UNIVERSITY OF GOTHENBURG Department of Earth Sciences Geovetarcentrum/Earth Science Centre

Petrological and

mineralogical description

of the Sweconorwegian

Uddevalla Granite,

southwestern Sweden

Adi Fazic

ISSN 1400-3821 B893 Bachelor of Science thesis Göteborg 2016

Mailing address Address Telephone Telefax Geovetarcentrum Geovetarcentrum Geovetarcentrum 031-786 19 56 031-786 19 86 Göteborg University S 405 30 Göteborg Guldhedsgatan 5A S-405 30 Göteborg SWEDEN Abstract

Adi Fazic. University of Gothenburg, Department of Earth Sciences; Geology, Box 460, SE- 405 30 Gothenburg

The peculiar positioning and characteristics of the Uddevalla Granite in the Sveconorwegian Province, being situated along a shear zone and cross-cutting the Stora-Le Marstrand Formation, Hisingen and Göteborg Suites has triggered an interest in investigating its origin and giving it a marker in the Swedish geological history. In order to do so, a collaboration studying the granite massif was carried out between me and Erik Jansson where this thesis deals with the petrological aspects and Erik presents the age of the granite.

The S-type characteristics, such as the observed amphibolite xenoliths in outcrops, the lack of hornblende as a constituent and the peraluminous composition of samples indicate a syn-collisional tectonic setting for the granite massif. -dating of the Uddevalla Granite yields a Concordia-age of 1027±9 Ma further supporting the ‘S-type’ character as it fits well within the proposed Agder phase (1050-980 Ma) of the Sveconorwegian orogeny, in which peak metamorphic conditions occurred at 1029±6 Ma. Discovery of the Uddevalla Granite and its properties delivers a strong support for the continent-continent collision theory which is provided for the Sveconorwegian Province.

Field relationships of the monzogranitic Uddevalla Granite display a red to light-colored shifting throughout the whole intrusive massif, which may be explained by the mineral modality where a higher K- amount is present in the red granites. It is suggested that two pulses or hydrothermal processes could explain the variations in the incompatible elements. Geothermometric calculations proved unreliable due to an observed post-crystallization alteration.

Keywords: Uddevalla Granite, Sveconorwegian, petrology, mineralogy, S-type, birdwing, geothermometry

Sammanfattning

Adi Fazic. University of Gothenburg, Department of Earth Sciences; Geology, Box 460, SE- 405 30 Gothenburg

Den udda positionen och karaktär på Uddevallagraniten i den Sveconorwegiska provinsen, belägen längs en skjuvzon samt att den klipper av Stora-Le Marstrandformationen, Hisingen och Göteborg Suites har väckt ett intresse i att ta reda på dess ursprung samt ge den en markör i Sveriges geologiska historia. För att kunna utföra detta så har ett samarbete mellan mig och Erik Jansson gjorts där detta kandidatarbete handskas med de petrologiska aspekterna och Erik presenterar granitens ålder.

Den S-type karaktär, som de observerade amfibolitxenoliterna på hällar, avsaknaden av hornblende och de peraluminösa kompositioner av proverna, indikerar på en syn-kollisional tektonisk miljö. Zirkon-datering på Uddevallagraniten resulterade i en Concordia-ålder på 1027±9 Ma vilket stöder dess ’S-type’ drag men vilken också passar bra in med den föreslådda Agder-fasen (1050-980 Ma) under den Sveconorwegiska orogenesen, där kulmen av metamorfa förhållanden ägde rum 1029±6 Ma. Fyndet ger ett starkt stöd för den en kontinent-kontinent kollisionsteori som är tillhandahållen för den Sveconorwegiska provinsen.

Fältobservationer på den monzogranitiska Uddevalla Graniten påvisar ett rött till vitt färgskiftande längs hela intruderande massivet, vilken kan förklaras av mineralmodaliteten där en högre K-fältspat mängd är närvarande i de röda graniterna. Det är föreslaget att två magma pulser eller hydrotermala processer kan förklara variationen i de inkompatibla ämnen. Geotermometriska berkäningar visade sig opålitliga på grund av en observerad post-kristallin ombildning.

Nyckelord: Uddevallagranit, Sveconorwegian, petrologi, mineralogi, S-type, birdwing, geotermometer

2 Contents 1. Introduction ...... 4 1.1. Geological Setting ...... 4 2. Samples and methods ...... 5 2.1. Sample description ...... 5 2.2. Field Observations ...... 6 2.3. Whole rock sampling ...... 6 2.4. Thin Sections and petrography ...... 6 2.5. Scanning Electron Microscope (SEM) ...... 7 2.6. -biotite Geothermometer...... 7 3. Results ...... 7 3.1. Mineralogy ...... 7 3.2.1. Alumina Saturation Index ...... 7 3.2.2 Geothermometer ...... 7 3.2.3. Trace Elements ...... 7 3.2.4. Pearce Diagram ...... 8 3.2.5. Spider Diagram ...... 8 4. Discussion ...... 8 Mineralogy ...... 8 Geothermometer ...... 8 Incompatible Elements ...... 9 Magma Pulses ...... 9 Tectonics and timeline ...... 9 Source rock ...... 9 5. Conclusions ...... 10 Acknowledgements ...... 10 References ...... 10 Appendix ...... 13 Appendix A ...... 13 Appendix B ...... 13 Appendix C ...... 13

3 1. Introduction cutting the N-S trending Stora-Le Marstrand In order to shed light to the origin of the Formation (SLM) and Hisingen Suite. Field Uddevalla Granite, a comprehensive study was observations at Frölandskrossen and Kallsås conducted by Erik Jansson and myself. Erik reveals a contact with the overlying SLM concentrated on the age (Zircon dating of the Formation and late-stage metamorphism along intrusive Uddevalla Granite) whilst the foci of the shear zone. this study are the petrological aspects, 1.1. Geological Setting achieved using geochemistry, mineralogy The recently dated Uddevalla Granite yields a along with geothermometric calculations and Concordia age of 1027±8,7 Ma (Jansson, field observations. 2016) and lies in the Idefjorden Terrane, Previously interpreted as post-orogenic granite southwestern Sweden. The Idefjorden Terrane, dating from 900-1000 Ma, the hereby called sometimes referred to as the Western Segment, Uddevalla Granite is the first syn-collisional comprises mainly of the SLM Formation, granite to be discovered in the Idefjorden defined as a metasedimentary rock and is Terrane. Field relationships and the S-type argued to be formed from a back-arc setting at signature of the Uddevalla Granite provides a about 1590 Ma (Åhäll et al., 1998; Cornell et better understanding of the Sveconorwegian al., 2000). The two other large constituents are orogeny and supports the continent-continent the mafic to calc-alkaline Hisingen- and collisional model proposed by Bingen et al. Göteborg Suites, dated to 1634-1522 Ma (2008). Its age of 1027±8,7 Ma fits the (Åhäll et al., 1998; Åhäll & Connelly, 2008). timeline of the proposed Agder phase at 1050- The Idefjorden Terrane, separated to the east 980 Ma where peak metamorphic conditions in by the Mylonite zone (Magnusson, 1960) the Idefjorden Terrane enabled intrusion of the where the Eastern Segment lies, comprises massif along the shear zone near Uddevalla, mostly of 1800-1640 Ma gneissic granitoids Sweden (figure 1). (Bingen et al., 2008, and references therein.). To the west of the Idefjorden Terrane lies the Telemarkia, Bamble and Kongsberg Terranes, described by Andersen et al. (2004); Bingen et al. (2005; 2008).

Peak metamorphic conditions that enabled intrusion of the Uddevalla Granite reached amphibolite facies conditions at about 1046- 1020 Ma (Romer & Smeds, 1996; Åhäll et al., 1998; Hegardt et al., 2007; Hegardt, 2010; Söderlund et al., 2008). The conditions during this period are well within the proposed timeline of the Agder Phase (Bingen et al., 2008) where syn-collisional granitoids are suggested to have formed. Other granites in the area, such as the post-orogenic 919-922 Ma Bohus Granite, intruded during the later stages Figure 1, Map from SGU (2015) of the of the orogeny and is believed to be the last region and locations of samples. episode of the Sveconorwegian plutonism The granite stretches about 27,5 km from (Eliasson & Schöberg, 1991). Ljungskile to Munkedal and is a NW-SE orientated body of elongated shape, cross-

4 2. Samples and methods number in crystals. Accessory also occur, usually about 1 mm in size. 2.1. Sample description Samples DC1501, DC1502 and DC1503 were DC1503 (not used in analysis), Frölandskrossen, foliated amphibolite all collected from Frölandskrossen (figure 1) (intercalated) by Adi Fazic, Erik Jansson and David Cornell. Collected from Frölandskrossen, the foliated The outcrop at Frölandskrossen displayed amphibolite consists mainly of biotite. Smaller intercalated rocks with red granite (DC1501), amounts of mafic minerals and (DC1502) and amphibolite xenoliths which give the salt-and-pepper appearance (DC1503). These intercalations of rock appear were also observed. The plagioclase grains to be gradual and are of varying depth in the vary in size from 2-10 mm and the biotite vary different layers. Samples DC1506 and DC1507 from 2-4 mm. were collected by Adi Fazic, Erik Jansson and David Cornell from the road cut at Torp DC1507 (Leuco 1), Torp road cut, fine- (figure 1) which displayed xenoliths such as grained leucocratic granite the one at Frölandskrossen. TEN150001, The sample is a leucocratic granite with its TEN150003 and TEN150004 (figure 1) were light color possibly due to the amount of collected by Thomas Eliasson, where sample plagioclase and smaller amount of K-feldspar. TEN150004 was retrieved from the northern , plagioclase, K-feldspar and biotite or part of the intrusion in figure 1. Outcrops of muscovite constitutes most of the sample with TEN150001, TEN150003 and TEN150004 garnet and iron-oxide as accessory minerals. showed more homogenous phaneritic granites Grains are mostly 1-2 mm in size. with the occasional and aplites. For DC1506 (not used in analysis), Torp road cut, further reference all samples will have labels fine-grained leucocratic granite with streaks corresponding to their rock type, i.e. Red for of garnet the red granites, Leuco for the leucogranites The specimen is very similar to DC1507 in and Peg for the pegmatite (table 1). mineralogy with the exception of a garnet- bearing streak throughout a small part of the DC1501 (Red 1), Frölandskrossen, fine- area. DC1506 and DC1507 were both collected grained red granite (intercalated) from the outcrop at Torp road cut. This granite has grain sizes up to 5 mm with K-feldspar, quartz and plagioclase making up TEN150001 (Red 2), Kissleberg, medium to most of the sample. Muscovite and biotite also coarse grained red granite occur and comprise about 15% of the rock. The sample was taken from Kissleberg (see figure 1) and is fine to medium in grain size. DC1502 (Peg), Frölandskrossen, pegmatitic TEN150001 consists mainly of K-feldspar, granite (intercalated) which gives the granite its red color. Quartz, Pegmatitic granite with K-feldspar grain sizes plagioclase and muscovite or biotite makes up of about 2-10 cm. Quartz and muscovite rest of the rock with similar amounts. Grain appear in smaller sizes, from 2-10 mm. K- size is fairly constant with grains from 1-4 feldspar comprises most of the volume of the mm’s. sample with muscovite and quartz being lesser constituents, although still a relatively large

Table 1, Rock type, sample locality and mineral modalities of samples. Sample Rock type Coordinate N Coordinate E Quartz K-feldspar Plagioclase Biotite Muscovite Chlorite Garnet Zircon Opaques DC1501 (Red 1) Red granite 6470714 316376 35 25 15 15 5 1 4 DC1502 (Peg) Granite-pegmatite 6470714 316376 40 35 20 5 DC1507 (Leuco 1) Leucocratic granite 6472786 313343 40 15 25 15 2 3 TEN150001 (Red 2) Red granite 6472731 315395 45 35 15 5 TEN150003 (Leuco 2) Leucocratic granite 6478429 309149 40 20 20 2105 3 TEN150004 (Red 3) Pinkish-red granite 6480736 306970 35 25 20 28 7 Trace3

5 TEN150003 (Leuco 2), Kallsås, NCC Roads indicating no post-crystallization deformation. AB, fine to medium-sized leucocratic granite. The deformation is thought to have occurred This light colored granite consists mainly of during the crystallization of the granite whilst quartz and but also minor biotite and the shear zone was still active. garnet. The specimen is from the northern part of the intrusion and is similar to the DC1507 sample.

TEN150004 (Red 3), Skaveröd, Skredsvik, fine to medium-sized pinkish-red granite The specimen from the outcrop at Skredsvik (northernmost part of intrusion) contains mainly K-feldspar, plagioclase, quartz and lesser amounts of muscovite or biotite. Grain sizes vary from 1-5 mm. The K-feldspar grains tend to be larger in size compared to the quartz Figure 4, Frölandskrossen, pegmatitic veins cross-cutting and micas. the slightly deformed granite. Figure 5 displays leucocratic parts of the 2.2. Field Observations Uddevalla Granite incorporating xenoliths, Field observations of the Uddevalla Granite possibly from the Hisingen Suite or SLM. with contacts and xenoliths at three different locations.

Figure 2 and figure 3 show the Stora-Le Marstrand (SLM) Formation in contact with both the red and its leucocratic counterpart of the underlying Uddevalla Granite.

Figure 5, Torp road cut, DC1507 with amphibolite enclaves.

2.3. Whole rock sampling Figure 2, Frölandskrossen, picture of a contact with the About 2-4 kg of each sample were coarsely SLM Formation and Uddevalla Granite. crushed and 1/8th were sent to labs (ALS Piteå and ALS Loughrea) for whole rock analysis. The analytical procedures used can be found in appendix C.

2.4. Thin Sections and petrography Polished thin sections (table 1) were made for six samples. They were carbon-coated with 25 nm for mineral identification using optical- Figure 3, Kallsås, picture of the leucocratic Uddevalla Granite underlying the SLM Formation (picture by and Scanning Electron Microscopes. The Thomas Eliasson, SGU). mineral modes were estimated using a petrographic microscope. Unfortunately Figure 4 shows the slightly deformed granite DC1506 did not contain garnet and biotite in being cross-cut by its pegmatitic veins,

6 the thin section. TEN150003 (Leuco 2) was 1,5 the only sample used for geothermometry. 3

O Peralkaline 2 2.5. Scanning Electron Microscope 1 Metaluminous Peraluminous

(SEM) O)/Al 2 The minerals were analyzed with the Hitachi O+K S-3400N Scanning Electron Microscope with 2 0,5 an energy dispersive X-ray detector, calibrated (Na Red 1 Leuco 1 Red 2 Red 3 using cobalt linked to simple element or oxide Peg Leuco 2 0 standards. Specimen current was set at 6 nA 0,5 1,0 1,5 with an accelerating voltage of 20 kV. The Al2O3/(Na2O+K2O+CaO) working distance was fixed to 9.6 ± 0.1 mm. Figure 7, ASI Index for all samples, (see table 1 for sample labels). 2.6. Garnet-biotite Geothermometer 3.2.2 Geothermometer The geothermometer uses garnet and biotite Table 2 shows the calculated garnet-biotite analyses to calculate equilibrium temperatures. geothermometer from sample TEN150003 Used geothermometers were Hodges & Spear (Leuco 2). The garnet and biotite data are (1982) and Perchuk & Lavrent’Eva (1983). given in appendix b. Important to note is that the calculated biotite and garnet grains were apart and not in contact The calculated temperatures vary from 516 °C with each other which may have some as the lowest temperature to 584°C as the implications on the results. highest with an average of the averages at 561°C. Unfortunately the biotite minerals were not representative enough and several analyses 3. Results were carried out on one single grain of biotite. Petrography in sample TEN150003 (Leuco 2) 3.1. Mineralogy displayed many of the biotite grains to have Table 1 shows estimated mineral modes and been altered to chlorite. rock types. According to a QAPF diagram (Streckeisen, 1974), all samples are classified Table 2. Calculations for the geothermometer, based on as , which is a sub-group of (Hodges & Spear, 1982) and (Perchuk & Lavrent’Eva, 1983). granites (figure 6). Reference points Temperature (degrees C°) Mean Hodges & Spear (1982) 541 516 588 547 557 581 572 557 Perchuk & Lavrent’Eva (1983) 547 534 574 565 571 584 579 565 Mean of Means 561 3.2.3. Trace Elements Figure 8 shows trace element profiles with concentrations normalized to the chondritic values of Evensen et al. (1978). Samples Red 1, Red 2 and Red 3 show a consistent LREE enrichment and steady decrease in concentration of these, with minor or no Eu Figure 6, QAPF Diagram after Streckeisen (1974). negative anomalies. Samples Leuco 1, Leuco 2 and Peg show lower concentrations of LREE, 3.2.1. Alumina Saturation Index enrichment in HREE and slightly larger The alumina saturation index (figure 7), show negative Eu anomalies compared to the red that all samples are of a slightly peraluminous granites. This trend is a so called birdwing composition. profile, well described by Schade et al. (1989).

7 100 10

1

10

0,1 Sample/Chondrite Sample/Contineltal crust Sample/Contineltal Red 1 Leuco 1 Red 1 Leuco 1 Red 2 Red 3 Red 2 Red 3 Peg Leuco 2 Peg Leuco 2 1 0,01 La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu Ba Rb Th K Nb La Ce Sr Nd P Sm Zr Ti Y Yb

Figure 8, Trace element concentrations normalized Figure 10, Spider diagram of various elements in all against chondrite values (see table 1 for sample labels). samples (see table 1 for sample labels).

3.2.4. Pearce Diagram Diagram based on Pearce et al. (1984), which 4. Discussion deals with a geochemical classification for granitic rocks (figure 9). It indicates a syn- Mineralogy collisional setting for the sampled rock. First impressions of the granite samples are given from the difference in color. The light color in leucocratic granites is likely due to the 1000 lower K-feldspar and higher plagioclase Syn-collisional granite content which is displayed in table 1. All

Within-plate granite samples show a monzogranitic composition, as 100 seen in figure 6. Garnets were identified in Volcanic-arc granite samples DC1507 (Leuco 1) and TEN150003

Rb (ppm) Ocean-ridge granite (Leuco 2) and will be discussed further on as 10 they are of interest from a petrological view.

Red 1 Leuco 1 Red 2 Red 3 Leuco 2 Geothermometer 1 1 10 100 Eliasson & Schöberg (2003) carried out Yb + Ta (ppm) geothermobarometric calculations on four Figure 9, Diagram after Pearce et al. 1984, indicating of the tectonic setting of sample (see table 1 for sample garnet-biotite bearing Bohus-granite samples. labels). Their results yield an intruding temperature of at least 715°C with a final crystallization 3.2.5. Spider Diagram temperature of 670-680°C. Along with the The spider diagram (figure 10) is normalized temperature-values Eliasson & Schöberg to continental crust. The figure shows a good (2003) also estimated pressure to be at about 4 correspond to the normalized values with some kbar or slightly higher, equivalent to about 15 smaller variations in certain elements. Samples km beneath the surface. DC1502, DC1507 and TEN150003 generally have lower concentrations in the LREE and Geothermometer values in table 2 shows a higher in HREE. In the same three samples a mean temperature of about 561°C and much lower ratio of Ba is also observed and assuming similar pressures it would the same trend seems to follow Sr, although correspond to lower amphibolite facies not as dramatic. (Winter, 2001). Instead it is suggested that the rock has been altered after crystallization. Evidence for this is the chloritization which is

8 seen throughout sample TEN150003 (Leuco known to be the last to crystallize in a melt, 2). (Quirke & Kremers, 1943) would incorporate some of the fractionated HREE that remained. It is advised that upcoming studies could investigate both red and leucocratic granite A second pulse of magma could then crystallization temperatures and pressures. crystallize the leucocratic granites from the These could help to understand the conditions LREE-depleted source. The HREE would then under which the two groups of rocks be incorporated in the garnets of the crystallized. leucocratic granites. Further support for this theory would have been a leucocratic Incompatible Elements pegmatite sample. This pegmatite would A distinction between red granites and theoretically show very low LREE values and leucogranites and pegmatite is seen in the trace even higher HREE than previous samples, elements (figure 8) showing a birdwing profile crystallized from the last remaining magma. (Schade et al., 1989). A reason for this trend could be the higher concentration of HREE in Tectonics and timeline leucocratic granites due to the incorporation of Field observations (figure 2 and 3) show the these elements in garnets. Such an example is overlaying metasedimentary rock where the the leucocratic and, yielding higher amounts of Uddevalla Granite may well have intruded. garnets in contrast to the red granites. The Figure 1 displays how the granitic body elevated HREE concentrations in the pegmatite follows the shear zone, where faults are may be caused by it being in a last-stage evident and hot magma can rise easily through crystallization of the granite and thus the faults and crystallize. Deformation incorporates some of the remaining structures being cross-cut by pegmatitic veins fractionated elements (Winter, 2001). in figure 4 shows an active shear zone during the crystallization of the Uddevalla Granite, A different explanation for the birdwing indicating late-stage metamorphism. profile in figure 8 can be a cause of hydrothermal processes. Schade et al. (1989) The evident tectonics and Pearce diagram states that these birdwing-shaped profiles are a (figure 9) along with the Concordia age of result of rare earth element mobility caused by 1027±8,7 Ma (Jansson, 2016) support the interaction of REE with special fluids. continent-continent collisional model for the Sveconorwegian orogeny submitted by Bingen The difference in Ba between red granites and et al. (2008). The model proposes syn- the leucogranites and pegmatite (figure 10) collisional granitoids during the Agder Phase may be explained by the larger amount of (1050-980 Ma) with amphibolite facies where biotite and K-feldspar that comprise the red metamorphic conditions of the granites. Barium is a large-ion lithophile Sveconorwegian province peaked (Bingen et element and can substitute for K in K-feldspar al., 2008; Hegardt, 2010). We therefore and biotite (Rossiter et al. 2008). propose a sedimentary type source rock for the Uddevalla Granite as they are often associated Magma Pulses with continental collisions and which will be Since there is an apparent color variation further discussed in the next section. through the granite massif, the idea of two different magma pulses may explain the color Source rock contrast. The first magma to crystallize would Earlier studies seem to believe that a deeper explain the red granitic ones which would granite-body can be the source of the deplete the LREE from the source. Hereon Uddevalla Granite (Romer & Smeds, 1996) after the pegmatite, as earlier mentioned, although Jansson (2016) discusses the

9 possibility of a sedimentary source as during tectonic thickening event xenocryst cores yield ages of a during the Agder Phase (1050-980 metasedimentary sources, such as the SLM Ma). Formation. An indicator of a sedimentary  Late-stage metamorphism is evident origin would also be the metasedimentary during the crystallization of the xenoliths observed at outcrops in figure 2, 3 Uddevalla Granite. and 5.  Many petrological aspects support the characteristics of an S-type granite. The support for S-type granite can be established using studies concluded by Acknowledgements Chappell & White (2001). Their revisions of Foremost I would like express my deepest large granitic batholiths in the Tasman gratitude to my family for their support. My Orogenic Zone have enabled the possibility to co-author and friend Erik Jansson along with distinguish S-type from I-type granites using the advisors David H. Cornell and Thomas various approaches. One approach, such as Eliasson were extremely helpful and great to hornblende being present as a mafic mineral in work with. Sincere thanks go out to Thomas the host rock is an exemplary of an I-type Zack for helping with ICP-Ms analysis and granite. Hornblende as such was not identified undertaking the task as an examiner. I also in any of the samples; instead the mafic thank Emily Whitehurst Zack, Johan Hogmalm mineral in sampled granites is biotite. Biotite and Andreas Karlsson for giving a hand in may according to Chappell & White (2001) creating thin sections, ICP-Ms guidance and even be an abundant mineral in the more mafic lab work Last but not least I would like to S-type granites, compiling up to 35% of the thank Danial Farvardini for being a friend and total composition. Their study shows that mentor throughout my Bachelor’s programme garnets are often accessory minerals in S-type here at GVC. granites because of the peraluminous property. Garnets generally, are observed in the References leucocratic granites, while all samples are Åhäll, K. I., & Daly, J. S. (1989). Age, peraluminous (figure 7). Chappell & White tectonic setting and provenance of (2001) also emphasize that low Ca Östfold-Marstrand Belt Supracrustals: concentrations are very distinctive of S-type west-ward crustal growth of the Baltic granites which coincides well with the low Shield at 1760 Ma. Precambrian amount in samples of the Uddevalla Granite, at research, 45(1-3), 45-61. concentrations of ~1% (table 3, appendix A). Åhäll, K. I., Cornell, D. H., & Armstrong, R. (1998). Ion probe zircon dating of 5. Conclusions metasedimentary units across the  Mineralogical differences can explain Skagerrak: new constraints for early the color variation from the dissimilar Mesoproterozoic growth of the Baltic granites. Shield. Precambrian Research, 87(3),  The garnet-biotite geothermometer 117-134. was inconclusive, most likely due to Åhäll, K.-I., & Connelly, J. (2008). Long- chloritization. term convergence along SW  There is a clear variation in trace- and Fennoscandia: 330 m.y. of Proterozoic incompatible elements within the crustal growth. Precambrian Research color-contrasting granites. 161, 452-474.  The Uddevalla Granite is likely to have intruded along the shear zone

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11 Perchuk, L. L., & Lavrent’Eva, I. V. Schade, J., Cornell, D. H., & Theart, H. F. (1983). Experimental investigation of J. (1989). Rare earth element and exchange equilibria in the system isotopic evidence for the genesis of the cordierite-garnet-biotite. In Kinetics and Prieska massive sulfide deposit, South equilibrium in mineral reactions, 199- Africa. Economic Geology, 84(1), 49- 239. Springer New York. 63.

Quirke, T. T., & Kremers, H. E. (1943). Shand, S. J. (1927). Eruptive rocks: their Pegmatite crystallization. Am. Mineral, genesis, composition, classification, and 28, 571-580. their relation to ore-deposits, with a chapter on meteorites. T. Murby. Romer, R. L., & Smeds, S. A. (1996). U-Pb columbite ages of pegmatites from Söderlund, U., Hellström F.A., & Kamo, Sveconorwegian terranes in S.L. (2008). Geochronology of high- southwestern Sweden. Precambrian pressure mafic granulite dykes in SW Research, 76(1), 15-30. Sweden; tracking the P-T-t path of metamorphism using Hf isotopes in Rossiter, A. G., & Gray, C. M. (2008). zircon and baddeleyite. Journal of Barium contents of granites: key to Metamorphic Geology 26, 539-560. understanding crustal architecture in the southern Lachlan Fold Belt?. Australian Winter, J. D. (2014). Principles of igneous Journal of Earth Sciences, 55(4), 433- and metamorphic petrology. Pearson. 448.

12 Appendix

Appendix A

Table 3, Geochemical data in percentage for all samples. Sample SiO2 Al2O3 Fe2O3 CaO MgO Na2OK2OCr2O3 TiO2 MnO P2O5 CS TEN150001 73 14,5 0,8 1,1 0,16 3,7 5,1 0,02 0,05 0,03 0,02 0,01 <0.01 TEN150003 74,7 14,2 0,8 1,1 0,10 3,9 4,8 0,02 0,05 0,05 0,01 0,01 <0.01 TEN150004 74,2 14,3 1,0 1,0 0,20 3,6 5,2 0,02 0,09 0,02 0,02 0,03 <0.01 DC1501 74,7 14,2 1,1 1,2 0,19 3,8 4,7 0,02 0,09 0,03 0,03 0,02 <0.01 DC1502 74,6 15 0,5 0,5 0,07 3,4 6,9 0,02 0,02 0,04 <0.01 <0.01 <0.01 DC1507 74,9 14,6 0,8 1,2 0,07 4,2 3,8 0,02 0,03 0,11 0,02 0,01 <0.01 Table 4, Geochemical data used in spider diagram.

Sample Ba Rb Th K Nb La Ce Sr Nd P Sm Zr Ti Y Yb TEN150001 677 270 3,4 2,1 22,5 7,4 16 248 8,5 44 2,1 43 1,4 15,4 15 TEN150003 159 249 3,6 3,1 15,2 3,6 8 109 4,4 218 1,8 53 3,9 35,5 36 TEN150004 764 159 5,5 2,6 5,6 15,1 33 366 15,8 436 3,4 91 0,6 6,2 6 DC1501 538 265 3,9 1,9 5,9 9,4 21 229 10,2 655 2,2 66 1,1 10,2 10 DC1502 77 356 4,9 3,2 14,4 3,5 7 62 4 655 1,7 26 5,8 57,6 58 DC1507 34 261 4,8 4,2 27,8 6,6 14 57 7,8 436 2,6 49 5,9 52,3 52 Table 5, Data for trace element concentrations (values in ppm, except for K) Sample La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu Y TEN150001 7,4 16 1,9 8,5 2,1 0,4 2,1 0,4 2,2 0,4 1,3 0,2 1,4 0,2 15,4 TEN150003 3,6 8 1,0 4,4 1,8 0,4 3,1 0,7 5,2 1,2 3,7 0,5 3,9 0,6 35,5 TEN150004 15,1 32,8 4,0 15,8 3,4 0,7 2,6 0,3 1,4 0,2 0,6 0,1 0,6 0,1 6,2 DC1501 9,4 20,6 2,5 10,2 2,2 0,7 1,9 0,3 1,6 0,3 1,1 0,2 1,1 0,2 10,2 DC1502 3,5 7,3 0,9 4 1,7 0,4 3,2 0,9 7,3 1,8 5,5 0,9 5,8 0,9 57,6 DC1507 6,6 14 1,8 7,8 2,6 0,4 4,2 0,9 7,1 1,7 5,3 0,9 5,9 0,9 52,3

Appendix B

Table 6, Data for three garnets (7 spots) and one biotite grain (3 different spots). Mg/(Mg+Fe) Garnet end members Biotite vi Sample Grt Bt KD Alm Sps Prp Grs X(Ti) X(Al ) Grt 1-1 / Bt 1-1 0,04 0,21 6,81 0,50 0,42 0,02 0,07 0,04 0,39 Grt 1-2 / Bt 1-1 0,04 0,21 7,35 0,52 0,40 0,02 0,06 0,04 0,39 Grt 1-3 / Bt 1-1 0,04 0,21 5,83 0,51 0,40 0,02 0,06 0,04 0,39 Grt 2-1 / Bt 1-2 0,04 0,18 6,13 0,53 0,39 0,02 0,06 0,04 0,43 Grt 2-2 / Bt 1-2 0,04 0,18 5,94 0,52 0,40 0,02 0,06 0,04 0,43 Grt 3-1 / Bt 1-3 0,04 0,18 5,52 0,49 0,43 0,02 0,06 0,04 0,44 Grt 3-1 / Bt 1-3 0,04 0,18 5,67 0,50 0,41 0,02 0,07 0,04 0,44

Appendix C

Table 7, Analytical procedures for geochemical data Analytical Procedures ALS Code Description Instrument ME-MS81 Lithium Borate Fusion ICP-MS ICP-MS ME-MS42 Up to 34 elements by ICP-MS ICP-MS OA-GRA05 Loss on ignition at 1000C WST-SEQ TOT-ICP06 Total Calculation for ICP06 ICP-AES ME-4ACD81 Base Metals by 4-acid dig. ICP-AES ME-ICP06 Whole Rock Package - ICP-AES ICP-AES C-IR07 Total Carbon (Leco) LECO S-IR08 Total Sulphur (Leco) LECO

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