of water conductivity.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=L/RE=R/LS=R/L

Left-/right-normal fault

Average dip/dip direction 37/140. Mean fault vector orientation 26/033.

INTERSECTIONS OL_KR13_BFI_40941_42389

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics, VSP

2 (1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

409.42-410.91 m RiIII 410.15-410.53 m core loss 0.1 m

COMPARISON TO BEDROCK MODEL 2003/1

KR13_9R

UPDATES - version history V 0 FILE group_b_12.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Seppo Paulamäki

APPENDIX 3 255

ID OL-BFZ046

DIMENSIONS 200 m in NE-SW-direction 200 m in NW-SE-direction

DESCRIPTION OL_KR15_BFI_49350_49650

The intersection is composed of MGN. The rock exhibits only a few old, welded, calcite-bearing fractures. The fractures (13) dip towards SE with horizontal to steep dip. The fractures are parallel to the foliation. The majority of the fractures in the intersection contain slickensided surfaces (9) having a NE-SW trend. No water conductivity measurement has been carried out in this part of the borehole.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=L/R? E=R/L? S=R/L?

Left-normal/right-reverse? fault

Average dip/dip direction 83/130. Mean fault vector orientation 15/225.

INTERSECTIONS OL_KR15_BFI_49350_49650

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics

1 (1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_b_13.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Seppo Paulamäki

APPENDIX 3 256

ID OL-BFZ047

DIMENSIONS 333 m in NE-SW-direction 269 m in NW-SE-direction

DESCRIPTION OL_KR6_BFI_480_1395

Characteristic fracturing of surface part of the bedrock with random orientation. Clay- and grain-filled fractures, slickensides and weathering as well as porosity. Some coatings are rusty. Veined gneiss and pegmatite. In veined gneiss there is strong shearing in short zones. Moderately strong kaolinization and illitization.

OL_KR19B_BFI_4045_4505

The intersection is composed of VGN. The intersection contains old, welded fractures with calcite and mica (?) infillings. Some of these welded fractures have been reactivated later. The intersection contains 43 joints. The fractures dip directions are towards SE with moderate dip. The rock in the intersection is evenly fractured. 18 fractures in the intersection exhibit a slickensided surface, but most of them are shattered or drilling has made them rounded. Three slickensided surfaces have striation direction towards SE and SW with horizontal to moderate plunge. At 40.69-41.35, 42.97-43.41 and 44.80-44.85 the fractures show water conductivity (kaolinite infilling). Mechanical fracturing has occurred during the drilling. There is no WellCAD picture available from 43.27 to 45.05 (this part contains also 7 slickensided surfaces).

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=RE=LS=L

Right-normal fault

Average dip/dip direction 19/154. Mean fault vector orientation 17/226.

INTERSECTIONS OL_KR6_BFI_480_1395 OL_KR19B_BFI_4045_4505

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

44.59-46.23 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR19B_4H

UPDATES - version history V 0 FILE group_b_14.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Seppo Paulamäki

APPENDIX 3 257

ID OL-BFZ048

DIMENSIONS 250 m in NE-SW-direction 250 m in NW-SE-direction

DESCRIPTION OL_KR8_BFI_34848_35265

The intersection is composed of DTX. The intersection contains old and welded fractures where calcites are present. These old fractures have partly been reactivated later. The fractures have a random direction with horizontal to moderate dip. The intersection contains 29 joints. The rock is most fractured in section 348.60-349.15 (containing 12 fractures) and 351.12-351.26 (exhibiting 5 fractures). The former section contains water-conductive fractures. The intersection exhibits 8 slickensided surfaces but the striation orientation and the movement is totally random. No mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=RE=RS=L(R)

Right-reverse fault

Average dip/dip direction 42/155. Mean fault vector orientation 23/214.

INTERSECTIONS OL_KR8_BFI_34848_35265

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics

0 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_b_15.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Seppo Paulamäki

APPENDIX 3 258

ID OL-BFZ049

DIMENSIONS 200 m in N-S-direction 200 m in E-W-direction

DESCRIPTION OL_KR6_BFI_50596_50933

Densely-fractured intersection in veined gneiss. Random fracturing wit fractures parallel to and crosscutting foliation. An older small-scaled microfracturing and -breakage, which is welded. On slickensides graphite-coatings can be seen. One observation on direction vector, FDV = 40°/14°. Drilling-induced splitting of the core sample.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=no data E=no data S=no data

Average dip/dip direction 20/090. Mean fault vector orientation 14/040.

INTERSECTIONS OL_KR6_BFI_50596_50933

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics

0 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

506.88-508.85 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR06_12R

UPDATES - version history V 0 FILE group_b_16.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Seppo Paulamäki

APPENDIX 3 259

ID OL-BFZ050

DIMENSIONS 100 m in N-S-direction 100 m in E-W-direction

DESCRIPTION OL_KR16_BFI_11968_13469

DTX is the main rock type in the intersection, with some shorter sections of VGN, MGN and PGR. The feldspars are slightly altered to sericite. The intersection contains a few old and welded fractures with calcite infillings. It contains 52 fractures with an average of 3.5/m. The fractures dip direction and dip is very scattered, with a slight concentration of fractures, showing a dip direction towards SE with various dip. The water conductivity measurements show signs of water flowing at four places, but only two of these exhibit signs in the drill core. These three fractures (129.08, 133.74 &133.78) contain grey clay infilling. The intersection exhibit 17 fractures with a slickensided surface, six of these have a striation direction towards NE, with a nearly horizontal to moderate plunge. Several of the slickensided surfaces are in a shattered drill core, thus mechanical fracturing has occurred during the drilling.

OL_KR17_BFI_12350_13092

VGN is the main rock type in the intersection, with some DTX in the beginning. The feldspars are slightly altered to sericite. The intersection contains a few old and welded fractures with calcite and pyrite infillings. It exhibits 56 fractures, with a dip direction towards SE and a moderate dip. The rock is intensely fractured at 124.30-124.70 (12 joints) and 128.90-129.45 (13 joints). These sections show signs of water flowing, containing kaolinite and grey-green clay infilling. The latter section also contains 20 cm core loss. The intersection exhibit 8 fractures with a slickensided surface, six of these have a striation direction varying from NE to SE, with a moderate plunge. Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=LE=RS=R

Left-normal fault

Average dip/dip direction 50/112. Mean fault vector orientation 09/033.

INTERSECTIONS OL_KR16_BFI_11968_13469 OL_KR17_BFI_12350_13092

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics

2 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

Water flowing in KR16 at 129.08, 133.74 and 133.78 m, the fractures containing grey clay infilling. Signs of water flowing in KR17, containing kaolinite and grey-green clay infilling.

IMPLICATIONS TO CONSTRUCTION

KR17 124.33-125.14 m RiIII KR17 128.27-129.81 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

R78 (KR17_3R)

APPENDIX 3 260

UPDATES - version history V 0 FILE group_b_17.dtm

COMPILATION DATE AND COMPILED BY

14.12.2005 Seppo Paulamäki

APPENDIX 3 261

ID OL-BFZ051

DIMENSIONS 415 m in N-S-direction 129 m in E-W-direction

DESCRIPTION OL_KR4_BFI_8154_8239

Tectonic breccia or protocataclastite, in which the average diameter of the fragments exceeds 0.5 cm and the proportion of the fault rock is 10 – 15%. Products of pervasive alteration: sulphides, kaolinite and illite. Late stage fractures are often coplanar with earlier mylonitic foliation.

OL_KR8_BFI_13822_13994

Fractured intersection and sample is splitted into pieces, which have a diameter of just a few centimetres. Many slickensided fractures with calcite and illite-coatings. Majority of the fractures concentrate on the contact zone of mica gneiss and coarse-grained granite at depth of 138.60 m, Fractures are almost in the direction of the core sample. Fracturing is at least partly drilling-induced phenomena, although in and just outside the intersection there are four measurements of significant water-conductivities.

OL-KR24: ca. 16 fractures at 94-95 m

Onkalo: 958-964 m

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=LE=RS=R

Sinistral strike-slip fault

Average dip/dip direction 08/105. Mean fault vector orientation 05/030.

INTERSECTIONS OL_KR4_BFI_8154_8239 OL_KR8_BFI_13822_13994 OL-KR24 ca. 95 m Onkalo ca. 960 m

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

2 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

OL_KR8_BFI_13822_13994: in and just outside the intersection there are four measurements of significant water-conductivities.

IMPLICATIONS TO CONSTRUCTION

OL-KR4 81.41-82.61 m RiIII, Rp2 OL-KR8 138.22-139.94 m RiIII OL-KR24 94.02-94.35 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR04_2RH (RH19A) KR08_8R (R24B)

UPDATES - version history V 0 FILE group_b_18.dtm

APPENDIX 3 262

COMPILATION DATE AND COMPILED BY

14.12.2005 Seppo Paulamäki

APPENDIX 3 263

ID OL-BFZ052

DIMENSIONS 255 m in N-S-direction 353 m in E-W-direction

DESCRIPTION OL_KR15_BFI_44962_45600

The intersection is composed of MGN. The rock exhibits a few old, welded, calcite-bearing fractures. The fractures are randomly orientated with horizontal to moderate dip. The intersection contains 53 joints, with a more fractured part (449.85-451.95) exhibiting 36 fractures. The slickensides (only 5) have striation trend of NE-SW with moderate plunge. Some fractures (at least at 451.25 m, containing dark, unidentified clay mineral) might act as a water channels, but no water conductive measurements has been carried out in this part of the borehole. Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=LE=RS=R

Left-normal fault

Average dip/dip direction 44/170. Mean fault vector orientation 44/227.

INTERSECTIONS OL_KR15_BFI_44962_45600

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics, VSP

2 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

KR15_4R

UPDATES - version history V 0 FILE group_b_19.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Seppo Paulamäki

APPENDIX 3 264

ID OL-BFZ053

DIMENSIONS 555 m in NE-SW-direction 550 m in SE-NW-direction

DESCRIPTION OL_KR27_BFI_30256_32607

The intersection contains roughly 1 slickensided surface per meter and has not a particularly high fracture density. The section and its surrounding rocks contain some healed fractures with calcite infillings. Some old and healed fractures may have been reactivated. The slickensided surfaces often occur parallel to the foliation (NW-SE) and normally have lineations with a NE-SW trend. The slickensides often contain some carbonates. The rock type is mainly DTX but in the centre of this intersection there is a section of PGR. The rock is cohesive but some small parts show signs of semi-brittle deformation with angular feldspar crystals (5 mm).

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=R(L) E=R(L)S=R(L)

Right-/left-normal? fault

Average dip/dip direction 84/133. Mean fault vector orientation 14/208.

INTERSECTIONS OL_KR27_BFI_30256_32607

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics, charge potential?

2 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

The borehole did not exist in 2003.

UPDATES - version history V 0 FILE group_b_20.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Seppo Paulamäki

APPENDIX 3 265

ID OL-BFZ054

DIMENSIONS 214 m in NE-SW-direction 414 m in SE-NW-direction

DESCRIPTION OL_KR27_SFI_33385_34842

The intersection contains DTX that is strongly sheared and contains a lot of paleofractures of which some are reactivated and occur as joints and slickensided surfaces. The rock contains a lot of angular, altered feldspar crystals, which show a cataclastic structure. The diameter of the feldspars is usually a couple of millimetres but crystal up to 4 cm in length are present. On both sides of this intersection there is a 25 m wide zone where the rocks occasionally show some weak signs of semi-brittle deformation. The intersection contains a 3,25 m wide section, which is strongly fractured and faulted (see below).

OL_KR27_BFI_33519_33994

This brittle fault intersection contains DTX and lies inside the semi-brittle fault intersection BFI_OL_KR27_33385-34842 (above). Fractures and slickensides usually have a NW-SE direction but lineations occur in random directions. The fractures often have some greyish clay infilling, and some contain carbonates or graphite. Some of the fractures (with clay infillings) are water conductive.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=RE=LS=L

Right-reverse fault

Average dip/dip direction 56/121. Mean fault vector orientation 17/204.

INTERSECTIONS OL_KR27_SFI_33385_34842 OL_KR27_BFI_33519_33994

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics, charge potential?

2 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

Some of the fractures (with clay infillings) are water conductive.

IMPLICATIONS TO CONSTRUCTION

338.21-339.77 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

The borehole did not exist in 2003.

UPDATES - version history V 0 FILE group_b_21.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Seppo Paulamäki

APPENDIX 3 266

ID OL-BFZ055

DIMENSIONS 377 m in NE-SW-direction 650 m in SE-NW-direction

DESCRIPTION OL_KR27_SFI_42600_43990

The intersection contains mostly PGR that has a texture, which resembles DTX, some small sections of VGN are also present. The rock is sheared and deformed in a semi-brittle fashion and it is still cohesive and fairly unaltered. The rock is in this section cataclastic and contains large amounts of angular (broken) crystals of feldspar and quartz, the crystals vary in size from a couple of millimetres to 5 cm (mostly 0.5 cm). The feldspar and quartz grains lie scattered in a dark greyish matrix, which probably has a MGN composition. The rock is extremely abundant in old healed fractures that give the rock an almost brecciated look at places. The healed fractures contain mostly pyrite, calcite and a dark greyish matrix (fault gauge?). Inside this intersection lies the younger and brittle intersection BFI_OL_KR27_42709-43342 (see below).

OL_KR27_BFI_42709_43342

This intersection contains coarse-grained deformed PGR and lies inside the semi-brittle intersection SFI_OL_KR27_42600-43990 (see before). The section contains 55 joints of which 12 have slickensided surfaces. Most fractures have a NE-SW trend, the slickensides have lineations showing movement in a N-S direction. The fractures usually have infillings of calcite and pyrite. The section is within the older deformation that may have been reactivated during the formation of this intersection. Some technical reopening of the old and healed fractures may have occurred during the drillings.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=LE=LS=R

Left-normal fault

Average dip/dip direction 72/130. Mean fault vector orientation 13/039.

INTERSECTIONS OL_KR27_SFI_42600_43990 OL_KR27_BFI_42709_43342

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics, charge potential?

2 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION

426.50-426.67 m RiV 426.67-427.83 m RiIII 433.38-434.14 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

The borehole did not exist in 2003.

UPDATES - version history V 0

APPENDIX 3 267

FILE group_b_22.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Seppo Paulamäki

APPENDIX 3 268

ID OL-BFZ056

DIMENSIONS 352 m in NE-SW-direction 350 m in SE-NW-direction

DESCRIPTION OL_KR27_SFI_27485_28824

The intersection contains mostly VGN and a short section of PGR (283.70-284.63). The intersection is strongly altered and shows a palaeoshearing, which was reactivated. The intersection also contains old, randomly oriented "welded" fractures; fractures, which are welded by calcite and some greenish mineral. The rock exhibits angular, altered feldspar crystals, which show a cataclastic structure. The diameter of feldspars is usually 2 mm. Also some larger crystals up to 4 cm in length were observed. Small shearing and faulting along the welded fractures are observed. The intersection includes a narrower section, which is strongly fractured (see below).

OL_KR27_BFI_27751_28440

Approx. 50 % of the fractures has a slickensided surface. These slickensides have a stretching lineation with a NE-SW trend and contain graphite. Some of the slickensided fractures are parallel to the foliation, but several different orientations were observed. The most fractured section contains 7 fractures/20 cm, average being 5-8 fractures/m. The most fractured section at 283.00-283.50 m, shows some water conducting fractures but otherwise the zone is dry. Drilling has crushed some of the core sample.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=L(R) E=RS=R

Right-reverse/left-normal? fault

Average dip/dip direction 45/148. Mean fault vector orientation 28/216.

INTERSECTIONS OL_KR27_SFI_27485_28824 OL_KR27_BFI_27751_28440

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics, charge potential?

2 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

Some water conducting fractures at 283.00-283.50 m.

IMPLICATIONS TO CONSTRUCTION

277.87-279.02 m RiIII 280.77-284.88 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

The borehole did not exist in 2003.

UPDATES - version history V 0 FILE group_b_23.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Seppo Paulamäki

APPENDIX 3 269

ID OL-BFZ057

DIMENSIONS 200 m in N-S-direction 200 m in E-W-direction

DESCRIPTION OL_KR27_BFI_29270_29612

A short fault intersection. The central part (293.10-295.20) of the intersection is slightly sheared and deformed (semi-brittle). The central part contains some angular feldspar crystals and old fractures with pyrite infillings. The crystals are 3-7 mm in diameter. The intersection contains 23 slickensided surfaces, usually planar and parallel to the foliation. The slickensides have a lineation with a NE-SW trend and often contain some carbonate, pyrite and clay minerals. Many fractures show signs of water conductivity.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=R(L) E=RS=R

Right-normal fault

Average dip/dip direction 25/170. Mean fault vector orientation 32/210.

INTERSECTIONS OL_KR27_BFI_29270_29612

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics, charge potential?

2 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

Many fractures show signs of water conductivity.

IMPLICATIONS TO CONSTRUCTION

292.79-294.11 m RiIII 295.50-296.19 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

The borehole did not exist in 2003.

UPDATES - version history V 0 FILE group_b_24.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Seppo Paulamäki

APPENDIX 3 270

ID OL-BFZ058

DIMENSIONS 240 m in NE-SW-direction 256 m in SE-NW-direction

DESCRIPTION OL_KR22_BFI_7790_10300

The intersection contains DTX and a couple of short sections of MGN and VGN. The intersection contains 179 fractures and has an average density of 7 fractures / m. Of these fractures at least 16 are slickensides. There is only one set of joints with dip dip directions of about 20/115 (often occur parallel to the foliation.). The slickensides have lineations indicating horizontal movement in a NE-SE direction. Some old and healed fractures with calcite infillings occur. Signs of water conductivity have been observed in some fractures throughout this intersection. Mechanical fracturing has probably been sparse in this section.

OL_KR31_BFI_8600_9000

The rock in the intersection is mainly composed of PGR with some short sections of DTX. The intersection contains 19 joints and old, welded, calcite bearing fractures. The fractures are showing a NE-SW dip direction trend with a moderate dip. The rock in the intersection has an average of ca. 5 fractures/m. The intersection exhibit 5 fractures with a slickensided surface, these have a striation direction towards NE, with a moderate-horizontal plunge. No signs of water conductivity.

OL_KR31_BJI_10250_10800

The intersection is composed of DTX with short section of QGN. The QGN is slightly altered (skarn). The intersection contains a lot of old and welded fractures where calcite and pyrite are present. These old fractures have partly been reactivated later. The fractures show an NE-SW trend, with various dips. The fractures seem to follow the foliation. The intersection contains 39 joints, with an average of 7 fractures/m. The rock is fractured throughout the intersection. Many of these fractures exhibit water conductivity signs. Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=R(L) E=R(L)S=R(L)

Right-reverse/left-normal? fault

Average dip/dip direction 40/120. Mean fault vector orientations 17/042 and 07/218.

INTERSECTIONS OL_KR22_BFI_7790_10300 OL_KR31_BFI_8600_9000 OL_KR31_BJI_10250_10800

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics

2 (0=very low, 1=low, 2=moderate, 3=high)

APPENDIX 3 271

HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION

OL-KR22 at 81.85-82.65 m RiIII OL-KR22 at 89.97-90.92 m RiIII OL-KR22 at 96.92-97.96 m RiIII OL-KR31 at 102.66-103.60 m RiIII OL-KR31 at 103.87-104.75 m RiIII OL-KR31 at 107.29-108.01 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR22_2R KR22_3RH (RH19B)

UPDATES - version history V 0 FILE group_b_25.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Seppo Paulamäki

APPENDIX 3 272

ID OL-BFZ059

DIMENSIONS 300 m in NE-SW-direction 300 m in SE-NW-direction

DESCRIPTION OL_KR22_BFI_13880_14605

This intersection contains mostly DTX. The intersection contains 61 joints and has an average density of 8 fractures/m. The dominating joint set has a dip/dip directions of about 30/130 but some other directions do occur. At least 8 fractures have slickensided surfaces. The slickensides have lineations in varying directions but most have a moderate plunge and are NE-SW trending. Some old and healed fractures with pyrite infillings are present. Many fractures have graphite infillings, no signs of water conductivity were observed.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=RE=LS=L

Right-reverse fault

Average dip/dip direction 47/140. Mean fault vector orientation 15/215.

INTERSECTIONS OL_KR22_BFI_13880_14605

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION

OL-KR22 at 138.87-140.83 m RiIII OL-KR22 at 144.57-145.62 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR22_4RH

UPDATES - version history V 0 FILE group_b_26.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Seppo Paulamäki

APPENDIX 3 273

ID OL-BFZ060

DIMENSIONS 356 m in NE-SW-direction 160 m in SE-NW-direction

DESCRIPTION OL_KR22_BFI_18845_20050

This intersection contains DTX with a slightly banded texture. The intersection contains 79 fractures and has an average joint density of 6-7 joints / m. At least 10 of these fractures have slickensided surfaces. Some old and healed joints with calcite infillings occur in the beginning of this intersection. The direction of the joints is a bit varying but one clear joint set parallel to the foliation is distinguished (dip/dip direction 20/150). The slickensides have nearly horizontal striations and most are NE-SW trending but two E-W trending also occur. Most fractures have calcite and pyrite infillings. No signs of water conductivity were observed. Some mechanical fracturing of the old and healed fractures may have occurred during the drillings.

OL_KR28_BFI_17021_17830

Mainly VGN with short sections of PGR and MGN. In VGN (from 170.21 to 173.50) there are about 7 fractures/ 1 metre. Two slickensided surfaces are also observed. They seem to be created into palaeo fractures which may have been reactivated. There are red feldspar crystals (rounded) in VGN. Old welded biotite, pyrite and calcite infillings are observed. In some places feldspars are sericitized. 172.65-172.70 crushed drill core. 173.50- 174.00 MGN with some old welded calcite bearing fractures. 174.00-174.12 several fractures in random directions. In depth of 174.12-174.90 VGN contains some slickensides (NE orientated). 174.90-175.85 PGR contains some fractures in random orientation and old welded calcite bearing fractures. 175.85-178.00 VGN contains only a few fractures in random orientation. In sections of 168.50-171.99 and 172.90-173.16 there are water conductive fractures.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=L/RE=L(R)S=L(R)

Left-/right-normal fault

Average dip/dip direction 34/130. Mean fault vector orientation 12/223.

INTERSECTIONS OL_KR22_BFI_18845_20050 OL_KR28_BFI_17021_17830

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics, charge potential survey

3 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

In OL-KR28 water conductive fractures in sections 168.50-171.99 m and 172.90-173.16 m.

APPENDIX 3 274

IMPLICATIONS TO CONSTRUCTION

OL-KR22 at 188.70-191.45 m RiIII OL-KR22 at 194.44-195.45 m RiIII OL-KR28 at 172.35-174.11 m RiIII OL-KR28 at 172.60-173.20 m RiIV OL-KR28 at 175.50-176.60 m RiIII OL-KR28 at 177.02-178.02 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR22_5R

UPDATES - version history V 0 FILE group_b_27.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Seppo Paulamäki

APPENDIX 3 275

ID OL-BFZ061

DIMENSIONS 150 m in N-S-direction 150 m in E-W-direction

DESCRIPTION OL_KR27_BFI_29270_29612

A short fault intersection. The central part (293.10-295.20) of the intersection is slightly sheared and deformed (semi-brittle). The central part contains some angular feldspar crystals and old fractures with pyrite infillings. The crystals are 3-7 mm in diameter. The intersection contains 23 slickensided surfaces, usually planar and parallel to the foliation. The slickensides have a lineation with a NE-SW trend and often contain some carbonate, pyrite and clay minerals. Many fractures show signs of water conductivity.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=R(L) E=RS=R

Right-/left-normal fault

Average dip/dip direction 59/127. Mean fault vector orientation 32/210.

INTERSECTIONS OL_KR27_BFI_29270_29612

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

Many fractures show signs of water conductivity.

IMPLICATIONS TO CONSTRUCTION

292.79-294.11 m RiIII 295.50-296.19 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

The borehole did not exist in 2003.

UPDATES - version history V 0 FILE group_b_28.dtm

COMPILATION DATE AND COMPILED BY

15.12.2005 Seppo Paulamäki

APPENDIX 3 276

ID OL-BFZ062

DIMENSIONS 100 m in N-S-direction 100 m in E-W-direction

DESCRIPTION OL_KR5_BFI_48178_48335

Short densely fractured intersection in veined gneiss. An old microfracturing and calcite-filled fractures of an earlier phase. A short graphite-bearing section can be identified. Pervasive kaolinitization and illitization are characteristic. Drilling has probably split the core also. No water-conductivity. The major part of the core is missing.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=no data E=no data S=no data

Strike-slip fault

Average dip/dip direction 35/142. Mean fault vector orientation 22/202.

INTERSECTIONS OL_KR5_BFI_48178_48335

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics

0 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

481.77-483.25 m RiIII (RiIV)

COMPARISON TO BEDROCK MODEL 2003/1

KR05_8R (RH21)

UPDATES - version history V 0 FILE group_b_29.dtm

COMPILATION DATE AND COMPILED BY

16.12.2005 Seppo Paulamäki

APPENDIX 3 277

ID OL-BFZ063

DIMENSIONS 150 m in N-S-direction 150 m in E-W-direction

DESCRIPTION OL_KR14_BFI_44500_44908

The intersection is composed of VGN and in the latter part of MFGN and MGN. The intersection contains 28 fractures. The dip directions and dips of the fractures are scattered, with a concentration of fractures showing a dip direction towards SE with a moderate dip. The rock in the intersection has an average of 7 fractures/m. The central part of the intersection contains two sections (446.40-446.83 m and 447.68-448.13 m) of intensely fractured and partly crushed rock. The latter section exhibit slightly altered feldspars (white-green alteration) and it also show signs of water conductivity (grey clay infillings). The majority of the fractures (16) in the intersection exhibit a slickensided surface, with two different striation directions one towards NE and the other towards SE. The striations have a moderate plunge. Seven of these slickensided surfaces indicate a R, L, L movement. Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=RE=LS=L

Right-reverse fault

Average dip/dip direction 66/266. Mean fault vector orientation 28/028.

INTERSECTIONS OL_KR14_BFI_44500_44908

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics

0 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

Signs of water conductivity (grey clay infillings) at 447.68-448.13 m.

IMPLICATIONS TO CONSTRUCTION

446.44-448.11 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_b_30.dtm

COMPILATION DATE AND COMPILED BY

16.12.2005 Seppo Paulamäki

APPENDIX 3 278

ID OL-BFZ064

DIMENSIONS 200 m in NE-SW-direction 200 m in SE-NW-direction

DESCRIPTION OL_KR2_BFI_60080_60477

Intersection shows partial shearing, old microfracturing and -breccia, which are welded in placed by strong silicification. Rock is mica-prevailing gneiss and pegmatite dykes. Illitization occurs both in gneiss and pegmatites. The old welded fracture system is quite vertical and in places opened by drilling. In younger phase there was a slip in direction of foliation aided by graphite-bearing layers and partly by illite, which can be seen on slickensides. The most broken core of the section joins the location of the old microbreccia, graphitic section and illitization at dept of 603.60 - 604.55 m.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=no data E=no data S=no data

Average dip/dip direction 40/158. Mean fault vector orientation 47/198.

INTERSECTIONS OL_KR2_BFI_60080_60477

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics, VSP?

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

Signs of water conductivity (grey clay infillings) at 447.68-448.13 m.

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

KR02_8RH (R21)

UPDATES - version history V 0 FILE group_b_31.dtm

COMPILATION DATE AND COMPILED BY

16.12.2005 Seppo Paulamäki

APPENDIX 3 279

ID OL-BFZ065

DIMENSIONS 150 m in N-S-direction 150 m in E-W-direction

DESCRIPTION OL_KR19_BFI_53327_53591

The intersection is composed of VGN with a short section of PGR (at 534.75-534.96 m). The intersection contains old, welded fractures with calcite infillings. The intersection contains 35 fractures. The fractures dip directions are towards E and SE with moderate dip. Most of the fractures follow the foliation. The rock in the intersection is evenly fractured. Four fractures in the intersection exhibit a slickensided surface, with the striation direction towards NE with moderate plunge. The fractures at 533.28-533.32 m, 533.38 m, and 533.91 m show water conductivity (kaolinite infilling). At 533.27-533.37 there is weathered and altered VGN. Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=RE=LS=L

Right-reverse fault

Average dip/dip direction 38/099. Mean fault vector orientation 25/040.

INTERSECTIONS OL_KR19_BFI_53327_53591

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

0 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

The fractures at 533.28-533.32 m, 533.38 m, and 533.91 m show water conductivity (kaolinite infilling).

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

KR19_12R

UPDATES - version history V 0 FILE group_b_32.dtm

COMPILATION DATE AND COMPILED BY

16.12.2005 Seppo Paulamäki

APPENDIX 3 280

ID OL-BFZ066

DIMENSIONS 100 m in N-S-direction 100 m in E-W-direction

DESCRIPTION A concentration of slickensided fractures in OL-KR4 at 41-57 m. The slickensided fractures within the section mostly belong to fault groups A and B. The fault zone is modelled on the basis of a cluster of faults of fault group B at 46.65-53.76 m, which have the same fault plane and the fault vector orientation.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=no data E=no data S=no data

Average dip/dip direction 49/181. Mean fault vector orientation 42/208.

INTERSECTIONS 6 single fault planes in Ol-KR4 at 46.85-53.76 m

BASIS FOR INTERPRETATION

CONFIDENCE

Kinematics

0 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_b_33.dtm

COMPILATION DATE AND COMPILED BY

16.12.2005 Seppo Paulamäki

APPENDIX 3 281

ID OL-BFZ067

DIMENSIONS 261 m in NE-SW-direction 250 m in SE-NW-direction

DESCRIPTION OL_KR12_BFI_7375_8020

Long intersection in mica-rich migmatite, mafic gneiss and quartz-feldspar -rich altered sections. A clean-cut fault zone, fractures are mainly slickensides with some calcite and sulphides on fracture planes and thin clayey coatings. Alteration includes at least illite and possible kaolinite. Slickensides are partly on foliation planes, partly crosscutting core sample and foliation in low angle. Some slickensides have graphite-fillings. Drilling has also effect on core splitting. 4 to 5 water-conductive fractures are observed with flow meter.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=no data E=no data S=no data

Average dip/dip direction 36/120. Mean fault vector orientation 22/102.

INTERSECTIONS OL_KR12_BFI_7375_8020 OL-TK4_P17_110_P17_200??

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

4 to 5 water-conductive fractures are observed with flow meter.

IMPLICATIONS TO CONSTRUCTION

OL-KR12 73.86-79.46 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR12_2R (RH26)

UPDATES - version history V 0 FILE group_c_1.dtm

COMPILATION DATE AND COMPILED BY

16.12.2005 Seppo Paulamäki

APPENDIX 3 282

ID OL-BFZ068

DIMENSIONS 150 m in NE-SW-direction 150 m in SE-NW-direction

DESCRIPTION OL_KR20_BJI_7008_7290

The intersection is composed mainly of VGN with a short section of QGN. In VGN there are old, welded fractures bearing green unidentified mineral. The intersection contains 21 fractures, which have dip direction towards SE with moderate dip. The intersection contains also one slickensided surface (trend towards SE, moderate plunge). At 71.13-71.37 m and 71.79 m there are water conductive fractures. Some mechanical fracturing has occurred during the drillings.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=RE=RS=L

Right-reverse fault

Average dip/dip direction 42/158. Mean fault vector orientation 38/112.

INTERSECTIONS

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

At 71.13-71.37 m and 71.79 m there are water conductive fractures.

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_c_4.dtm

COMPILATION DATE AND COMPILED BY

16.12.2005 Seppo Paulamäki

APPENDIX 3 283

ID OL-BFZ069

DIMENSIONS 250 m in NE-SW-direction 250 m in SE-NW-direction

DESCRIPTION OL_KR13_BFI_47500_48052

The intersection is composed of VGN and PGR. The intersection contains 16 fractures of which 10 have slickensided surfaces. The PGR does not contain any joints and is also totally un-deformed. The fractures occur in different directions but most are N-S trending. The slickensided surfaces have lineations in random directions but most plunge towards south. The F vector shows a L-R-L pattern in most of the faults. No signs of water conductivity occur in this section.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=L(N) E=R(N)S=L

Reverse/left-reverse fault

Average dip/dip direction 54/056. Mean fault vector orientation 27/101.

INTERSECTIONS OL_KR13_BFI_47500_48052

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_c_5.dtm

COMPILATION DATE AND COMPILED BY

16.12.2005 Seppo Paulamäki

APPENDIX 3 284

ID OL-BFZ070

DIMENSIONS 250 m in NE-SW-direction 250 m in SE-NW-direction

DESCRIPTION OL_KR12_BFI_50500_50600

Short section of slickensides occurring in slightly sheared mica migmatite. Main part of fractures are slickensides, which are closely parallel to each other and foliation.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=no data E=no data S=no data

Average dip/dip direction 22/145. Mean fault vector orientation 17/090.

INTERSECTIONS OL_KR12_BFI_50500_50600

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION

505.52-507.06 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_c_6.dtm

COMPILATION DATE AND COMPILED BY

16.12.2005 Seppo Paulamäki

APPENDIX 3 285

ID OL-BFZ071

DIMENSIONS 265 m in N-S-direction 261 m in E-W-direction

DESCRIPTION OL_KR15_BFI_32308_33200

The intersection is composed of VGN. The plagioclases are slightly altered to sericite/epidote. The intersection contains (330.55-331.05) a quartz vein with sphalerite and chalcopyrite. It also contains a few old and welded fractures with calcite infillings. The intersection contains 53 fractures. The dip directions and dips of the fractures are scattered, with a concentration of fractures showing a dip direction towards SSW with a moderate dip. The fractures are partly parallel to the foliation. The rock in the intersection has an average of 5 fractures/m, with a more intensely fractured part (327.11-330.15 m) exhibiting 27 fractures. One fracture (327.55 m) in this part also contains gouge (dark grey clay infilling) but no water conductivity measurement has been carried out in this part of the borehole. The intersection exhibit 13 fractures with a slickensided surface having a striation direction from E to S, with a moderate plunge. Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=RE=RS=L

Average dip/dip direction 26/170. Mean fault vector orientation 24/095.

INTERSECTIONS OL_KR15_BFI_32308_33200

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_c_7.dtm

COMPILATION DATE AND COMPILED BY

19.12.2005 Seppo Paulamäki

APPENDIX 3 286

ID OL-BFZ072

DIMENSIONS 420 m in NE-SW-direction 250 m in SE-NW-direction

DESCRIPTION OL_KR13_BFI_24584_25500

The intersection is composed of VGN with some short sections of PGR (248.00-249.35 m). Both rock types are evenly fractured and contain old and welded fractures where calcite is present. The fractures have a direction parallel to the foliation (NE-SW trend) with moderate dip towards SSE. The intersection contains 65 fractures, app. 7 fractures per 1 metre. The intersection exhibits 10 slickensided surfaces with E-W striation (moderate dip towards E).

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=R(L) E=R(L)S=L(R)

Right-reverse or left –normal fault?

Average dip/dip direction 41/143. Mean fault vector orientation 40/110.

INTERSECTIONS OL_KR13_BFI_24584_25500

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION

248.00-249.70 m RiIII (clay-/grain-filled fracture at the bottom of the zone) 254.03-254.96 m RiIII (almost half of the fractures are closed)

COMPARISON TO BEDROCK MODEL 2003/1

KR13_6R (RH20C)

UPDATES - version history V 0 FILE group_c_8.dtm

COMPILATION DATE AND COMPILED BY

19.12.2005 Seppo Paulamäki

APPENDIX 3 287

ID OL-BFZ073

DIMENSIONS 100 m in NE-SW-direction 100 m in SE-NW-direction

DESCRIPTION OL_KR7_BFI_22701_22880

Core sample is totally splitted. Veined gneiss is porous, cavities are visible, grain-filled fractures. in places on fracture surface, lots of pyrite and clay minerals can be detected. Strong geophysical anomalies are connected to this section.

OL_KR7_DSI_22701_23035

Shear zone, in places blastomylonite.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=RE=NS=L

Right-reverse fault

Average dip/dip direction 47/150. Mean fault vector orientation 28/095.

INTERSECTIONS OL_KR7_BFI_22701_22880

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

0 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

KR07_3RH (RH20A)

UPDATES - version history V 0 FILE group_c_9.dtm

COMPILATION DATE AND COMPILED BY

19.12.2005 Seppo Paulamäki

APPENDIX 3 288

ID OL-BFZ074

DIMENSIONS 150 m in NE-SW-direction 150 m in SE-NW-direction

DESCRIPTION OL_KR8_BJI_8000_8380

Brittle fracturing stays on old sheared, brecciated and welded section. Brittle fractures are more abundant than normally. 2 to 3 open fractures with orientations of 40º/26º, 50º/33º and 29º/28º. At depth of 82.30 m a high water-conductivity linked to a separate remarkably large open fracture. Majority of the brittle phase fractures are rather parallel. In total, modest-looking.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=no data E=no data S=no data

Average dip/dip direction 51/043. Mean fault vector orientation 28/103.

INTERSECTIONS OL_KR8_BJI_8000_8380

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

A high water-conductivity linked to a separate remarkably large open fracture at 82.30 m

IMPLICATIONS TO CONSTRUCTION

81.13-83.46 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR08_3RH (RH19A)

UPDATES - version history V 0 FILE group_c_10.dtm

COMPILATION DATE AND COMPILED BY

19.12.2005 Seppo Paulamäki

APPENDIX 3 289

ID OL-BFZ075

DIMENSIONS 200 m in N-S-direction 200 m in E-W-direction

DESCRIPTION OL_KR14_BFI_44500_44908

The intersection is composed of VMGT and in the latter part of MAFGN and MGN. The intersection contains 28 fractures. The fractures dip direction and dip is scattered, with a concentration of fractures showing a dip direction towards SE with a moderate dip. The rock in the intersection has an average of 7 fractures/m. The central part of the intersection contains two sections (446.40-446.83 & 447.68-448.13) of intensely fractured and partly crushed rock. The latter section exhibit slightly altered feldspars (white-green alteration) and it also show signs of water conductivity (grey clay infillings). The majority of the fractures (16) in the intersection exhibit a slickensided surface, with two different striation direction one towards NE and the other towards SE. The striations have a moderate plunge. Mechanical fracturing has occurred during the drilling.

OL_KR15_BFI_44962_45600

The intersection is composed of MGN. The rock exhibits a few old, welded, calcite-bearing fractures. The fractures are randomly orientated with horizontal to moderate dip. The intersection contains 53 joints, with a more fractured part (449.85-451.95 m) exhibiting 36 fractures. The slickensides (only 5) have striation trend of NE-SW with moderate plunge. Some fractures (at least at 451.25 m, containing dark, unidentified clay mineral) might act as a water channels, but no water conductive measurements has been carried out in this part of the borehole. Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=LE=NS=R

Left-normal fault

Average dip/dip direction 32/172. Mean fault vector orientation 22/118.

INTERSECTIONS OL_KR14_BFI_44500_44908 OL_KR15_BFI_44962_45600

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION

OL-KR14 446.44-448.11 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR15_4R

UPDATES - version history V 0

APPENDIX 3 290

FILE group_c_11.dtm

COMPILATION DATE AND COMPILED BY

19.12.2005 Seppo Paulamäki

APPENDIX 3 291

ID OL-BFZ076

DIMENSIONS 890 m in NE-SW-direction 310 m in SE-NW-direction

DESCRIPTION OL_KR13_BFI_44550_46800

The intersection is mainly composed of VGN, and some sections of PGR and MGN. The intersection contains 133 fractures of which 45 are slickensides. The VGN is usually more densely fractured than the other rock types. Old and welded fractures are rare except for the GRPG where paleo shear zones and healed fractures with calcite infillings occur. The fractures in the intersection occur parallel to the foliation (NNE-SSW trend with moderate dips towards SSE). The slickensided surfaces have lineations in random directions but most plunge towards south. At 456-467 m there is signs of water conductivity in many fractures (greyish clay infillings).

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=RE=R(L)S=L

Right-reverse fault

Average dip/dip direction 36/148. Mean fault vector orientation 38/103.

INTERSECTIONS OL_KR13_BFI_44550_46800

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

At 456-467 m there is signs of water conductivity in many fractures (greyish clay infillings).

IMPLICATIONS TO CONSTRUCTION

451.04-451.84 m RiIII 454.34-454.97 m RiIII (almost half of the fractures are closed) 457.33-459.23 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR13_10R

UPDATES - version history V 0 FILE group_c_12.dtm

COMPILATION DATE AND COMPILED BY

19.12.2005 Seppo Paulamäki

APPENDIX 3 292

ID OL-BFZ077

DIMENSIONS 250 m in N-S-direction 250 m in E-W-direction

DESCRIPTION OL_KR7_BFI_40925_41040

A short breakage in mica-prevailing migmatite, which is strongly aided by drilling and the sample is practically macadam. Strong geophysical anomalies, except water-conductivity, which is insignificant. Older strong ductile shear is visible.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=RE=NS=L

Right-reverse fault

Average dip/dip direction 45/170. Mean fault vector orientation 24/109.

INTERSECTIONS OL_KR7_BFI_40925_41040

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

KR07_9R (R56)

UPDATES - version history V 0 FILE group_c_13.dtm

COMPILATION DATE AND COMPILED BY

19.12.2005 Seppo Paulamäki

APPENDIX 3 293

ID OL-BFZ078

DIMENSIONS 370 m in NE-SW-direction 400 m in SE-NW-direction

DESCRIPTION OL_KR19_BFI_17458_18675

The intersection is composed of VGN with a short section of MFGN (at 175.31-175.82 m), TGG (176.81-182.46 m) and PGR. MFGN is altered (skarn). The intersection contains old, welded fractures with calcite infillings. Some of these welded fractures have been reactivated later. The intersection contains 45 fractures. The dip directions of the fractures are towards NE and SE with moderate dip. The rock in the intersection is evenly fractured. The majority of the fractures (29) in the intersection exhibit a slickensided surface, with the striation direction towards SE with moderate plunge. At 182.00-183 m and 184.26-184.76 m the fractures show water conductivity (kaolinite infilling). Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=RE=LS=L

Right-reverse fault

Average dip/dip direction 33/137. Mean fault vector orientation 30/114.

INTERSECTIONS OL_KR19_BFI_17458_18675

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

At 182.00-183 m and 184.26-184.76 m the fractures show water conductivity (kaolinite infilling).

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_c_14.dtm

COMPILATION DATE AND COMPILED BY

19.12.2005 Seppo Paulamäki

APPENDIX 3 294

ID OL-BFZ079

DIMENSIONS 245 m in N-S-direction 407 m in E-W-direction

DESCRIPTION OL_KR5_BFI_26945_27068

Short intensively fractured intersection in veined gneiss. Strong shear in narrow seams. kaolinitisation and illitisation are visible. Fractures are quite parallel with each other and shearing. Slickensided fractures and in TV image 1 - 2 open fractures can be detected. Small water-conductivity. FDV = 153º/10º can be seen on stepped slickensides.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=LE=LS=R

Left-normal fault

Average dip/dip direction 27/161. Mean fault vector orientation 30/107.

INTERSECTIONS OL_KR5_BFI_26945_27068 Single groupB-faults in KR20 at 412-413 m (upper part of OL_KR20_BFI_41059_42445)

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics, charge potential

3 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

Small water-conductivity

IMPLICATIONS TO CONSTRUCTION

OL-KR5 269.38-270.63 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR05_5R (RH9)

UPDATES - version history V 0 FILE group_c_15.dtm

COMPILATION DATE AND COMPILED BY

19.12.2005 Seppo Paulamäki

APPENDIX 3 295

ID OL-BFZ080

DIMENSIONS 100 m in NE-SW-direction 100 m in SE-NW-direction

DESCRIPTION OL_KR25_BJI_36931_37320

The intersection is composed of DTX and VGN. The DTX section (369.70-371.75 m) in the rock is strongly altered, containing feldspars, which are altered to albite (yellow-greenish coloured). This section also contains thick (max. 5 cm) calcite bearing water-conducting fractures (20 fractures). The neosomes in the VGN exhibit a green soft unidentified mineral. The VGN contains only a few fractures. The fractures are randomly orientated, usually with a nearly horizontal dip. At 370.75 m there is 10 cm of core loss and the Wellcad-picture shows in this part a large fracture/cavity (this part contains small calcite crystals). This fracture/cavity also shows a clear peak in the flow rate table. Some mechanical fracturing has occurred during the drillings.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=LE=LS=R

Left-normal fault

Average dip/dip direction 23/120. Mean fault vector orientation 20/110.

INTERSECTIONS OL_KR25_BJI_36931_37320

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

A clear peak in the flow rate table at 370.75 m, where there is a large fracture/cavity containing small calcite crystals, and.10 cm of core loss.

IMPLICATIONS TO CONSTRUCTION

369.90-371.23 m RiIII, strongly weathered (Rp1-2)

COMPARISON TO BEDROCK MODEL 2003/1

The borehole did no exist in 2003.

UPDATES - version history V 0 FILE group_c_16.dtm

COMPILATION DATE AND COMPILED BY

20.12.2005 Seppo Paulamäki

APPENDIX 3 296

ID OL-BFZ081

DIMENSIONS 50 m in NE-SW-direction 50 m in SE-NW-direction

DESCRIPTION OL_KR10_BFI_10970_11045

4 to 5 single slickensides cross-cutting each other in high angle. Some of the slickensides are parallel to foliation, some of them crosscuts foliation and schistosity. On one slickenside there is a thin pyrite-coating. FVD's are almost parallel and heading to east. Not very remarkable intersection.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=LE=R(N)S=L

Left-reverse fault

Average dip/dip direction 47/121. Mean fault vector orientation 32/106.

INTERSECTIONS OL_KR10_BFI_10970_11045

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_c_17.dtm

COMPILATION DATE AND COMPILED BY

20.12.2005 Seppo Paulamäki

APPENDIX 3 297

ID OL-BFZ082

DIMENSIONS 100 m in NE-SW-direction 100 m in SE-NW-direction

DESCRIPTION OL_KR19_BJI_20234_20286

The intersection is composed of VGN. The rock contains old, welded, calcite bearing fractures. One thick (1 cm), calcite- and kaolinite-bearing fracture at 202.50 m has reactivated later. The intersection contains 19 fractures. The fractures are randomly orientated. The rock in the intersection is evenly fractured. Most of the fractures show signs of water conductivity (kaolinite infillings). Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=RE=RS=L

Right-reverse fault

Average dip/dip direction 39/160. Mean fault vector orientation 11/090.

INTERSECTIONS OL_KR19_BJI_20234_20286 4 group C faults at 200-201 m

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics, (VSP?)

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

Most of the fractures show signs of water conductivity (kaoline infillings).

IMPLICATIONS TO CONSTRUCTION

202.34-202.86 m RiIII 202.02-203.01 Rp1

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_c_18.dtm

COMPILATION DATE AND COMPILED BY

20.12.2005 Seppo Paulamäki

APPENDIX 3 298

ID OL-BFZ083

DIMENSIONS 100 m in N-S-direction 100 m in E-W-direction

DESCRIPTION OL_KR19_BFI_20986_21153

The intersection is composed of VGN. The rock contains a few old, welded, calcite-bearing fractures. Some of them have been reactivated later. The intersection consists about 7 fractures/ 1 metre (14 fractures altogether). The dip directions and dips of the fractures are scattered. Four slickensided surfaces are also observed (NE and SE orientated). Some of them seem to be created into paleo fractures, which have been reactivated. At 209.86-209.89 m there are water conductive fractures (two fractures).

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=LE=RS=R

Left-normal/left-reverse? fault

Average dip/dip direction 45/169. Mean fault vector orientation 18/091.

INTERSECTIONS OL_KR19_BFI_20986_21153

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

Two water-conductive fractures at 209.86-209.89 m.

IMPLICATIONS TO CONSTRUCTION

211.29-212.20 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_c_19.dtm

COMPILATION DATE AND COMPILED BY

20.12.2005 Seppo Paulamäki

APPENDIX 3 299

ID OL-BFZ084

DIMENSIONS 247 m in N-S-direction 400 m in E-W-direction

DESCRIPTION OL_KR3_BFI_15820_16275

Pegmatite containing voluminous mica-rich parts, around which the rock has slipped and plenty of slickensides were born. Slight alteration, some pyrite on fracture surfaces and sporadic illite-coatings.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=RE=NS=L

Right-normal fault

Average dip/dip direction 64/182. Mean fault vector orientation 19/099.

INTERSECTIONS OL_KR3_BFI_15820_16275

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

0 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION

158.97-161.69 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR03_3R (R10A)

UPDATES - version history V 0 FILE group_c_20.dtm

COMPILATION DATE AND COMPILED BY

20.12.2005 Seppo Paulamäki

APPENDIX 3 300

ID OL-BFZ085

DIMENSIONS 153 m in N-S-direction 224 m in E-W-direction

DESCRIPTION OL_KR1_BFI_10851_11036

Densely-fractured intersection in veined gneiss. Fractures parallel with foliation are abundantly present as well as fractures perpendicular to foliation. Drilling has assisted the splitting up of the drill core sample. Macadam-looking core sample, however, show some slickensided surfaces. TV image shows 2 - 3 clear open fractures. Fracture surfaces carry powder-like clay minerals. Porosity and sericitization (zinnwaldite) are detected. Two remarkable water-flow anomalies are situated in this very section.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=no data E=no data S=no data

Average dip/dip direction 58/185. Mean fault vector orientation 27/090.

INTERSECTIONS OL_KR1_BFI_10851_11036

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

0 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

Two remarkable water-flow anomalies are situated in this section.

IMPLICATIONS TO CONSTRUCTION

108.58-109.86 m RiIII 108.45-112.20 m Rp1

COMPARISON TO BEDROCK MODEL 2003/1

KR01_2RH (RH11_ALT, RH20A_ALT)

UPDATES - version history V 0 FILE group_c_21.dtm

COMPILATION DATE AND COMPILED BY

20.12.2005 Seppo Paulamäki

APPENDIX 3 301

ID OL-BFZ086

DIMENSIONS 100 m in NE-SW-direction 100 m in SE-NW-direction

DESCRIPTION OL_KR17_BFI_12350_13092

VGN is the main rock type in the intersection, with some DTX in the beginning. The feldspars are slightly altered to sericite. The intersection contains a few old and welded fractures with calcite and pyrite infillings. It exhibits 56 fractures, with a dip direction towards SE and a moderate dip. The rock is intensely fractured at 124.30-124.70 m (12 fractures) and 128.90-129.45 m (13 fractures). These sections show signs of water flowing, containing kaolinite and grey-green clay infilling. The latter section also contains 20 cm core loss. The intersection exhibit 8 fractures with a slickensided surface, six of these have a striation direction varying from NE to SE, with a moderate plunge. Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=R/LE=R/NS=L

Right-reverse/left-reverse? fault

Average dip/dip direction 37/141. Mean fault vector orientation 22/099.

INTERSECTIONS OL_KR17_BFI_12350_13092

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

0 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

Intensely fractured sections 124.30-124.70 m and 128.90-129.45 m show signs of water flowing, containing kaolinite and grey-green clay infilling.

IMPLICATIONS TO CONSTRUCTION

124.33-125.14 m RiIII 128.27-129.81 m RiIII 124.14-125.12 m Rp1

COMPARISON TO BEDROCK MODEL 2003/1

KR17_3R (R78)

UPDATES - version history V 0 FILE group_c_22.dtm

COMPILATION DATE AND COMPILED BY

20.12.2005 Seppo Paulamäki

APPENDIX 3 302

ID OL-BFZ087

DIMENSIONS 100 m in NE-SW-direction 100 m in SE-NW-direction

DESCRIPTION OL_KR19_BFI_17458_18675

The intersection is composed of VGN with a short section of MFGN (at 175.31-175.82 m), TGG (176.81-182.46 m) and PGR. MFGN is altered (skarn). The intersection contains old, welded fractures with calcite infillings. Some of these welded fractures have been reactivated later. The intersection contains 45 fractures. The fractures dip directions are towards NE and SE with moderate dip. The rock in the intersection is evenly fractured. The majority of the fractures (29) in the intersection exhibit a slickensided surface, with the striation direction towards SE with moderate plunge. At 182.00-183 and 184.26-184.76 the fractures show water conductivity (kaolinite infilling). Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=RE=RS=L

Right-reverse fault

Average dip/dip direction 24/073. Mean fault vector orientation 26/102.

INTERSECTIONS OL_KR19_BFI_17458_18675

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

0 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

At 182.00-183 and 184.26-184.76 the fractures show water conductivity (kaolinite infilling).

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_c_23.dtm

COMPILATION DATE AND COMPILED BY

20.12.2005 Seppo Paulamäki

APPENDIX 3 303

ID OL-BFZ088

DIMENSIONS 100 m in NE-SW-direction 100 m in SE-NW-direction

DESCRIPTION OL_KR10_BFI_10970_11045

4 to 5 single slickensides cross-cutting each other in high angle. Some of the slickensides are parallel to foliation, some of them crosscuts foliation and schistosity. On one slickenside there is a thin pyrite-coating. FVD's are almost parallel and heading to east. Not very remarkable intersection.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP C

U=LE=RS=L

Left-reverse fault

Average dip/dip direction 24/073. Mean fault vector orientation 26/102.

INTERSECTIONS OL_KR10_BFI_10970_11045 + 3 single faults at 106-108 m

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_c_24.dtm

COMPILATION DATE AND COMPILED BY

20.12.2005 Seppo Paulamäki

APPENDIX 3 304

ID OL-BFZ089

DIMENSIONS 39 m in N-S-direction 265 m in E-W-direction

DESCRIPTION OL_KR15_BFI_32308_33200

The intersection is composed of VGN. The plagioclases are slightly altered to sericite/epidote. The intersection contains (330.55-331.05) a quartz vein with sphalerite and chalcopyrite. It also contains a few old and welded fractures with calcite infillings. The intersection contains 53 fractures. The fractures dip direction and dip is scattered, with a concentration of fractures showing a dip direction towards SSW with a moderate dip. The fractures are partly parallel to the foliation. The rock in the intersection has an average of 5 fractures/m, with a more intensely fractured part (327.11-330.15) exhibiting 27 fractures. One fracture (327.55) in this part also contains gouge (dark grey clay infilling) but no water conductivity measurement has been carried out in this part of the borehole. The intersection exhibit 13 fractures with a slickenside surface, these have a striation direction from E to S, with a moderate plunge. Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP D

U=RE=RS=L

Right-reverse fault

Average dip/dip direction 84/152. Mean fault vector orientation 40/070.

INTERSECTIONS OL_KR15_BFI_32308_33200 Two group D faults in OL-KR12 at 327 m

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_d_1.dtm

COMPILATION DATE AND COMPILED BY

20.12.2005 Seppo Paulamäki

APPENDIX 3 305

ID OL-BFZ090

DIMENSIONS 130 m in NE-SW-direction 46 m in SE-NW-direction

DESCRIPTION OL_KR14_BFI_46985_47623

The rock in the intersection is mainly composed of VGN and some sections of massive PGR. The intersection contains 26 fractures. The fractures are showing a dip direction towards ENE with a moderate dip. The rock in the intersection has an average of ca. 4 fractures/m. The intersection exhibit 8 fractures with a slickensided surface, these have a striation direction towards NE, with a moderate plunge. Three of these slickensided surfaces indicate a L, R, R movement. No signs of water conductivity.

OL_KR15_BFI_49350_49650

The intersection is composed of MGN. The rock has only a few old, welded, calcite-bearing fractures. The fractures (13) dip towards SE with horizontal to steep dip. The fractures are parallel to the foliation. The majority of the fractures in the intersection contain slickensided surfaces (9) having a NE-SW trend. No water conductivity measurement has been carried out in this part of the borehole.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP D

U=LE=RS=R

Left-normal fault

Average dip/dip direction 71/137. Mean fault vector orientation 29/061.

INTERSECTIONS OL_KR14_BFI_46985_47623 OL_KR15_BFI_49350_49650

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

2 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION

470.03-471.39 Rp0 (Rp1)

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_d_2.dtm

COMPILATION DATE AND COMPILED BY

20.12.2005 Seppo Paulamäki

APPENDIX 3 306

ID OL-BFZ091

DIMENSIONS 100 m in NE-SW-direction 156 m in SE-NW-direction

DESCRIPTION OL_KR29_BFI_84830_85197

The intersection is mainly composed of PGR, with some short sections of VGN. The PGR contains a section (849.26-849.53 m) with soft and crushed rock, partly caused by the drilling. This section is 27 cm thick and it is probable that water has been flowing. The intersection has 25 fractures and some of them contain illite and kaolinite infillings, indicating water flowing, although this is not shown in the flow measurements. 10 of these fractures contain a slickensided surface. Due to absent Wellcad picture and base line no directions have been measured, but some of the fractures have foliation parallel direction. Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP D

U=L(N) E=LS=L

Reverse/left-reverse fault

Average dip/dip direction 47/020. Mean fault vector orientation 23/063. The orientation is based on two faults above and below the intersection.

INTERSECTIONS OL_KR29_BFI_84830_85197

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

1 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION

849.26-849.52 m RiV 851.45-851.81 m RiIV

COMPARISON TO BEDROCK MODEL 2003/1

The borehole did not exist in 2003.

UPDATES - version history V 0 FILE group_d_3.dtm

COMPILATION DATE AND COMPILED BY

20.12.2005 Seppo Paulamäki

APPENDIX 3 307

ID OL-BFZ092

DIMENSIONS 410 m in NE-SW-direction 231 m in SE-NW-direction

DESCRIPTION OL_KR13_BFI_36275_37446

The intersection is mainly composed of clearly foliated TGG and one section of quartz (372.12-373.30m). The intersection is relatively un-fractured but contains signs of paleo shearing with old welded fractures with greyish matrix and calcite infillings. The intersection contains 51 fractures, app. 4 fractures per metre. The fractures have a random direction with steep dip. The intersection has 11 slickensided surfaces, which are randomly orientated (moderate dip). At 363.23-363.70 m the drill core is crushed and shows signs of water conductivity.

OL_KR19_BFI_20986_21153

The intersection is composed of VGN. The rock contains a few old, welded, calcite-bearing fractures. Some of them have been reactivated later. The intersection consists about 7 fractures/ 1 metre (14 fractures altogether). The fractures dip direction and dip is scattered. Four slickensided surfaces are also observed (NE and SE orientated). Some of them seem to be created into paleo fractures, which have been reactivated. At 209.86-209.89 there are water conductive fractures (two fractures).

OL_KR20_BJI_17760_18105

The intersection is composed of PGR. The intersection contains a few old and welded fractures where calcite is present. The intersection contains 29 fractures. The dip directions of the fractures are between E and SE with from almost horizontal to moderate dip. The intersection contains one slickensided surface at 181.05 (SE trend, moderate plunge). Some of the fractures follow the foliation. The rock in the intersection is mainly evenly fractured. Between 179.88 and 180.26 there are fractures showing signs of water conductivity.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP E

U=RE=RS=L

Right-reverse fault

Average dip/dip direction 38/111. Mean fault vector orientation 32/142.

INTERSECTIONS OL_KR13_BFI_36275_37446 OL_KR19_BFI_20986_21153 OL_KR20_BJI_17760_18105

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

3 (0=very low, 1=low, 2=moderate, 3=high)

APPENDIX 3 308

HYDROLOGICAL FEATURES

OL-KR13: At 363.23-363.70 m the drill core is crushed and shows signs of water conductivity. OL-KR19: At 209.86-209.89 m there are water conductive fractures (two fractures). OL-KR20: Between 179.88 m and 180.26 m there are fractures showing signs of water conductivity.

IMPLICATIONS TO CONSTRUCTION

OL-KR13 362.96-363.89 m RiIV, 362.53-373.41 m Rp1 OL-KR19 211.29-212.20 m RiIII OL-KR20 179.34-181.05 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR13_8R KR20_3R

UPDATES - version history V 0 FILE group_e_1.dtm

COMPILATION DATE AND COMPILED BY

20.12.2005 Seppo Paulamäki

APPENDIX 3 309

ID OL-BFZ093

DIMENSIONS 497 m in NE-SW-direction 288 m in SE-NW-direction

DESCRIPTION OL_KR4_BFI_79100_79200

Sheared mica gneiss, which is indented in the whole intersection but especially at the contact of pegmatite. Mica gneiss is strongly altered, chloritized and illitized and the sample is totally crushed.

OL_KR7_BFI_68990_69200

Short breakage with splitted core sample. Intersection is located in mica-rich migmatite inside an intact pegmatite. Above the breakage there is ca. 5 m and below ca. 3 m of un-fractured pegmatite. Intersection is joined with porosity and gouge clay. No water-conductivity.

OL_KR29_BFI_74570_74730

The rock type in the intersection is DTX. The intersection contains plenty of old and welded fractures with calcite infillings. The intersection exhibits 18 fractures, with a E-W trend with a shallow dip, towards N or S. It contains one fracture, which indicates water flowing (kaolinite infilling). The intersection exhibit 5 fractures with a slickensided surface and three of these have a striation direction towards N or S with a moderate plunge.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP E

U=RE=LS=R

Right-normal fault

Average dip/dip direction 29/139. Mean fault vector orientation 26/152.

INTERSECTIONS OL_KR4_BFI_79100_79200 OL_KR7_BFI_68990_69200 OL_KR29_BFI_74570_74730

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

3 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION

OL-KR29 746.31-747.22 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR07_10 R (RH21)

UPDATES - version history V 0 FILE group_e_2.dtm

COMPILATION DATE AND COMPILED BY

20.12.2005 Seppo Paulamäki

APPENDIX 3 310

ID OL-BFZ094

DIMENSIONS 100 m in NE-SW-direction 100 m in SE-NW-direction

DESCRIPTION OL_KR12_BFI_58240_58410

Short brittle section in fine-grained mica-rich rock with scarce or no neosome. The rock changes in the bottom of the section into cordierite-bearing gneiss. Brittle section covers an old welded micro-fracturing and -breccia of some very early stage. Fractures and slickensides carry voluminous fillings.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP E

U=LE=RS=L

Left-reverse fault

Average dip/dip direction 74/117. Mean fault vector orientation 37/144.

INTERSECTIONS OL_KR12_BFI_58240_58410

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

0 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION

581.53-584.02 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR12_15 R

UPDATES - version history V 0 FILE group_e_3.dtm

COMPILATION DATE AND COMPILED BY

21.12.2005 Seppo Paulamäki

APPENDIX 3 311

ID OL-BFZ095

DIMENSIONS 100 m in N-S-direction 100 m in E-W-direction

DESCRIPTION OL_KR19_BJI_7506_7730

The intersection is mainly composed of VGN with a short section of PGR. The rock contains old, welded, calcite bearing fractures. Here and there the feldspars are altered (sericitized?). The intersection contains 23 fractures. Most of the fractures have a dip direction towards SE with a moderate dip. The rock in the intersection is evenly fractured having an average of 10 fractures/m. The fractures at 76.00-77.00 m show signs of water conductivity (kaolinite infillings). At 76.71 m there is 0.07 m core loss. Mechanical fracturing has occurred during the drilling.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP E

U=LE=RS=L

Left-reverse fault

Average dip/dip direction 13/093. Mean fault vector orientation 30/136.

INTERSECTIONS OL_KR19_BJI_7506_7730

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

0 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

The fractures at 76.00-77.00 m show signs of water conductivity.

IMPLICATIONS TO CONSTRUCTION

75.90-77.00 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR19_4R

UPDATES - version history V 0 FILE group_e_4.dtm

COMPILATION DATE AND COMPILED BY

21.12.2005 Seppo Paulamäki

APPENDIX 3 312

ID OL-BFZ096

DIMENSIONS 200 m in N-S-direction 200 m in E-W-direction

DESCRIPTION OL_KR12_BFI_20245_20600

Mica-rich migmatite displays an old welded micro-fracturing and -breccia, which has later broken. Slickensides with fillings of calcite and small fragments in hard clay. Many of the slickensides are in low angle to the core and FDV seems to be quite horizontal.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP E

U=no data E=no data S=no data

Average dip/dip direction 85/244. Mean fault vector orientation 15/157.

INTERSECTIONS OL_KR12_BFI_20245_20600

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

0 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION

203.15-204.45 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

KR12_5R

UPDATES - version history V 0 FILE group_e_5.dtm

COMPILATION DATE AND COMPILED BY

21.12.2005 Seppo Paulamäki

APPENDIX 3 313

ID OL-BFZ097

DIMENSIONS 100 m in NE-SW-direction 100 m in SE-NW-direction

DESCRIPTION A set of faults (13 slickensides) in OL-KR4 at 51.65-54.52 m dominated by group E faults.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP E

U=no data E=no data S=no data

Average dip/dip direction 47/156. Mean fault vector orientation 35/155.

INTERSECTIONS

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersections, kinematics

0 (0=very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1 UPDATES - version history V 0 FILE group_e_6.dtm

COMPILATION DATE AND COMPILED BY

21.12.2005 Seppo Paulamäki

APPENDIX 3 314

ID OL-BFZ098

DIMENSIONS X/Y/Z, m

DESCRIPTION OL_KR1_BJI_14118_14395

Granitic - pegmatitic section with steeply-dipping fractures and in the bottom also subhorizontal fractures. Obviously drilling has opened fractures, which seem to be old and welded. Slight alteration is visible in granite, quartz, epidote (?), illite.

OL_KR14_BFI_21755_21913

The intersection is composed of VMGT. The fractures seem to mainly be parallel to the foliation, but no certainty could be established because of absent Wellcad picture. The intersection contains 8 joints, with an average of ca. 4 fractures/m. The intersection contains 5 fractures with slickenside surface, but due to the absent Wellcad picture no direction and movement could be established. No signs of water conductivity.

OL_KR22_BFI_33765_34045

This intersection contains DTX that contains large amounts of GRPG neosome. Between 338.50 m and 340 m the rock is slightly sheared. The intersection contains 34 fractures and has an average joint density of 12 joints / m. At least 10 of these fractures have slickenside surfaces but the drillcore is so shattered near the slickensides that measurements could only be carried out on 3 ss. Some old and healed joints with calcite infillings occur and some mechanical fracturing of them may have occurred during the drillings. The direction of the joints is so varying that any clear joint set can not be distinguished. The measured slickensides are also randomly oriented. Many fractures have calcite and epidote infillings. No signs of water conductivity were observed.

OL_KR29_BJI_33046_33086

Set of 11 fractures in medium grained MGN. Few thin neosome veins with fractures in contacts. Quite varying fracture directions. Some fractures filled by carbonate.

OL_KR3_BJI_4630_4880

Mica gneiss shows slightly elevated fracturing. In fact, the intersection shows 2 - 3 short (20 - 30 cm) sets of parallel fractures. Some of fractures are slickensides. Two FDV's are 225º/14º and 152º/37º

OL_KR4_BFI_31340_31615

Several, 246/80 oriented slickensides roughly parallel to the drilling direction. Transverse, open and weathered fractures have been found in direction 242/46 at length of 313.49 m and in direction 221/22 at length of 315.14 m. Thick fillings in these fractures are composed of calcite, iron sulphides and zinc blende.

APPENDIX 3 315

OL_KR7_BFI_28732_28870

Just below the previous section, a short two-folded breakage, agin drilling-induced effects on splitting. On fracture surfaces, light and greenish clay minerals and pyrite. A single slickenside. Water-conductivity. Short and modest-looking.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Group A?

U = R E = R S = L

Right-reverse fault

Gently dipping, semiplanar feature. Dip/dip direction c. 15 – 30/140 – 160. Fault vector orientation 21/165 or 28/357.

INTERSECTIONS OL_KR1_BJI_14118_14395 OL_KR14_BFI_21755_21913 OL_KR22_BFI_33765_34045 OL_KR29_BJI_33046_33086 OL_KR3_BJI_4630_4880 OL_KR4_BFI_31340_31615 OL_KR7_BFI_28732_28870 OL-KR10 248.93 – 251.04 OL-KR25 294.74 – 295.33

BASIS FOR INTERPRETATION

CONFIDENCE

Mise-a-la-masse, drillhole intersections

2 Moderate (0= very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR1: 136.05 – 143.95 Rp0-1 OL-KR1: 141.66 – 143.81 RiIII

OL-KR3: 40.58 – 68.05 Rp1

OL-KR4: 313.00 – 323.00 Rp0-1 OL-KR4: 313.41 – 316.10 RiIII

OL-KR10: 169.20 – 260.40 Rp0

OL-KR14: 184.22 – 292.00 Rp0

OL-KR22: 331.75 – 355.15 Rp0(Rp1)

OL-KR25: 284.00 – 320.70 Rp0

OL-KR29: 320.20 – 333.50 Ri1(Rp2) COMPARISON TO BEDROCK MODEL 2003/1

R56_ALT (OL-KR1) RH20A (OL-KR4) RH20B (OL-KR7)

UPDATES - version history V 0 FILE Zone1.dtm

COMPILATION DATE AND COMPILED BY

21.12.2005 Markku Paananen

APPENDIX 3 316

ID OL-BFZ099

DIMENSIONS X/Y/Z, m 1650/1580/960

DESCRIPTION OL_KR1_BFI_52520_52620

Short section of veined gneiss, in places of augen structure. Very strong illitization makes the core sample "soapy". Illite occurs on fracture surfaces and as pervasive alteration. Water-low anomaly. TV image shows open fractures. Generally fracturing has random orientation which has been opened by drilling.

OL_KR11_BFI_62502_62647

In veined migmatite there is a short section, which contains a lots of graphite. Old small-scale microbreccia with calcite-filling. In later stage in this section a total crushing has happened and produced plenty of graphite-coated slickensides and black fine-grained clay fillings. Some water-conductivity has been measured.

OL_KR12_BFI_58240_58410

Short brittle section in fine-grained mica-rich rock with scarce or no neosome. The rock changes in the bottom of the section into cordierite-bearing gneiss. Brittle section covers an old welded microfracturing and -breccia of some very early stage (like at depth of 202.45 - 206.00 m). Fractures and slickensides carry voluminous fillings.

OL_KR13_BFI_44550_46800

The intersection is mainly composed of VMGT,and some sections of GRPG and MGN. The intersection contains 133 fractures of which 45 are slickensides. The VMGT is usually more densely fractured than the other rocktypes. Old and welded fractures are rare except for the GRPG where paleo shearzones and healed fractures with calcite infillings occur. The fractures in the intersection occur parallel to the foliation (NNE-SSW trend with moderate dips towards SSE). The slickenside surfaces have lineations in random directions but most plunge towards south. At 456-467 m there is signs of water conductivity in many fractures (greyish clay infillings).

OL_KR19_BFI_25335_25982

The intersection is mainly composed of VMGT with a short section of GRPG. The rock contains old, welded, calcite bearing fractures. Here and there the feldspars are altered (sericitized). The intersection contains 58 joints. The fractures are randomly orientated. 5 fractures in the intersection exhibit a slickenside surface, with the striation direction towards SW with moderate plunge. The intersection contains three gouges (rock fragments in dark clay and/or calcite matrix) at 253.60-253.70, 255.05-255.22 and 255.52-256.17. The rock in the intersection is evenly fractured having an average of 10 fractures/m. The fractures at 253.64-255.58 and 259.01-259.63 show signs of water conductivity (kaoline infillings). Mechanical fracturing has occurred during the drilling.

OL_KR2_BFI_50404_50795

APPENDIX 3 317

Veined gneiss, which is sheared, illitized and kaolinitized. Random fracturing, partly opened by drilling. A couple of open fractures. Many fracture surfaces carry voluminous kaolinite and powderised calcite.

OL_KR20_BFI_44963_45264

The intersection is composed of VMGT. The intersection contains 6 joints. The fractures dip direction and dip is scattered, with a concentration of fractures showing a dip direction towards NE with a moderate dip. The rock is evenly fractured. The intersection also contains four slickenside surfaces. These fractures have SSE trend with from almost horizontal to moderate plunge. The intersection contains a few old, calcite bearing, welded fractures. There are no signs of water conductivity.

OL_KR29_BFI_84830_85197

The intersection is mainly composed of GRPG, with some short sections of VMGT. The GRPG contains a section (849.26-849.53) with soft and crushed rock, partly caused by the drilling. This section is 27 cm thick and it is probable that water has been flowing. The intersection exhibits 25 fractures and some of them contain illite and kaolinite infillings, indicating water flowing, although this is not shown in the flow measurements. 10 of these fractures contain a slickenside surface. Due to absent Wellcad picture and base line no directions have been measured, but some of the fractures have foliation parallel direction. Mechanical fracturing has occurred during the drilling.

OL_KR33_BFI_27591_28043

The intersection composed of VMGT and DTX containing 55 fractures, some slickensides. Fracture density is varying inside the intersection and also technical breaking occurs in two 10-15 cm sections. Core loss in two depths (15 cm and 20 cm). Carbonate, kaolinite and illite infillings. Faults in two different directions. Clear pressure shadow carbonates in one fault in drillhole direction. Some old welded fractures. Not clear main directions of fracturing. High content of blueish pinitized cordierite with grain size of 1-10 mm. In appearances of K-feldspar grains also indicators of ductile shear.

OL_KR33_BFI_28678_28815

MGN intersection with 27 fractures and also breaks caused by drilling. Couple of fractures slickensides with strong striation. Fractures in different directions but usually dipping to SE like foliation (121/66), more discordance in GRPG section. Kinematic vector around 180/30. Slight alteration, kaolinite.

OL_KR4_BFI_75770_76270

The sample is totally crushed but relicts of several slickensides have been found. A fracture parallel to drilling direction is located in the section between drilling lengths of 758.30 – 758.50 m. The section contains many fractures steeply cross cutting the drilling direction and filled by kaolinite, illite, chlorite and grey clay. The wall roc is also pervasively illitized.

OL_KR5_BFI_26945_27068

Short intensively fractured intersection in veined gneiss. Strong shear in narrow seams. kaolinitisation and illitisation are visible. Fractures are quite parallel with each other and shearing. Slickensided fractures and in TV image 1 - 2 open fractures can be detected. Small water-conductivity. FDV = 153º/10º can be seen on stepped slickensides.

APPENDIX 3 318

OL_KR5_BFI_27897_28244

Stromatic gneiss, where narrow shear zones can be observed. Strong alteration has produced yellowish mineral, which is too hard to be illite (epidote?). Dense fracturing joins most often the direction of foliation. Thick fractures healed by calcite. In TV image there is an open fracture and voluminous porosity in the hanging wall of the pegmatite dyke or granitic band at depth of 280.60 m, where the core sample is lacking. Moderate water-conductivity.

OL_KR6_BFI_11753_11805

Short breakage in sheared veined migmatite. It is located on an old welded microbreccia. Intersection shows fractures parallel to foliation and one fracture in direction of core sample. Kaolinization, in places strong illitization and some graphite. Drilling has an effect on splitting of the core, in places the core sample has splitted to small grains suggesting to some grade of porosity.

OL_KR6_BFI_12322_12945

Veined gneiss and pegmatitic sections. Intersection is multiphase breakage with early stage microfracturing, -breccia and fault, which are healed. Faulting is almost parallel to core sample. Old opened undulating fault is filled with quartz and some dark-coloured euhedral mineral. Later opening of the fault has produced coatings of calcite and some clay mineral (altered calcite?). Strong hydrothermal alteration (silicification, epidotisation, illitisation) has welded the old breakage. Foliation is crosscut also by separate graphite-filled slickenside. Probably drilling has splitted the core sample remarkably. At first stage there was only 1 - 2 filled slickensides.

OL_KR7_BFI_68990_69200

Short breakage with splitted core sample. Intersection is located in mica-rich migmatite inside an intact pegmatite. Above the breakage there is ca. 5 m and below ca. 3 m of unfractured pegmatite. Intersection is joined with porosity and gouge clay. No water-conductivity.

OL_KR7_BFI_69410_70210

Long fractured intersection in mica-prevailing fine-grained gneiss and veined gneiss. Strong illitization is observable on fracture surfaces. Majority of fractures are illite-coated slickensides, most often parallel to foliation, but also crosscutting fractures are found. Illite occurs mostly as nematoblastic crystals.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Contradictory kinematic information

Fault

Gently dipping, semiplanar feature. Dip/dip direction c. 30 – 40/160 – 170

INTERSECTIONS OL_KR1_BFI_52520_52620 OL_KR11_BFI_62502_62647 OL_KR12_BFI_58240_58410 OL_KR13_BFI_44550_46800 OL_KR19_BFI_25335_25982 OL_KR2_BFI_50404_50795 OL_KR20_BFI_44963_45264 OL_KR29_BFI_84830_85197 OL_KR33_BFI_27591_28043

APPENDIX 3 319

OL_KR33_BFI_28678_28815 OL_KR4_BFI_75770_76270 OL_KR5_BFI_26945_27068 OL_KR5_BFI_27897_28244 OL_KR6_BFI_11753_11805 OL_KR6_BFI_12322_12945 OL_KR7_BFI_68990_69200 OL_KR7_BFI_69410_70210

BASIS FOR INTERPRETATION

CONFIDENCE

Mise-a-la-masse, drillhole intersections

2 Moderate (0= very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR1: 512.00 – 527.00 Rp1-0 OL-KR1: 525.65 – 526.14 RiIII

OL-KR2: 503.65 – 513 Rp0-1 OL-KR2: 506.68 – 507.12 RiIII

OL-KR5: 128 – 270 Rp0, 270 – 279.50 Rp1, 279.50 – 283.00 Rp2 OL-KR5: 269.38 – 270.63 RiIII, 278.19 – 283.00 RiIII

OL-KR6: 4.80 – 300.62 Rp0(1) OL-KR6: 124.10 – 129.45 RiIII

OL-KR11: 625.00 – 626.50 Rp1 OL-KR11: 624.82 – 626.39 RiIII (IV)

OL-KR12: 580.00 – 584.28 Rp0-1 OL-KR12: 581.53 – 584.02 RiIII

OL-KR13: 445.21 – 451.69 Rp0, 451.69 – 455.69 Rp0-1, 455.69 – 463.26 Rp0, 463.26 – 463.85 Rp0-1, 463.85 – 490.90 Rp0 OL-KR13: 451.04 – 451.84 RiIII, 454.34 – 454.97 RiIII, 457.33 – 459.23 RiIII

OL-KR19: 248.43 – 259.63 Rp1, 259.63 – 262.96 Rp0-1 OL-KR19: 253.64 – 254.00 RiIV, 259.01 – 259.63 RiIV

OL-KR20: 443.80 – 463.20 Rp0(1)

OL-KR29: 847.60 – 849.26 Rp1, 849.26 – 849.52 Rp2-3, 849.52 – 852.00 Rp1 OL-KR29: 849.26 – 849.52 RiV, 851.45 – 851.81 RiIV

OL-KR33: 275.00 – 275.90 Rp1, 275.90 – 276.30 Rp2-3, 276.30 – 279.30 Rp1-2, 279.30 – 286.60 Rp1(Rp2) OL-KR33: 275.91 – 276.22 RiV, 276.22 – 280.42 RiIII, 282.13 – 283.10 RiIII, 286.63 – 288.13 RiIV

APPENDIX 3 320

COMPARISON TO BEDROCK MODEL 2003/1

KR01_5RH KR02_6R RH21 (OL-KR4, OL-KR11) R2 (OL-KR5, OL-KR19) KR07_10R KR12_15R KR13_10R

UPDATES - version history V 0 FILE Zone2.dtm

COMPILATION DATE AND COMPILED BY

21.12.2005 Markku Paananen

APPENDIX 3 321

ID OL-BFZ100

DIMENSIONS X/Y/Z, m

37/340/100

DESCRIPTION OL_KR25_BJI_9445_9730

The intersection is composed of VMGT. The intersection contains old and welded fractures where pyrite and some calcite are present. These old fractures have partly been reopened during drilling. The rock has a clear foliation and the fracturing follow it. All the fractures have a NE-SW direction and a moderate dip. The intersection contains 21 joints, ca. 7 fractures / m. The rock is weathered, crushed and altered in section 96.35-96.66. The section also exhibits clear water conductivity signs. Some mechanical fracturing has occurred during the drillings.

OL_KR26_BJI_9580_9825

The intersection is composed of DTX. The intersection contains old and welded fractures where calcite is present. These old fractures have partly been reactivated later. The fractures seem to have a random direction but no certainty could be established because of absent Wellcad picture. The intersection contains 28 joints. The rock is most fractured in section 97.24-97.64, exhibiting 14 fractures. The water conductivity measurement was not carried out at this depth. Some mechanical fracturing has occurred during the drillings.

OL_PH1_BFI_15164_15432

The intersection is composed of heterogeneous and altered PGR with biotite-rich schlieren. The feldspars are mainly altered to chlorite and sericite. A majority of the fractures contain chlorite and some have a light greenish clay filling, indicating water flowing, although no flow measurements were carried out this part of the borehole. The intersection contains 34 fractures. A few old and welded fractures with calcite fillings occur. 3 fractures with slickenside surface are present. Due to absent Wellcad picture and base line no directions have been measured, but some of the fractures have foliation parallel direction. Mechanical fracturing has occurred during the drilling.

OL-TK7_P8_BFI_347_P8_400

Brittle fault zone with calcite and chlorite coated fractures oriented ca. 085/75°

ONK_BFI_12850_12930

Brittle fault intersection which visible across the whole tunnel and has a trace length of approximately 15-20 meters. The fault plane has an average dip/dip direction of 70/115. The width of the zone is at the tunnel roof approximately 4 meters but in the lower part of the tunnel, fault planes combine into an intersection with an width of 20 cm. The fault has partly a semi-brittle character as calcite-filled tension veins can be observed. Fault crosscuts foliation. Lineation has a plunge/trend of 11/044 and is visible in some of the fractures (STRIA, STEP, PSGR). These two features show a following sense-of-movement;

U=LS=RE=R

APPENDIX 3 322

The fault has a thin core of a width of 5-10 cm and which contains of crushed rock (pieces up to 20 mm in diameter) and gray-greenish clay/silt. The core can be defined as fault breccia, as most of the material consists of rock pieces (70-80%). In places the core material show strong tectonic fabric, which could be defined even as schistosity.

Within the fault pyrite, chalcopyrite, galena and graphite mineralisations are common. Chalcopyrite seems to be associated with calcite-filled fractures/tension veins.

The intersection is moist.

Main rock type is veined migmatite.

ONK_BFI_52150_52300

Brittle fault intersection that has about ten slickensided fractures with clear lineation. A core can be defined for the fault intersection and it has a width of approximately 5-25cm. The core consist of fault breccia containing crushed rock pieces, the rock pieces are 0.001- 4 cm in diameter. The core contains also clay which is greyish black in colour. Within the core, lenses that are approximately 5-35cm wide can be observed. Lenses have dip/dir 89/284 and 86/098. The surrounding rock is VGN. There are also some fractures with cc and sk infillings. Fracture with dip/dip direction of 89/284. Lineation 14/012. There are some fractures on the left side of the zone but there are no fractures on the right side of the zone. The roof of the tunnel is wet and the walls of the tunnel are damp.

OL_TK11_BFI_C20_S25

The eastern part of the trench is intersected by a continuous fracture zone, which can be defined as brittle fault based on observed kinematic indicators. The trace length of the fault is approximately 50 meters and it has an average trace direction of 015°. The average dip and dip direction of the fault plane are 65° and 110°, correspondingly. The continuity of the fault outside the trench area is unknown but the visible part of the fault runs through mapping sections C20 and S25. The fault splays into two different fault planes in the southern part of the investigation trench but the continuation of the secondary fault plane is also unknown. The fault consists of a clearly definable core and transition zone; the core has a varying width of 0.15 to 2 metres and has in places strongly developed schistose fabric with associated slickensided surfaces. Quartz, pyrite, chalcopyrite, graphite, galena and talc mineralisations can be observed within the fault core. Pyrite mineralisation occurs within cavities associated with quartz-filled tension veins. In squares E21 and E22, where the fault splays into two different planes, the rock is strongly broken by intensive fracturing.

The transition zone forms an area where the fracture density is higher than in the rest of the excavated area. The width of transition zone varies and cannot be explicitly measured, as it seems to continue outside the trench area on the eastern side of the fault core. Nevertheless, on the western side of the fault, the transitional area with higher fracture density has a varying width of 2 to 6 meters. In addition to the higher fracture density, the transition zone is also characterised by long, planar and vertical synthetic and anthithetic secondary Riedel-fractures (R- and R’-fractures, correspondingly)

The fault shows sinistral sense of movement by numerous kinematic indicators. In the core of the fault, in sections O24 and P24, quartz-filled tension veins show clear sinistral vergeance in horizontal plane. The fault also

APPENDIX 3 323

crosscuts older, east-west trending ductile shear zone, which shows sinistral deflection towards the fault core. Based on the crosscutting relationship and the amount of deflection of the older shear zone it can be estimated that within the fault the sinistral horizontal movement has been at least 2 meters. Sinistral sense of shear is also supported by the existence of planar secondary Riedel shear fractures or R-fractures, which form an approximate angle of 15 to 25 degrees (trace of 160-170 degrees) to the fault core, or the P-shear plane. Planar R’-fractures, which are less developed than the R-fractures, have an approximate angle of 5-15 degrees (trace of 110-120 degrees) to the main fault plane.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Sinistral strike-slip fault, small component of normal dip-slip movement

U=LS=RE=R

Steeply dipping, branching and slightly tortuous feature. Dip/dip direction c. 55 – 70/090 – 120.

INTERSECTIONS OL_KR25_BJI_9445_9730 OL_KR26_BJI_9580_9825 OL_PH1_BFI_15164_15432 OL-TK7_P8_BFI_347_P8_400 ONK_BFI_12850_12930 ONK_BFI_52150_52300 OL_TK11_BFI_C20_S25

BASIS FOR INTERPRETATION

CONFIDENCE

Drillhole intersections, surface mapping, ONKALO intersections

3 High (0= very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

OL-KR25: 69.40 – 96.10 Rp0-1, 96.10 – 96.70 Rp1-2, 96.70 – 113.40 Rp0-1 OL-KR25: 96.09 – 96.73 RiIII

OL-KR26: 95.10 – 98.00 Rp1, 98.00 – 100.80 Rp0 OL-KR26: 96.82 – 97.90 RiIII-IV

COMPARISON TO BEDROCK MODEL 2003/1

-

UPDATES - version history V 0 FILE Zone3.dtm, ‘Storage Hall’ fault

COMPILATION DATE AND COMPILED BY

5.1.2006 Markku Paananen

20.1.2006 Additions (ONK_BFI_12850_12930,ONK_BFI_52150_52300, OL_TK11_BFI_C20_S25) Jussi Mattila

APPENDIX 3 324

ID OL-BFZ101

DIMENSIONS X/Y/Z, m

70/24/14

DESCRIPTION ONK_BFI_7000_7190 Brittle fault intersection which visible across the whole tunnel and has a trace length of more than 40 meters. The fault plane has an average dip/dip direction of 10/151. The width of the zone is approximately 2 meters. The fault has partly a semi-brittle character as the foliation near the fault shows well-developed deflection and thus indicating that the hanging wall of the fault has moved towards west (reverse fault). The fault plane crosscuts the foliation. Accordingly, sense-of-movement viewed from south is sinistral; due to lack of viewing planes, the movement in other dimensions is unknown:

U=? S=L (sinistral) E=?

The fault has a well developed core of width of 10-30 cm and which contains of intensively crushed rock (0.1-30 mm in diameter) and greenish clay. The core can be defined as fault breccia, as most of the material consists of rock pieces (70-80%). The fault has also an intensively altered “transition intersection” in which the rock is quite homogenous K-feldspar porphyric tonalite/granodiorite; the K-feldspar phenocrysts are 5-50 mm in diameter and are both eu- to subhedral. The width of this K-feldspar porhyritic zone is 20 cm:s to 2 meters in the hanging wall and approximately 1 meter in the footwall. The zone has gradational contacts to veined migmatite, which is the main rock type of the fault area.

The fault breccia is moist and partly also dripping.

Small-scale D3-folding can be observed in the near vicinity of the fault.

OL-PH1_97.77 _ 99.85

At 98.65 a 1.05 m loss of drill core has occurred, rods dropped several times during the drillings, some hard rock pieces between loose sections (silty clay). The surrounding rock is a heterogeneous and altered K-Feldspar Porphyry. The K-Feldspars are partly sericitised and has a yellowish colour.

OL-PP40 17.85 – 18.53 OL-PP41 27.10 – 27.89 OL-PR5 4.24 – 4.64 OL-PR6 5.55 – 6.00 OL-PR7 7.56 – 8.09 OL-PR8 11.90 – 12.30

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

Brittle fault zone

Reverse fault when viewed from south

S=L

Subhorizonta, undulating feature. Dip/dip direction c. 11/116.

APPENDIX 3 325

INTERSECTIONS ONK_BFI_7000_7190 OL_PH1_97.77 _ 99.85

OL-PP40 17.85 – 18.53

OL-PP41 27.10 – 27.89

OL-PR5 4.24 – 4.64

OL-PR6 5.55 – 6.00

OL-PR7 7.56 – 8.09

OL-PR8 11.90 – 12.30 BASIS FOR INTERPRETATION

CONFIDENCE

Borehole intersections, GPR, ONKALO intersection

3 High (0= very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

ONK-PH1 98.05 – 99.76 RiV OL-PP40: 17.95 – 18.55 RiIII OL-PP41: 27.10 – 28.75 RiIII OL-PR6: 5.50 – 6.00 RiIII OL-PR8: 11.90 – 12.30 RiIII

COMPARISON TO BEDROCK MODEL 2003/1

-

UPDATES - version history V 0 FILE Zone4.dtm

COMPILATION DATE AND COMPILED BY

5.1.2006 Markku Paananen 20.1.2006 Jussi Mattila – Additions: ONK_BFI_7000_7190 OL-PH1 97.77 – 99.85

APPENDIX 3 326

ID OL-BJZ102

DIMENSIONS X/Y/Z, m

314/379/111

DESCRIPTION ONK_DSI_24000_28230

VGN with 20-60cm wide PGR dykes. Ductile shear zone intersection. Sheared and altered zone, the clearest alterations are visible in the kaolinisation of feldspar grains and chloritisation of biotite. Rotation is visible in the feldspar grains. The direction of shearing is 47/125, which is same as the direction of the foliation. The intersection is visible across the whole tunnel. In some parts there is strongly sheared and mylonitised sections. Plenty of pale kaoline veins/grains.

There is one clear vertical fracture, which branches to shorter joints in some parts the main orientation of the joint is 25/39. On the right tunnel wall fracture begins from 242m, +2m and it ends to 267m in the left tunnel wall, fracture ending is not visible in the right wall because of the shotcrete. It seems that in the right wall there is horizontal sinistral movement related to this fracture. The thickness of the fracture varies 10-60mm and the colour of the fracture infilling is greenish consisting of unidentified clay mineral and chlorite.

There are a lot of short fractures in the ductile zone

ONK_DSI_44970_45330

VGN and SGN. Ductile shear zone intersection. Sheared and altered zone. The rock is intensively kaolinitised. In the centre of this intersection there is a strongly sheared zone, the width of this zone varies 30-100mm. This sheared zone is greenish and composed of chlorite, biotite, kaolinite and unidentified clay mineral. Some sand fragments are also present. The direction of shearing is 56/158, which is same as the direction of the foliation. The intersection is visible across the whole tunnel. The surrounding rock is also pervasively kaolinitised and has some rotated grains. One undulating slickensided fracture with an uncertain lineation (24/240) is also present.

There are a lot of short fractures in the ductile zone

Weathered and strongly fractured zone KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE Moderately dipping, curving feature. Dip/dip direction c. 40-60/110-170.

INTERSECTIONS ONK_DSI_24000_28230 ONK_DSI_44970_45330

BASIS FOR INTERPRETATION

CONFIDENCE

Mapping observations on the ground surface and in ONKALO, mise-a-la-masse

2 Moderate (0= very low, 1=low, 2=moderate, 3=high)

APPENDIX 3 327

HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION COMPARISON TO BEDROCK MODEL 2003/1

OL-KR4 115.6 – 117.6: RH19B?

UPDATES - version history V 0 FILE Zone5.dtm

COMPILATION DATE AND COMPILED BY

9.1.2006 Markku Paananen

APPENDIX 3 328

ID OL-BFZ103

DIMENSIONS 174 m in N-S-direction 102 m in W-E-direction

DESCRIPTION OL_KR8_BFI_30393_30675

Chlorite-, calcite- and illite-coated fractures at dept of 303.93 - 304.65 m. In places the feldspars of granitic veins in mica gneiss are greenish due to strong illitization. Quartz vein in the altered and fractured intersection between 304.80 - 305.60 m shows cavities, which are filled by some mineral (quartz?). Many slickensides almost parallel to core sample between 305.60 - 306.00. In the bottom of the intersection there is one water-conductive fracture.

KINEMATICS OF THE ZONE – IF POSSIBLE

ORIENTATION/GEOMETRY OF THE ZONE

GROUP B

U=LE=RS=R

Left-normal fault

Average dip/dip direction 61/097. Mean fault vector orientation 24/021.

INTERSECTIONS OL_KR8_BFI_30393_30675

BASIS FOR INTERPRETATION

CONFIDENCE

Drill hole intersection, kinematics

0 (0= very low, 1=low, 2=moderate, 3=high) HYDROLOGICAL FEATURES

To be added later

IMPLICATIONS TO CONSTRUCTION

303.93-305.97 m RiIII

COMPARISON TO BEDROCK MODEL 2003/1

No matches found

UPDATES - version history V 0 FILE group_b_11.dtm

329 APPENDIX 4

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338

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348

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354

355 APPENDIX 4