Geological Mapping of Investigation Trench OL-TK18 at the Olkiluoto Study Site ... ·...
Transcript of Geological Mapping of Investigation Trench OL-TK18 at the Olkiluoto Study Site ... ·...
POSIVA OY
FI-27160 OLKILUOTO, FINLAND
Tel +358-2-8372 31
Fax +358-2-8372 3709
Jon Engström
Apri l 2012
Working Report 2012-18
Geological Mapping of Investigation TrenchOL-TK18 at the Olkiluoto Study Site,
Eurajoki, SW Finland
Apri l 2012
Working Reports contain information on work in progress
or pending completion.
Jon Engström
Geological Survey of F inland
Working Report 2012-18
Geological Mapping of Investigation TrenchOL-TK18 at the Olkiluoto Study Site,
Eurajoki, SW Finland
Base maps: ©National Land Survey, permission 41/MML/12
GEOLOGICAL MAPPING OF INVESTIGATION TRENCH OL-TK18 AT THE OLKILUOTO STUDY SITE, EURAJOKI, SW FINLAND
ABSTRACT Geological mapping of investigation trench OL-TK18 was carried out by the Geological Survey of Finland at the Olkiluoto study site, Eurajoki, as part of Posiva Oy’s site investigation programme for the development of an underground repository for nuclear waste. The E-W striking, ca. 55 m long trench is located in the central part of the Olkiluoto Island adjacent to investigation trenches OL-TK12 and OL-TK4. The trench was cleaned with a pressure washer and pressurized air. The rock types were determined macroscopically. The rock types in investigation trench OL-TK18 is of heterogeneous character, with a large variation in their composition. The rocks vary from tonalitic-granodioritic gneiss to diatexitic gneiss, with portions of K-feldspar porphyritic gneiss. Inclusions of mica gneiss and a well-preserved schollen migmatite is encountered. The trench ends in a feldspar-rich pegmatoid. The most dominant tectonic feature is D4 ductile deformation domain and associated S4 foliation. This domain and hence the S4 foliation is striking NE-SW with a moderate dip towards SE. Both ends of the trench are dominated by the earlier deformation phase, showing S3 foliation striking ENE-WSW and roughly dipping towards the S. The S3 foliation is associated with small-scaled granitic leucosome veining, while the S4 foliation have a schistose character and it is more sheared. D4 ductile deformation domain is also characterised by a sheared blastomylonitic rock having growth of roundish feldspar porphyroblasts and BT-schlierens indicating high alteration of the protolith. During the fracture mapping, all fractures intersecting the central thread were investigated and a total of 117 fractures were recorded. The average fracture frequency of the trench is 2.11 fractures/m. On the basis of fracture orientations one main set can be distinguished striking NE-SW (foliation parallel) with a moderate dip towards the SE. The median fracture trace length is 1.6 m and over half of the fractures exceed 1.5 m trace length, the longest measured fracture being 7.90 m. Fracture fillings include hematite, chlorite, biotite and muscovite. A few fracture surfaces also contain calcite, clay, pyrite, quartz, and illite. The thickness of the fillings varies between 0.1 – 60 mm and the average thickness is 1.7 mm. The trench contains two big faults, one with a distinct fault core of quartz, calcite and chlorite, and having a NW-SE strike and a moderate dip towards the NE. The other one is parallel to the D4 ductile deformation domain, having a NE-SW strike and a moderate dip to the SW, showing totally altered and sheared rock. A Q-classification for the investigation trench has been made for every mapping section and the quality varies from good to exceptionally good. The average Q-quality of the rocks is exceptionally good, indicating that no major brittle deformation zone intersects the trench. Keywords: Investigation trench, rock types, D4 ductile deformation domain, S3 and S4 foliation, fracturing, nuclear waste disposal, Olkiluoto.
EURAJOEN OLKILUODON TUTKIMUSKAIVANNON OL-TK18 GEOLOGINEN KARTOITUS
TIIVISTELMÄ Osana Olkiluodon sijoituspaikkatutkimuksia Geologian tutkimuskeskus teki Posiva Oy:n tilauksesta tutkimuskaivannon OL-TK18 geologisen kartoituksen kesäkuussa 2010. Tutkimuskaivanto OL-TK18 sijaitsee Olkiluodon tutkimusalueen keskiosassa, kaivantojen OL-TK12 ja OL-TK4 vieressä. Kaivanto on itä-länsi-suuntainen ja sen pituus on noin 55 m. Kartoitus tehtiin paineilmalla ja painepesurilla puhdistetulta kalliopinnalta. Pääkivilajit määritettiin makroskooppisesti kartoituksen yhteydessä. Kaivannossa ei ole selvää pääkivilajia, vaan se vaihtelee diateksiittisen gneissin, tonaliitti- granodioriittigneissin, K-maasälpäporfyyriin ja pegmatiittisen graniitin välillä. Kaivannosta löytyy myös hyvin säilynyt schollen-migmatiitti, jota aiemmin on havaittu vain ONKALOn tutkimustunnelista ja muutamilla yksittäisillä paljastumilla. Myös pari isompaa kiillegneissisulkeumaa havainnoitiin kartoituksen yhteydessä. Hallitsevin duktiili rakennepiirre on S4-liuskeisuus ja siihen liittyvä duktiili deformaatiovyöhyke, joka on hallitsevin piirre kaivannon keskiosassa. Tämä vyöhyke ja siihen yhdistyvä S4-liuskeisuus on koillis-lounas-suuntainen ja sen kaade on kohti kaakkoa. Kaivannon molemmissa päissä liuskeisuuden suunta muuttuu ja itäkoillis-länsilounas-suuntainen ja etelään kaatuva S3-liuskeisuus on hallitseva. S3-liuskeisuuden erityspiirteenä ovat graniittiset leukosomisuonet gneisseissä, kun taas S4-liuskeisuudessa on korkeampi hiertymisaste. Toisena erityspiirteenä ovat maasälpäporphyroblastit ja biotiitti-schlierenit jotka ovat tyypillisiä tunnusmerkkejä tästä viimeisestä duktiilideformaatiosta Olkiluodon tutkimusalueella. Kartoituksessa mitattiin kaikki raot, jotka leikkasivat kaivannon ylle pingotetun linjalangan. Rakojen kokonaismäärä oli 117 rakoa ja keskimääräinen rakotiheys 2,11 rakoa/m. Rakosuuntien perusteella yksi ryhmä hallitsee ja se on koillis-lounas-suuntainen ja kaade on kohti kaakkoa (liuskeisuuden suuntainen). Rakojen mediaani pituus on 1,6 m ja yli puolet raoista on yli 1,5 m pitkiä, pisin mitattu rako on 7,90 m. Rakotäytteitä ovat hematiitti, kloriitti, biotiitti ja muskoviitti. Muutamista raoista löytyy myös kalsiittia, savea, rikkikiisua, kvartsia ja illiittiä. Täytteiden paksuus vaihtelee 0,1 – 60 mm ja keskimääräinen paksuus on 1,7 mm. Tutkimuskaivannosta kartoitettiin kaksi isompaa haurasta siirrosta. Toinen niistä on luode-kaakko-suuntainen (kaade kohti koillista) ja toinen on duktiilin deformaatio-vyöhykkeen suuntainen, siis koillis-lounas-suuntainen. Ensimmäisessä siirroksessa on paksu kvartsitäyte, kun taas toisen siirroksen pinta on hiertynyt ja kivi on vahvasti muuttunut. Kaivannon jokaiselle paaluvälille arvioitiin Q-luokituksen mukainen kallio-laatu ja sen perusteella kaivannon kalliolaatu vaihtelee hyvästä poikkeuksellisen hyvään. Keskimääräinen Q-laatu on poikkeuksellisen hyvä, mikä tarkoittaa sitä, että isoja hauraita siirrosvyöhykkeitä ei kaivannosta havaittu. Avainsanat: Tutkimuskaivanto, kivilajit, D4 duktiili deformaatiovyöhyke, S3- ja S4- liuskeisuus, rakoilu, ydinjätteiden loppusijoitus, Olkiluoto.
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TABLE OF CONTENTS ABSTRACT TIIVISTELMÄ 1 INTRODUCTION .................................................................................................... 2 2 RESULTS OF INVESTIGATIONS .......................................................................... 5
2.1 Lithology ........................................................................................................ 5 2.2 Ductile deformation ....................................................................................... 9
2.2.1 High-grade ductile shear zone Intersection (HGI) ........................... 12 2.3 Brittle deformation ....................................................................................... 13
2.3.1 Fracture orientation data ................................................................. 13 2.3.2 Fracture frequencies ....................................................................... 16 2.3.3 Fracture characteristics ................................................................... 17
2.4 Rock mass quality (Q-classification) ........................................................... 21 3 SUMMARY ........................................................................................................... 22 REFERENCES ............................................................................................................. 23 APPENDICES ............................................................................................................... 24
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1 INTRODUCTION
Investigation trench OL-TK18 is located in the central part of the Olkiluoto study site adjacent to the investigation trenches OL-TK12 and OL-TK4 (Fig. 1-1). The trench has an E-W direction with a total length of 55.4 m and a width from 1 to 3 m. The trench was divided into 10 mapping sections (P1-P10) for the mapping purpose. The bedrock is close to the quaternary surface throughout the trench and the deepest parts are only a few meters deep. The purpose of the trench was to locate a brittle deformation zone OL-BFZ045 at surface, which was detected in the ONKALO research tunnel at chainage PL3333-3350, but also to investigate a geophysical mise-à-la-masse survey signature (Fig. 1-2). During the mapping every bolt (P1-P10) were given a detailed coordinate, thus x-, y-, and z-coordinates, giving starting and end points for every section. The location of each observation was determined by using a straight thread, which was extended and tightened over each mapping section, and measuring the horizontal distance from the starting point of the section to the observation point as well as the vertical distance from the thread to the observation point. Knowing the coordinates of the starting and end point of the section, the location of the observation point in the x-y-z coordinate system can be calculated. The rock types were determined macroscopically from the bedrock surface, which was cleaned with pressured air and water. The general mapping was performed using the standard operating procedures and guidelines of the Geological Survey of Finland (GTK) for the bedrock mapping (GTK Guide for bedrock mapping KPK3-O1). The structural investigations, however, were carried out using Posiva’s standard form for the ONKALO tunnel mapping, which was slightly modified for the investigation trench purpose. Investigations of the ductile deformation included measurements of foliation (deformation phase, type and intensity), lineation (slickenside), fold axis and axial planes. During the fracture mapping, all the fractures intersecting the central thread were investigated and in addition all fractures over 1 m in trace length were investigated from the whole trench area. Dip direction and dip, spacing (if more than one fracture had the same direction), length, filling (thickness), aperture, type (ends, joins or continues), undulation and rock type were determined for each fracture. A determination for the Jr (a value indicating roughness of joint surface) and Ja (a value indicating the degree of alteration or clay filling in the joint) values of the Q-system were also carried out for each fracture. A total of 94 fractures and fracture clusters were investigated. To obtain an accurate amount of fractures, all fractures in fracture clusters were added to the total tally, and this resulted in a total of 117 fractures for the trench. The measured fractures and other tectonic features are listed in Excel-tables in Appendix 2. The files were delivered to the POTTI database of Posiva and the original hand-written observations to Posiva’s archive. Orientations of structural elements are displayed using Fisher equal-area, lower hemisphere stereographic projection. The 5 declination has been added to the stereographic projections, but not to the original data gathered in Appendix 2. The investigation trench was also documented with digital photographs (Fig. 1-3). The photographs were stored into Posiva’s archive.
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Figure 1-1. Map illustrating the location of all investigation trenches at the Olkiluoto Island. OL-TK18 is highlighted by a red circle.
Figure 1-2. Map illustrating the location of the mise-à-la-masse survey (violet circles) and possible ground surface projection of a brittle zone (OL-BFZ045) detected at chainage PL3333-3350 in the ONKALO access tunnel (orange lines, location modelled using ground magnetic data).
OL-TK18
0 250 500 750 1 000125Meters
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Figure 1-3. General photo of the investigation trench OL-TK18. A view from mapping section P8 towards the west.
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2 RESULTS OF INVESTIGATIONS
2.1 Lithology
The rock types in the investigation trench OL-TK18 are of heterogeneous character, with a variation from tonalitic-granodioritic gneiss (TGG) to diatexitic gneiss (DGN), with portions of K-feldspar porphyritic gneiss (KFP). Inclusions of mica gneiss (MGN), quartz gneiss and skarn are also present throughout the trench. A few coarse-grained pegmatitic granite dykes (PGR) are also encountered. The trench ends in a feldspar-rich leucosomatic pegmatoid (PGR). The rock types are presented on a map in Appendix 1. Posiva’s practice of naming rocks, which has been used in this study, is introduced in Mattila (2006). The rock types are described in the summary report of the petrology of Olkiluoto (Kärki & Paulamäki 2006). The gneisses of Olkiluoto commonly have a migmatitic appearance and therefore the descriptive terminology (Wimmenauer & Bryhni 2002) of migmatites is useful. The leucosome is the leucocratic, lighter-coloured portion of the migmatite with plutonic appearance and the melanosome is the darkest part of the migmatite. The melanosome is here referred to the biotite rich stripes (schlieren) or narrow bands in the migmatite. The mesosome is the mesocratic, intermediately coloured, part of the migmatite with metamorphic appearance (in this case mostly mica gneiss). On the basis of the migmatite structure, the migmatitic gneisses at Olkiluoto can be divided to three groups: veined gneisses, stromatic gneisses and diatexitic gneisses. (Kärki & Paulamäki 2006). The leucosome of the veined gneiss shows vein like, more or less linear traces with some features similar to large-scale augen structures. Planar sheet-like leucosome dykes characterise the stromatic gneisses, whereas the migmatite structure of the diatexitic gneisses is more asymmetric and irregular. The leucosome amount varies from 10 % to over 80 %, the average amount being 20-40 % (Kärki & Paulamäki 2006). The western end of the trench is composed of DGN that consists of TGG paleosome and PGR leucosome (as veins and dykes) (Fig. 2.1-1A). The TGG is medium-grained and probably has a psammitic origin. In the middle of section P2 a pegmatoid with KFP signature prevails, containing clear pegmatitic groundmass and abundant in feldspar porphyroblasts. The rock contains biotite schlieren as melanosome and totally lacks paleosome (Fig. 2.1-1B). The section ends in a MGN inclusion which is approximately 3 m wide and 6 m long. The KFP pegmatoid gradually turns into a schollen-type migmatite in section P4, where the groundmass is a KFP pegmatoid containing BT-schlieren melanosome. The rock contains abundantly angular pieces (20-30 cm long) of MGN/skarn inclusions, which give the schollen character to the rock (Fig. 2.1-1C). The rock type changes gradually into a DGN with TGG paleosome and pegmatitic leucosome in the end of section P4. The DGN rock with TGG paleosome prevails from section P5 into the middle of section P7. The rock is unaltered and the leucosome content is 30-40 %. The veins are ambiguous and irregular in orientation but they are generally quite wide, the width is mostly 20-40 cm, the widest patches are up to 70 cm (Fig. 2.1-2A). After this the rock
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turns into homogenous tonalitic to granodioritic gneiss (TGG) containing small garnets and cordierite porphyroblasts together with a few patches/veins of pegmatite (Fig. 2.1-2B). This rock type ends in the middle of section P8 where a KFP pegmatoid is encountered. The contact between the TGG and the KFP is sheared, altered and densely fractured parallel with to the foliation plane. This rock contains clear pegmatitic groundmass and is abundant in feldspar porphyroblasts, but also some BT-schlieren melanosome is present. The rock is similar to the rock seen in section P3. Section P9 contains a large (ca. 0.75 m wide and 10 m long) MGN inclusion which is rich in mica and densely fractured (Fig. 2.1-2C). The end of the trench (eastern part) is composed of a feldspar-rich pegmatoid which is classified as PGR (see Mattila 2006) even though it’s not a typical pegmatitic granite occurring in Olkiluoto. The rock type has a granitic/granodioritic composition, but it contains feldspar porphyroblasts, which is characteristic of KFP type rocks (Fig. 2.1-2D). These porphyroblasts are generally 2-3 cm wide and 4-6 cm long and contain BT-schlieren in between. The pegmatoid/leucosome material composes approximately 80-90 % of the total rock volume and the rest of the rock contains BT-schlieren melanosome, but occasionally there are significantly more BT-schlieren as seen in Fig. 2.1-2D. This dominating character of the originally granitic/granodioritic composition of the rock is illustrated on a photo in the next chapter, which describes the late ductile deformation (D4) altering and deforming the protolith (Fig. 2.2-4).
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Figure 2.1-1. A) Diatexitic gneiss with TGG paleosome. OL-TK18, mapping section P1. B) KFP pegmatoid with pegmatitic groundmass and abundant in feldspar porphyroblasts. OL-TK18, mapping section P3. C) KFP/Scholllen migmatite with typically angular MGN/skarn inclusions. OL-TK18, mapping section P4. The length of the plate is 16 cm and the measuring stick is 4 m long. Photos by Jon Engström, Geological Survey of Finland.
A B
C
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Figure 2.1-2. A) Diatexitic gneiss with TGG paleosome and PGR neosome. OL-TK18, section P5. B) Tonalitic granodioritic gneiss with cordierite porphyroblasts. OL-TK18, mapping section P8. C) Large MGN inclusion located in a KFP pegmatoid. OL-TK18, mapping section P9. D) KFP pegmatoid with BT-schlieren melanosome and feldspar porphyroblasts. OL-TK18, mapping section P10. The length of the plate is 16 cm and the measuring stick is 4 m long. Photos by Jon Engström, Geological Survey of Finland.
A B
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2.2 Ductile deformation
In the course of Proterozoic tectonic evolution, the metamorphic, mainly supracrustal rocks at Olkiluoto has been subjected to a polyphase ductile deformation. Relicts of lithological layering and a weak foliation created by the first phase of deformation (D1) represent the oldest observed structural elements detected. Second phase (D2) is the most dominant in its entirety and it caused strong migmatitisation associated with intense folding and thrust related ductile shearing. During third deformation phase (D3), the deformed migmatites were again folded and sheared and subareas dominated by D3 structural elements were formed simultaneously with pegmatite-like dykes or migrated leucosomes which intruded mainly parallel to the D3 shear zones and S3 axial surfaces. Subsequently, all earlier structural elements were again re-deformed in fourth deformation phase (D4), which produced close to open folds and small-scaled ductile shear structures (Aaltonen et al. 2010). Based on the occurrence, type and intensity of the products of different deformation phases, Olkiluoto site can be divided into three tectonic sub-domains which are well observable, e.g. on the basis of magnetic map (Aaltonen et al. 2010). These “tectonic units” are bordered by deformation zones in which shear-related structures are important elements. One of these is the E-W striking Selkänummi Deformation Zone (SDZ), a strongly deformed domain in which ductile shear structures are significant elements. Southern border of this zone defines also the southern border of the northern tectonic unit (NTU). In the southern part of the study site, an E-W striking ductile shear zone (Liikla Shear Zone, LSZ) defines the northern border of the southern tectonic unit (STU) and the domain between those is designated as central tectonic unit (CTU). This unit is divided by the NE – SW striking Flutanperä Deformation Zone (FDZ), characterized by D3 deformation phase and by two intensively deformed D4 zones (Aaltonen et al. 2010). The investigation trench is located directly north of FDZ in an area with prevailing D3 deformation, but signs of the D4 deformation are also evident. The observations of the ductile deformation are gathered in Appendix 2. As stated earlier, the rocks of the investigation trench have experienced a multiphase ductile deformation and it is situated in an area were the latest ductile deformation phase, D4 prevails (Fig. 2.2-1). The rocks in the trench have a very heterogeneous character which occasionally shows a distinct foliation, while it at other places is absent. The oldest tectonic feature is the D2 leucosome veining visible in the beginning of the trench (Fig. 2.1-1A), but the oldest foliation seen in the trench is the S3 foliation and associated smaller-scaled granitic leucosome veining. The D3 deformation is the dominant ductile deformation phase in the middle of the Olkiluoto Island and structural elements of the subsequent fourth deformation phase, in many ways resemble the products created by this phase (Aaltonen et al. 2010).
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Figure 2.2-1. Distribution of poles to foliation S3 and S4 in investigation trench OL-TK18 (Fisher equal area, lower hemisphere projection). The main part of the trench is dominated by a domain of D4 ductile deformation, whereas the elements of the earlier deformation phase D3 are situated in both ends of the trench, giving an approximate width of 30 m for the D4 ductile domain (Appendix 1). In Figure 2.2-2 it is evident that the foliation S3 is more ENE-WSW orientated direction whereas the S4 foliation has a NE-SW strike. In addition to this difference in orientation, the different structural signature of these two deformation types is evident in the investigation trench. The S3 foliation is defined by smaller scaled granitic leucosome veining (Fig. 2.2-3A), while the S4 is a sheared, schistose type of foliation, including BT-schlieren and showing a blastomylonitic character (Fig. 2.2-3B). This blastomylonitic type of rock shows growth of roundish feldspar porphyroblasts which is typically associated with D4 fault rocks on the Olkiluoto Island (Aaltonen et al. 2010). Other ductile deformational features (e.g. folding and shear bands) were not encountered in the trench.
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Figure 2.2-2. Foliation sets for the two different deformation phases S3 and S4 in OL-TK18 (Fisher equal area, lower hemisphere projection).
Figure 2.2-3. A) Diatexitic gneiss with small-scale leucosome veining and associated S3 foliation. OL-TK18, section P2. B) KFP pegmatoid with blastomylonitic sheared typical D4 deformed rock and associated S4 schistose type foliation. OL-TK18, mapping section P8. The length of the plate is 16 cm. Photos by Jon Engström, Geological Survey of Finland.
B A
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2.2.1 High-grade ductile shear zone Intersection (HGI)
The middle part of the trench (see Appendix 1) is dominated by a D4 ductile domain or a high-grade ductile shear zone intersection in accordance with the classification developed by Milnes et al. 2007. The width of the zone is approximately 30 m wide (Appendix 1) beginning at mapping section P2 and ending (Fig. 2.2-4) in the beginning of section P10. The zone is characterised mainly by a sheared blastomylonitic rock having growth of roundish feldspar porphyroblasts and BT-schlieren melanosome indicating high alteration of the protolith. These BT-schlierens are together with the S4 schistosity strongly foliated and thus give the orientation for the D4 ductile deformation zone (Fig. 2-2-3B). Although both ends of the zone have typical D4 character, the center part of the zone is different exhibiting a schollen type migmatite (Fig. 2.1-1C) and less sheared rocks such as DGN (Fig. 2.1-2A) and TGG (Fig. 2.1-2B).
Figure 2.2-4. Photo showing the eastern border of the D4 ductile deformation domain, the border of the zone is showing the typical transposition between the D3 and D4 ductile deformation. The measuring stick (white bar) is 4 m long and the picture is approximately orientated with top towards north. Photo by Jon Engström, Geological Survey of Finland.
S4
S3
D4 Ductile domain D3 Ductile domain
Border zone between D3 and D4
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2.3 Brittle deformation
During the fracture mapping, all fractures that intersect the central thread were measured. In addition, fractures with a length of more than 1 m were measured from the entire area of the trench. The results of fracture investigations are shown in Appendix 2. The first six columns show the position of the fracture in relation to the central thread and the calculated x-y-z-coordinates. They are followed by the dip direction and dip, number of fractures, fracture space, fracture length, Jr, Ja, fracture filling and width, aperture, fracture ends, undulation, rock type, water leakage and kinematics. A total of 84 joints and 10 faults were investigated in the trench. Occasionally these joints and faults appear clustered together (thus one observation may represent as many as 6 joints/faults), and these clusters were investigated together, giving total amount of joints/faults to be 117. From this point forward in the report, the joints and the faults will be referred as fractures, regardless of if they show movement or not.
2.3.1 Fracture orientation data
The distribution of all fracture orientations in investigation trench OL-TK18 is shown in Fig. 2.3-1 as Fisher equal area, lower hemisphere projection.
Figure 2.3-1. Distribution of poles to fractures in OL-TK18 (Fisher equal area, lower hemisphere projection).
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On the basis of orientations of all measured fractures one main set can be distinguished (Fig. 2.3-2). This set covers 32 % of all measured fractures, and it strikes NE-SW with a moderate dip towards the SE (Set 1). The occurrence of this fracture set is explained by the D4 ductile deformation domain that is natural environment for the development of these fractures, following the foliation of the domain. Two other less distinct sets can also be extracted from the stereographic plot. They show a more vertical dip, one trending NW-SE with a sub-vertical dip towards NE (Set 2) and another trending NE-SW with a vertical dip (Set 3) (Fig. 2.3-2). The fracturing resembles the characteristic fracturing for diatexitic gneisses; this rock type occurs mainly in areas where the D3 and D4 ductile deformation is prevailing, mostly encountered in the SE part of the Olkiluoto site (Aaltonen et al. 2010).
Figure 2.3-2. Contour plot visualizing the main fractures set in OL-TK18 (Fisher equal area, lower hemisphere projection). There are no noticeable differences between fault and joint orientations in the trench. In fact almost all faults are in the same direction as the S4 foliation parallel joints (Fig 2.3-3). Only two faults have a different orientation one E-W orientated with sub-vertical dip towards the south and one striking NW-SE with moderate dip towards the NE. This latter fault is a big fault with a distinct, up to 6 cm thick, fault core of quartz, calcite and chlorite. On the side of the fault there is an alteration zone showing microbreccia (Fig. 2.3-4A). Another big fault is encountered in the middle of the D4 ductile deformation domain sub-parallel with the foliation, having a NE-SW strike and a moderate dip to the SW. The width of the fault is approximately 50 cm, showing totally altered and sheared rock (Fig. 2.3-4B). On the fault surface illite and other clays, which could not be indentified, were also observed.
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Figure 2.3-3. Pole plot visualizing all faults in OL-TK18 (Fisher equal area, lower hemisphere projection).
Figure 2.3-4. A) Photo showing the major fault in mapping section P2 with a thick (6 cm) fault core of quartz. The long side of the compass is ca 11 cm long and the picture is approximately orientated with top towards north. B) Photo showing the major fault in mapping section P4 with an ambiguous fault core of sheared and altered rock, with some clay. The long side of the compass is ca 11 cm long and the picture is approximately orientated with top towards south-east. Photos by Jon Engström, Geological Survey of Finland.
B A
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The majority of all the fractures show no indications of fault movement and although 20 faults were found in the trench only three had striations that could be measured. All these measurements are plunging moderately towards ESE (Fig. 2.3-5). All these measurements are from faults striking NE-SW and dipping to the SE, located in the large MGN inclusion in section P9 (Fig. 2.2-4).
Figure 2.3-5. Corrected fault-slip data from all faults with visible movement within TK-18, shown as an Anglier-plot (equal-area, lower hemisphere projection).
2.3.2 Fracture frequencies
The fracture frequencies of the investigation trench in each mapping section are presented in Fig. 2.3-6. 94 fractures were investigated in detail from the trench. As stated above a few of these measurements were fracture clusters and to get the total amount of fracturing these were added to total tally. This gives a total of 117 fractures, which has been used as basis for determining the fracture frequency (fractures/m). Accordingly, the average fracture frequency for the 55.43 m long trench is 2.11 fractures/m. The significantly more frequent fracturing observed in section P9 compared to the rest of the trench is due to a the large MGN inclusion intersecting the trench, as these inclusions typical have a higher fracture frequency and the same trend has also been observed in the ONKALO research facility.
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OL-TK18 Fracture frequency
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Figure 2.3-6. Fracture frequencies of the bedrock in sections P1-P10 of OL-TK18.
2.3.3 Fracture characteristics
Fracture lengths were measured from 117 fractures, including fracture clusters. The fracture length in fracture clusters was specified as an estimated average length of all fractures in the cluster. The width of the mapped area was commonly less than 2.5 m and this restriction have affected the lengths recorded for the fractures. The fracture length distribution is compiled and shown in the histogram in Fig. 2.3-7. 7.7 % of all fractures are less than 0.5 m in length, 37.6 % are 0.5-1.5 m in length and 54.7 % of the fractures are longer than 1.5 m. The median fracture trace length is 1.60 m and the longest measured fracture is 7.90 m.
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Histogram, OL-TK18
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0.1 0.3 0.5 0.7 0.9 1.1 1.3 1.5 1.7 1.9 2.1 2.3 2.5 2.7 2.9 3.1 3.3 3.5 3.7 3.9 4.1 4.3 4.5 4.9MoreBin
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60.00 %
80.00 %
100.00 %
120.00 %
Frequency Cumulative %
Figure 2.3-7. Fracture length distribution as histogram for the bedrock investigation trench OL-TK18. Approximately half (54.8 %) of the investigated fractures contained no identifiable mineral fracture fillings, which can be explained by the surface proximity and that some of the fillings probably have been washed away during the excavation of the trench. Mineral fillings observed on fracture surfaces are mostly hematite, but also chlorite biotite and muscovite is found. Less common are calcite, pyrite, clay and quartz (Fig. 2.3-8). The thicknesses of the fillings vary between 0.1-60 mm, the average thickness being 1.66 mm and the median thickness 0.30 mm. The distribution of the fracture filling thickness is shown in Fig. 2.3-9. The aperture of the open fractures varies from 0.1-45 cm, commonly being between 1-2 centimeters. All fractures were classified applying the Q-classification scheme (Barton 1974; Grimstad & Barton 1993) and the description of the various Q-parameters is found in Appendix 3. This scheme is described in detailed in the next chapter but the fracture profile describing the surface and the shape of the fracture is illustrated in Fig. 2.3-10. Slightly more than half of all fractures are undulating or stepped, where the undulation varies between 2-25 cm/m and mostly being 2-5 cm/m. The fractures mainly have rough surfaces (62.4 %), some smooth and slickenside fractures are also present in even amount (Fig. 2.3-10). Only a few stepped fractures were observed in the trench, whereas water-conducting fractures were absent.
19
Fracture filling distribution, OL-TK18
47
19
13 13
2 2 1 1 10
5
10
15
20
25
30
35
40
45
50
Hematite Chlorite Biotite Muscovite Calcite Pyrite Clay Illite Quartz
Num
ber
of fr
actu
res
Figure 2.3-8. The distribution of fracture fillings in OL-TK18.
Fracture filling thickness, OL-TK18
63
41
11
2
0
10
20
30
40
50
60
70
No filling 0.1-0.5 >0.5-1 >1-60
Filling thickness (mm)
Num
ber o
f fra
ctur
es
Figure 2.3-9. The distribution of fracture filling thickness in OL-TK18.
20
Fracture Profile Distribution, OL-TK18
9
13
32
11 10
36
0 1
5
0
5
10
15
20
25
30
35
40
PSL PSM PRO USL USM URO SSL SSM SRO
P=Planar, U=Undalating, S=Stepped and SL=SLickenside, SM=SMooth, RO=ROugh
Num
ber o
f fra
ctur
es
Figure 2.3-10. The fracture profile distribution observed in OL-TK18.
21
2.4 Rock mass quality (Q-classification)
The Q-classification scheme was used in order to determine the rock mass quality in the trench. The description of the various Q-parameters is found in Appendix 3. The rock quality designation (RQD) is defined on the basis of visual estimation of the total amount of fracturing. The joint set numbers (Jn) have been defined from stereo projections. Roughness (Jr) and alteration (Ja) numbers (median values) were calculated for each section. Joint water reduction number (Jw) is estimated visually for each section and stress reduction factor (SRF) was given 1 for all sections due to surface proximity. Q-value is calculated using the following equation (Barton 1974; Grimstad & Barton 1993):
SRFJ
JJ
JRQDQ w
a
r
n
**
The Q-classification for the investigation trench OL-TK18 has been made for every mapping section (1.97-7.4 m long) and the results are listed in Table 2.5-1. The Q-quality varies from good to extremely good. The average Q-quality of the rocks is extremely good, thus the trench is absent in major brittle deformation zones which would have affected the Q-quality. Table 2.4-1. Q-parameters and Q-quality for each section in investigation trench OL-TK18.
Section Section Length RQD Jn Jr Ja Jw SRF Q-value Rock type Q-quality
P1 5.9 100 1 1.5 1 1 1 150.0 DGN Extremely Good P2 7.34 98 2 1.5 1 1 1 73.5 DGN/KFP/MGN Very Good P3 4.06 100 1 1.5 2 1 1 75.0 MGN/KFP Very Good P4 7.4 100 1 1.5 2 1 1 75.0 KFP/DGN Very Good P5 5.63 100 1 3 1 1 1 300.0 DGN Extremely Good P6 1.97 100 1 1.5 1 1 1 150.0 DGN Extremely Good P7 4.57 100 1 3 1 1 1 300.0 DGN/TGG Extremely Good P8 6.75 97 2 3 2 1 1 72.8 TGG/KFP Very Good P9 5.11 97 2 1.5 2 1 1 36.4 KFP/MGN/PGR Good P10 6.7 100 1 1.5 1 1 1 150.0 PGR Extremely Good
22
3 SUMMARY
Investigation trench OL-TK18 is located in the central part of the Olkiluoto study site adjacent to investigation trench OL-TK12 and OL-TK4. The trench has an E-W direction with a total length of 55.4 m and a width from 1 to 3 m. The rock types in investigation trench OL-TK18 is of heterogeneous character, with a large variation in their composition. The rocks vary from tonalitic granodioritic gneiss (TGG) to diatexitic gneiss (DGN), with portions of K-feldspar porphyritic gneiss (KFP). Inclusions of mica gneiss (MGN), quartz gneiss and skarn are encountered throughout the trench. A few coarse-grained pegmatitic granite dykes (PGR) are also present in the middle of the trench. The trench ends in a feldspar-rich pegmatoid (PGR). The rocks in the investigation trench have been subjected to a multiphase ductile deformation and the trench is situated in an area were the latest ductile deformation phase, D4 prevails. The central part of the trench is dominated by this D4 ductile deformation domain whereas the elements of the earlier deformation phase D3 prevail in both ends of the trench. The deformation phase D3 has a more ENE-WSW orientated direction whereas the D4 is striking NE-SW. In addition to this difference in orientation, the different structural signature of these two deformation types is observed, the S3 foliation is defined by smaller scaled granitic leucosome veining whereas the S4 foliation is more sheared and have a schistose character. The D4 ductile deformation domain is also characterised by a sheared blastomylonitic rock having growth of roundish feldspar porphyroblasts and it contains BT-schlieren indicating high alteration of the protolith. These BT-schlieren are strongly foliated and together with the S4 schistosity it gives the orientation for the D4 ductile zone. On the basis of orientations of all measured joints and faults one main set can be distinguished, striking NE-SW with a moderate dip towards the SE. The occurrence of this fracture set is explained by the D4 ductile deformation domain that is a natural zone of weakness for the development of these fractures in the same direction. There are no noticeable differences between fault and joint orientations in the trench, almost all faults are follows the foliation parallel joints of the D4 ductile deformation domain. Two major faults were identified from the trench, one with a distinct fault core of quartz, calcite and chlorite, and having a NW-SE strike and a moderate dip towards NE. The other one is parallel to the D4 ductile deformation domain, having a NE-SW strike and a moderate dip to SW, showing totally altered and deformed rock due to shearing. Mineral fillings observed on fracture surfaces are mostly hematite, but also chlorite biotite and muscovite is found. The average Q-quality of the rocks is extremely good, since the trench is absent in major brittle deformation zones which would have affected the Q-quality. The trench was instigated to investigate a geophysical mise-à-la-masse survey signature and also try to locate a brittle deformation zone OLBFZ045 at surface, which was detected in the ONKALO research tunnel at chainage PL3333-3350. Although no major brittle deformation zones were detected, the trench gave valuable information about the latest ductile deformation phase (D4) and characteristics of that phase.
23
REFERENCES
Aaltonen, I. (ed.), Lahti, M., Engström, J., Mattila, J., Paananen, M., Paulamäki, S., Gehör, S., Kärki, A., Ahokas, T., Torvela, T. & Front, K. 2010. Geological Model of the Olkiluoto Site, Version 2.0. Working report 2010-70. Posiva Oy, Eurajoki. 580 p. Barton, N. Lien & R. Lunde, J. 1974. Engineering classification of rock masses for the design of tunnel support. Rock Mechanics, Vol 6, No 4, p. 189–236. Grimstad, E. & Barton, N. 1993. Updating of the Q-system for NMT. Proc. of the International Symposium on Sprayed Concrete. Fagernes, Norway. Kompen, E. Opsahl, Berg. Norwegian Concrete Association, p. 46–66. Kärki, A. & Paulamäki, S. 2006. Petrology of Olkiluoto. Posiva 2006-02, Eurajoki, Finland: Posiva Oy. Mattila, J. 2006. A system of Nomenclature for Rocks in Olkiluoto. Posiva 2006-32, Eurajoki, Finland: Posiva Oy. Milnes A. G., Aaltonen, I., Ahokas, T., Front, K., Gehör, S., Kemppainen, K., Kärki, A., Mattila, J., Paananen, M., Paulamäki, S. & Wikström, L. 2007. Geological Data Acquisition for Site Characterisation at Olkiluoto: a Framework for the Phase of Underground Investigations. Working report 2007-32. Posiva Oy, Eurajoki 133 p. Wimmenauer, W. & Bryhni, I. 2002. Towards a unified nomenclature of metamorphic petrology: Migmatites and related rocks. A proposal on behalf of the IUGS Subcommission on the Systematic of Metamorphic Rocks. Web-version 31.07.2002. www.bgs.ac.uk/SCMR/docs/paper_7/scmr_paper_07.pdf.
24
APPENDICES
Appendix 1: Geological map of investigation trench TK-18 Appendix 2: Observations of all measured structures in investigation trench TK-18 Appendix 3: Q-classification scheme
App
endi
x 1
App
endi
x 2:
Mea
sure
men
ts a
nd o
bser
vatio
ns o
f all
map
ping
dat
a in
OL-
TK18
. Se
e en
d of
tabl
e fo
r exp
lana
tion
of a
bbre
viat
ions
.
ID
Structural Element
Dis
tanc
e fr
om b
olt
Nor
thin
g (m
) E
astin
g (m
)
Elevation (m)
Ori
enta
tion
Number of fractures
Fracture spacing (m)
Fracture length (m)
Displacement (cm)
Jr
Ja
Frac
ture
filli
ng
Aperture (cm)
Frac
ture
end
s
Undulation (cm/m)
Rock type
Foliation Type
Foliation intensity
Kin
emat
ic in
dica
tors
Remarks
Horizontal (m)
Vertical (cm)
Dip
Dip /Dir
No.
Profile
minerals + oxidation
width (mm)
End 1
to
End 2
to
F_Dip
F_Dir
Sens
e
of
Mov
e-m
ent
Uncertainty
P1_
1 JO
0.
57
0 67
9256
7.07
9 15
2578
3.66
1 8.
617
80
305
1
5.00
1.5
PR
O
1
P
J
PG
R
P1
_2
JO
3.30
17
67
9256
6.55
1 15
2578
6.30
9 8.
044
65
300
1
1.02
1.5
PRO
1
P
P
MG
N
P1
_3
JO
5.30
18
67
9256
6.16
4 15
2578
8.24
9 7.
739
40
170
1
5.50
3 U
RO
1
Y
2P
1 J
6
PG
R
P1
_4
JO
0 23
67
9256
8.85
6 15
2578
3.44
1 8.
471
75
190
1
3.70
3 U
RO
1
Y
2P
1 J
10
TG
G
N-s
ide
P1_5
JO
1.
50
43
6792
570.
037
1525
785.
189
8.05
0 65
15
1
2.
50
3
UR
O
1
J
Y
2P1
5 TG
G
N-s
ide
P1_6
JO
1.
40
10
6792
568.
585
1525
784.
798
8.39
4 75
20
2
0.4
1.40
1.5
PRO
1
Y
4
P
TGG
N
-sid
e P1
_7
JO
0 16
67
9256
6.31
6 15
2578
2.93
4 8.
541
70
20
1
1.22
1.5
PRO
1
P
J
P
GR
S
-sid
e P2
_1
FAU
LT
0.14
1
6792
566.
039
1525
788.
962
7.80
0 60
60
1
6.
00
0.
5 PS
L 2
KV, C
C, K
L 60
J
J
P
GR
M
easu
red
P2_
2 FO
L 1.
3 25
67
9256
5.95
5 15
2579
0.10
6 7.
385
55
170
1
D
GN
B
AN
1
S3
P2_
3 JO
1.
6 20
67
9256
5.93
3 15
2579
0.40
1 7.
390
60
315
1
3.50
1.5
PR
O
1
J
J
D
GN
M
easu
red
P2_
4 JO
1.
75
30
6792
565.
922
1525
790.
549
7.26
7 85
28
0 1
0.
90
1.
5 P
RO
1
Y
3
P
DG
N
P
2_5
FOL
3.4
52
6792
565.
803
1525
792.
176
6.79
8 50
13
0 1
KFP
S
CH
1
S4
P2_6
JO
3.
92
54
6792
565.
766
1525
792.
689
6.70
0 50
15
0 1
2.
60
2
USM
2
HE,
KL
0.3
J
J
4
KFP
M
easu
red
P2_7
JO
5.
15
57
6792
565.
677
1525
793.
901
6.48
4 15
13
0 1
1.
60
2
USM
1
HE
0.
3
Y
8 Y
3P
1 3
KFP
P2_
8 JO
5.
4 52
67
9256
5.65
9 15
2579
4.14
8 6.
496
80
320
1
1.20
2 U
SM
1
HE
0.
3
J
Y
3P1
3 M
GN
P2_
9 JO
5.
7 46
67
9256
5.63
7 15
2579
4.44
4 6.
511
75
10
1
0.40
1.5
PR
O
1
P
P
M
GN
P2_1
0 JO
5.
75
51
6792
565.
633
1525
794.
493
6.45
4 80
32
0 1
1.
50
1
PSM
1
HE
0.
3
J
Y
3P1
M
GN
P2_1
1 JO
5.
96
41
6792
565.
618
1525
794.
700
6.52
2 75
65
1
0.
40
1
PSM
1
HE
0.
3
Y
10
P
MG
N
P2
_12
JO
6 38
67
9256
5.61
5 15
2579
4.73
9 6.
546
25
146
3 0.
10
1.60
2 U
SM
1 H
E
0.1
J
Y
3P
1 2
MG
N
P2
_13
JO
7 18
67
9256
5.54
3 15
2579
5.72
5 6.
595
28
150
1
2.30
2 U
SM
1 H
E
0.1
J
Y
3P
1 2
MG
N
P2
_14
JO
7.18
10
67
9256
5.53
0 15
2579
5.90
3 6.
648
55
270
2 0.
05
1.06
1 PS
M
1
J
P
MG
N
P
2_15
JO
0
0 67
9256
7.80
4 15
2578
8.95
3 7.
831
85
40
1
3.00
7
4 S
RO
1
Y
1
P
DG
N
N-s
ide
P2_
16
JO
0 0
6792
567.
246
1525
788.
912
7.83
1 70
26
5 3
0.7
1.27
1 P
SM
1
HE
0.
2
P
P
D
GN
N
-sid
e P
3_1
FAU
LT
0.23
1
6792
565.
481
1525
796.
291
6.68
7 36
14
3 1
6.
05
1.
5 U
SL
2 H
E, K
L 0.
5
P
J
7
MG
N
P
3_2
JO
0.63
2
6792
565.
416
1525
796.
684
6.63
3 87
23
1
1.
50
1
PS
M
2 H
E, K
L 0.
2
J
Y
10
M
GN
P3_
3 JO
0.
72
2 67
9256
5.40
1 15
2579
6.77
2 6.
623
50
165
1
0.45
3 U
RO
1
0.5
P
P
2 M
GN
P3_
4 JO
1.
40
8 67
9256
5.29
1 15
2579
7.43
9 6.
487
68
290
1
1.41
1.5
PR
O
1
0.
1 P
P
KFP
P3_5
JO
2
7 67
9256
5.19
3 15
2579
8.02
7 6.
430
60
290
1
1.20
3 U
RO
2
HE,
KL
0.5
P
P
2
KFP
P3_6
JO
2.
38
7 67
9256
5.13
2 15
2579
8.39
9 6.
388
37
294
1
0.70
3 U
RO
2
HE,
KL
0.2
P
P
2
KFP
P3_7
JO
2.
65
10
6792
565.
088
1525
798.
664
6.32
7 80
27
5 1
0.
31
1.
5 PR
O
2 H
E, K
L 0.
2
P
P
K
FP
P
3_8
JO
2.9
8 67
9256
5.04
7 15
2579
8.90
9 6.
320
72
131
1
0.51
1.5
PR
O
2 H
E
0.2
P
P
KFP
P3_9
JO
3.
05
11
6792
565.
023
1525
799.
056
6.27
3 70
80
1
0.
70
1.
5 PR
O
2 H
E, K
L 0.
2
P
P
K
FP
P3
_10
JO
0 -1
0 67
9256
4.74
8 15
2579
5.93
9 6.
823
40
174
1
1.30
2 U
SM
2 BT
, KL
0.4
P
J
5 KF
P
S-si
de
P4_1
FA
ULT
4.
70
100
6792
563.
939
1525
804.
664
5.42
9 40
14
9 1
5.
30
1.
5 U
SL
5 IL
, SV
10
45
J
J
6
KFP
M
easu
red
P4_
2 JO
5.
20
148
6792
563.
841
1525
805.
154
4.96
6 83
84
1
1.
80
1.
5 P
RO
2
HE
0.
2
P
J
DG
N
P
4_3
JO
5.40
10
3 67
9256
3.80
2 15
2580
5.35
0 5.
423
64
155
1
5.50
3 U
RO
1
2 J
J
10
D
GN
M
easu
red
P4_
4 JO
6.
70
34
6792
563.
548
1525
806.
624
6.15
7 46
75
1
2.
60
3
UR
O
2 C
C, H
E
0.3
2 Y
5
Y
5 5
DG
N
P
4_5
JO
7.00
55
67
9256
3.48
9 15
2580
6.91
8 5.
958
72
314
1
3.21
1.5
PR
O
1
2
Y
3 J
DG
N
P4
_6
FAU
LT
0.4
30
6792
565.
661
1525
800.
625
5.98
3 75
17
0 1
1.
20
1.
5 U
SL
3 H
E, K
L 0.
6
P
P
3 K
FP
N-s
ide
P5_
1 FO
L 0
0 67
9256
3.41
2 15
2580
7.30
5 6.
521
50
128
1
D
GN
B
AN
1
S4
P5_
2 JO
0.
85
23
6792
563.
573
1525
808.
122
6.46
3 76
31
5 1
1.
24
1.
5 P
RO
1
HE
0.
2
P
P
D
GN
P5_
3 JO
3.
49
55
6792
564.
072
1525
810.
658
6.67
9 56
26
3 1
0.
91
1.
5 P
RO
1
2.5
Y
5 Y
4
D
GN
P5_
4 JO
3.
83
40
6792
564.
137
1525
810.
985
6.89
8 83
14
4 1
5.
48
3
UR
O
1
3.
5 J
J
15
D
GN
M
easu
red
P5_
5 JO
4.
05
41
6792
564.
178
1525
811.
196
6.93
3 73
28
1
7.
90
1.
5 P
RO
1
HE
0.
2 1.
5 J
J
DG
N
Mea
sure
d P5
_6
JO
4.71
6
6792
564.
303
1525
811.
830
7.41
6 88
23
2 1
0.
99
2 4
SRO
1
Y
4
Y
5
TGG
P5_7
JO
1.
03
31
6792
564.
196
1525
808.
179
6.42
0 74
34
8 1
2.
15
2 4
SRO
2
HE,
KL
0.3
J
P
D
GN
N
-sid
e
P5_
8 JO
3.
88
9 67
9256
3.61
6 15
2581
1.13
7 7.
218
87
29
1
3.95
1.5
PR
O
1 H
E
0.2
P
J
D
GN
M
easu
red
/S-s
ide
P5_
9 JO
5.
03
0 67
9256
2.89
2 15
2581
2.42
7 7.
541
25
4 1
1.
90
3
UR
O
1
P
Y
2P
7 5
DG
N
S-s
ide
P5_1
0 JO
5.
03
0 67
9256
2.30
3 15
2581
2.54
3 7.
541
28
112
1
1.30
3 U
RO
1
Y
9
Y
2P7
4 D
GN
S
-sid
e P
6_1
JO
0.79
3
6792
564.
140
1525
813.
420
7.74
1 16
16
0 1
0.
39
3
UR
O
1
Y
3 P
2 TG
G
P
6_2
JO
0.89
3
6792
564.
097
1525
813.
510
7.75
5 76
23
8 1
0.
68
1.
5 P
RO
1
P
P
DG
N
P
6_3
JO
0.93
3
6792
564.
080
1525
813.
545
7.76
1 71
29
5 1
2.
07
3
UR
O
1
J
P
2
TGG
P6_4
JO
1.
00
3 67
9256
4.05
0 15
2581
3.60
8 7.
770
40
219
1
0.09
1.5
PRO
1
Y
3
P
TGG
P6_
5 JO
1.
63
0 67
9256
3.78
1 15
2581
4.17
1 7.
887
84
69
1
0.79
1.5
PR
O
1
P
P
D
GN
P7_
1 JO
0.
38
7 67
9256
3.61
4 15
2581
4.85
8 7.
831
88
58
1
0.24
1.5
PR
O
1
P
P
M
GN
P7_
2 JO
0.
50
11
6792
563.
607
1525
814.
977
7.78
0 70
14
4 1
7.
10
3
UR
O
1
J
J
5 D
GN
M
easu
red
P7_
3 JO
0.
83
14
6792
563.
589
1525
815.
306
7.72
2 85
12
4 1
1.
92
3
UR
O
1
P
P
2 TG
G
P
7_4
JO
0.90
18
67
9256
3.58
6 15
2581
5.37
5 7.
675
40
126
1
3.01
3 U
RO
1
P
J
4 TG
G
P7
_5
JO
3.52
87
67
9256
3.44
5 15
2581
7.98
1 6.
757
25
123
1
3.02
2 U
SM
1 H
E
0.5
J
J
10
TG
G
Mea
sure
d P7
_6
JO
3.99
59
67
9256
3.41
9 15
2581
8.44
9 6.
996
84
264
1
3.54
3 U
RO
1
J
J
6
TGG
M
easu
red
P7_7
JO
4.
00
57
6792
563.
419
1525
818.
459
7.01
5 62
14
4 1
2.
78
3
UR
O
1
Y
2 Y
5
5 TG
G
P7
_8
JO
0.40
12
67
9256
3.41
3 15
2581
4.86
7 7.
779
87
34
1
1.54
1
4 SR
O
1
Y
2 Y
5P
5
TGG
S-
side
P8
_1
JO
0.45
13
67
9256
3.34
3 15
2581
9.47
1 7.
355
86
294
1
5.55
3 U
RO
1
HE
0.
2
J
J
6 TG
G
Mea
sure
d P8
_2
JO
1.10
16
67
9256
3.27
9 15
2582
0.11
4 7.
253
80
290
1
3.90
3 U
RO
1
Y
1
Y
1 4
TGG
P8_
3 JO
1.
25
15
6792
563.
264
1525
820.
262
7.24
6 68
20
3 1
1.
52
3
UR
O
1
P
P
25
TGG
P8_4
JO
2.
23
11
6792
563.
167
1525
821.
231
7.17
7 85
24
2 1
0.
63
1.
5 PR
O
1
P
P
TG
G
P
8_5
FOL
3.42
21
67
9256
3.04
8 15
2582
2.40
8 6.
945
45
119
1
K
FP
SC
H
1
S
4 P8
_6
FAU
LT
3.55
38
67
9256
3.03
6 15
2582
2.53
6 6.
761
34
120
5 0.
05
4.91
1.5
USL
3
HE,
KL
0.5
J
J
KFP
M
easu
red
P8_7
FA
ULT
4.
20
40
6792
562.
971
1525
823.
179
6.66
8 35
10
9 2
0.1
3.01
1.5
USL
4
HE,
KL,
SK
, MU
0.
6
J
J
KF
P
P8
_8
JO
5.35
29
67
9256
2.85
7 15
2582
4.31
6 6.
651
45
124
1
3.30
3 U
RO
2
HE,
KL
0.3
J
Y
7
5 K
FP
P8
_9
JO
6.20
18
67
9256
2.77
2 15
2582
5.15
7 6.
666
48
143
1
0.76
3 U
RO
1
Y
Y
2
KFP
P8_1
0 JO
6.
50
10
6792
562.
743
1525
825.
453
6.71
3 59
15
3 1
2.
40
3
UR
O
4 BT
1
P
P
5
KFP
P8_
11
FOL
5.40
21
67
9256
2.85
2 15
2582
4.36
6 6.
725
43
140
1
K
FP
SC
H
1
S
4 P
8_12
FO
L 6.
75
0 67
9256
2.71
8 15
2582
5.70
1 6.
785
35
118
1
K
FP
SC
H
1
S
4 P8
_13
JO
5.72
20
67
9256
2.98
9 15
2582
4.69
9 6.
699
51
149
1
3.02
0.
5 3
UR
O
1 H
E
0.2
J
Y
8
8 K
FP
N-s
ide
P8_1
4 JO
4.
60
40
6792
562.
752
1525
823.
557
6.62
4 81
20
3 1
2.
30
0.5
3 U
RO
1
Y
7
Y
4
KFP
S
-sid
e P8
_15
JO
6.15
18
67
9256
2.67
8 15
2582
5.09
7 6.
672
60
68
1
1.40
3 U
RO
1
Y
10
J
10
K
FP
S-s
ide
P9_
1 JO
0.
86
7 67
9256
2.86
6 15
2582
6.55
5 6.
744
89
342
1
1.44
8
4 S
RO
1
P
P
MG
N
P
9_2
JO
1.40
12
67
9256
2.96
0 15
2582
7.08
7 6.
712
74
355
1
0.56
2
3 S
SM
1
P
P
MG
N
P
9_3
FAU
LT
1.46
10
67
9256
2.97
0 15
2582
7.14
6 6.
734
47
130
1
5.00
1.5
US
L 2
HE
, BT,
MU
0.
3
J
J
2 M
GN
50
12
5
P9_
4 FA
ULT
2.
20
27
6792
563.
098
1525
827.
874
6.59
0 33
13
0 1
3.
60
1
PS
L 2
BT,
MU
0.
3
P
P
M
GN
P9_
5 JO
2.
30
15
6792
563.
116
1525
827.
973
6.71
3 25
11
9 1
3.
40
2
US
M
2 B
T, M
U
0.2
P
J
2 M
GN
P9_
6 FO
L 2.
31
15
6792
563.
118
1525
827.
983
6.71
4 25
11
9 1
MG
N
SC
H
2
S
4 P
9_7
LIN
2.
31
13
6792
563.
118
1525
827.
983
6.73
4 20
89
1
MG
N
P
9_8
JO
2.65
24
67
9256
3.17
7 15
2582
8.31
7 6.
635
74
56
5 0.
6 0.
95
1.
5 P
SM
1
P
P
MG
N
P9
_9
FAU
LT
3.40
42
67
9256
3.30
7 15
2582
9.05
5 6.
481
26
130
1
3.80
1 PS
L 2
HE,
BT,
MU
0.
4
J
J
M
GN
20
10
6 H
WD
V
P9_
10
FAU
LT
3.8
36
6792
563.
376
1525
829.
449
6.55
5 34
14
1 6
0.02
3.
02
1
PS
L 3
HE
, BT,
MU
0.
7
P
P
M
GN
25
12
0
P9_
11
JO
4.35
34
67
9256
3.47
1 15
2582
9.99
0 6.
594
35
124
1
4.20
3 U
RO
2
HE
, MU
0.
5 3
J
J
3 P
GR
P9_
12
JO
4.8
30
6792
563.
549
1525
830.
433
6.65
0 27
11
6 1
2.
70
3
UR
O
1
1.
5 J
Y
11
7
PG
R
P
9_13
JO
0.
4 9
6792
563.
111
1525
826.
045
6.70
8 40
14
0 1
1.
60
3
UR
O
3 B
T 0.
6
P
Y
10
P8
2 K
FP
N-s
ide
P10
_1
JO
0.85
36
67
9256
3.62
6 15
2583
1.60
5 6.
585
45
125
1
3.41
3 U
RO
1
1 Y
3
Y
3 2
PG
R
P
10_2
JO
1.
45
34
6792
563.
640
1525
832.
204
6.59
4 88
12
8 1
1.
30
3
UR
O
1
0.
1 Y
1
Y
3 5
PG
R
P
10_3
JO
1.
60
20
6792
563.
643
1525
832.
354
6.73
1 75
13
2 1
5.
86
1.
5 P
RO
1
HE
0.
2 1
J
J
P
GR
M
easu
red
P10_
4 FO
L 3.
00
5 67
9256
3.67
6 15
2583
3.75
4 6.
855
50
168
1
P
GR
B
AN
1
S3
P10
_5
JO
5.00
12
67
9256
3.72
2 15
2583
5.75
3 6.
748
74
143
1
2.60
1.5
PR
O
1
0.
5 P
J
P
GR
P10_
6 JO
5.
25
15
6792
563.
728
1525
836.
003
6.71
3 30
60
1
2.
92
3
UR
O
1
Y
10
J
7 P
GR
P10
_7
JO
5.55
5
6792
563.
735
1525
836.
303
6.80
8 13
11
1 2
0.06
0.
25
1.
5 P
RO
1
P
P
PG
R
P1
0_8
JO
6.30
10
67
9256
3.75
2 15
2583
7.05
2 6.
744
89
143
1
1.30
3 U
RO
1
0.1
P
P
4 P
GR
P10_
9 JO
6.
54
12
6792
563.
758
1525
837.
292
6.72
0 32
12
0 1
1.
11
3
UR
O
1
P
P
2 P
GR
P10_
10
JO
1.40
46
67
9256
4.43
8 15
2583
2.13
6 6.
475
82
142
1
2.32
3 U
RO
1
J
P
3 P
GR
N
-sid
e P1
0_11
JO
4.
20
3 67
9256
4.80
3 15
2583
4.92
8 6.
853
62
125
2 0.
53
1.50
1.5
PRO
1
P
P
PG
R
N-s
ide
P10_
12
JO
1.40
0
6792
562.
139
1525
832.
189
6.93
5 89
130
2 0.
3 1.
20
1.
5 PR
O
1
P
P
P
GR
S
-sid
e P1
0_13
JO
6.
13
5 67
9256
3.87
8 15
2583
6.87
9 6.
797
6523
51
1.
12
1.
5 PR
O
1
Y
7 Y
P
GR
N
-sid
e A
bbre
viat
ions
: R
ock
type
s: M
GN
= M
ica
gnei
ss, D
GN
= D
iate
xitic
gne
iss,
PGR
= P
egm
atiti
c gr
anite
, TG
G =
Ton
aliti
c gr
anod
iorit
ic g
neis
s, K
FP =
Fel
dspa
r por
phyr
itc S
truct
ural
ele
men
t: JO
= Jo
int,
FOL
= Fo
liatio
n J r
(Joi
nt r
ough
ness
): P
= P
lana
r, U
= U
ndul
ated
, S =
Ste
pped
, SM
= S
moo
th, R
O =
Rou
gh, S
L =
Slic
kens
ided
, Fol
iatio
n T
ype:
BA
N =
Ban
ded,
SC
H =
Sch
isto
se
Min
eral
abb
reva
tions
: KL
= C
hlor
ite, B
T =
Bio
tite,
KA
= K
aolin
ite, S
V =
Cla
y, H
E =
Hem
atite
, CC
= C
alci
te, S
K =
Pyr
ite, I
L =
Illite
, KV
= Q
uartz
, MU
= M
usco
vite
Fr
actu
re e
nds:
P =
vis
ible
, J =
hid
den,
Y =
join
s Kin
emat
ic in
dica
tors
, Sen
se o
f mov
emen
t: H
WD
= H
angi
ng w
all d
own
O
ther
: W =
wes
t, E
= ea
st, S
= so
uth,
N =
nor
th. N
-Sid
e/S-
Side
= o
bser
vatio
ns o
utsi
de o
f the
cen
tral t
hrea
d. M
easu
red
= Fr
actu
res w
hich
hav
e be
en m
easu
red
with
a la
ser t
achy
met
er to
get
exa
ct c
oord
inat
es.
28
Appendix 3. Description of RQD (1), Jn (2), Jr (3), Ja (4), Jw (5) and SRF (6) (Grimstad & Barton 1993).