NORWEGIAN JOURNAL OF GEOLOGY Geochronology of magmatism in the Caledonian and Sveconorwegian belts of Baltica 267

Geochronology of magmatism in the Caledonian and Sveconorwegian belts of Baltica: synopsis for detrital zircon provenance studies

Bernard Bingen & Arne Solli

Bingen, B. & Solli, A.; Geochronology of magmatism in the Caledonian and Sveconorwegian belts of Baltica: synopsis for detrital zircon provenance studies. Norwegian Journal of Geology, vol. 89, pp. 267-290. Trondheim 2009. ISSN 029-196X.

A compilation of literature concerning U-Pb geochronological data recording magmatic events is presented for the Sveconorwegian and Caledonian belts of Baltica. It illustrates the episodic nature of magmatism along the western margin of Baltica from Archaean to Permian and helps identify primary zircon sources for detrital zircon provenance studies in North Atlantic regions. Archaean orthogneisses ranging from 2885 to 2635 Ma occur in basement windows in the northern Caledonides. Voluminous Palaeoproterozoic, mainly felsic, magmatism is regarded as part of the Transcandinavian Igneous Belt: it is dated at 1805-1770 Ma in the Nordland, Lofoten and Rombak windows, 1686-1621 Ma in the West Norway Gneiss Complex, and mainly 1797-1640 Ma in the Eastern Segment of the Sveconorwegian belt. As a first approximation, crystalline sheets in the Middle Allochthon mirror basement windows at equivalent latitudes. Voluminous Mesoproterozoic magmatism ranges from 1659 to 1517 Ma in the Idefjorden Terrane, 1572 to 1460 Ma in the Bamble and Kongsberg Terranes and 1555 to 1459 Ma in the Telemarkia Terrane. The Sveconorwegian belt hosts a variety of local to regional magmatic suites covering the entire time spans between 1473 and 1130 Ma and between 1060 and 914 Ma. Sveconorwegian post-collisional suites between 971 and 914 Ma are voluminous in the west of the belt and include anorthosites. Pre-Sveconorwegian (1257-1237 and 1190 Ma) and Sveconorwegian (976 to 891 Ma) intrusions are common in the southern part of the Caledonides, while, in the Northern Caledonides, minor 981-973 Ma granite plutonism is reported in the Kalak Nappes. The Caledonian and Sveconorwegian belts are poor in Cryogenian to Ediacaran magmatism, the only significant exceptions being the Seve and Kalak Nappes showing low volume suites at 876-825 Ma and 711-680 Ma and the 571-523 Ma Seiland Igneous Province. Cambro-Silurian magmatism ranging from 497 to 424 Ma and including Iapetan ophiolites and volcanic arcs is specific for the Upper and Uppermost Allochthons of the Caledonides. Scandian to late-Scandian pegmatites and minor intrusions range from 436 to 390 Ma in the basement windows and the Middle Allochthon. Dated magmatism in the Oslo rift ranges from 300 to 277 Ma. The compilation highlights the Mesoproterozoic signature of the Sveconorwegian belt. Erosion of primary magmatic sources in the Sveconorwegian belt can generate a whole range of Palaeoproterozoic to Mesoproterozoic detrital zircons ranging from ca. 1800 to 900 Ma, with only one clear gap between 1130 and 1060 Ma corresponding to the onset of the Sveconorwegian orogeny. Erosion of magmatic rocks in the Caledonides can produce a discontinuous distribution of detrital zircons characterized by a number of discrete modes ranging from Archaean to Devonian, and large gaps in the early Palaeoproterozoic (2500-1940 Ma), and in the Mesoproterozoic and Neoproterozoic. Primary magmatic source rocks contribute only marginally to the present day discharge from the Caledonides. This implies, not unsurprisingly, major sourcing in metasediments exposed in Caledonian allochthons and widespread sediment polycyclism.

Bernard Bingen (bernard.bingen @ ngu.no) & Arne Solli ([email protected]), Geological Survey of Norway, 7491 Trondheim, Norway.

Introduction Improved interpretation of detrital zircon provenance requires improved characterization of potential sources. The volume of U-Pb geochronological data has Zircon crystallizes dominantly during magmatic increased rapidly in recent years in all types of rocks. processes, but also during subsolidus high-grade This trend has been possible thanks to developments metamorphic processes. The primary sources of detrital in instrumentation with microsampling capacity, like zircons are thus magmatic rocks and their deformed/ secondary ion mass spectrometry (SIMS) and laser metamorphosed derivatives, and to a lesser extent ablation inductively coupled plasma mass spectrometry high-grade metamorphic rocks. The Caledonian and (LA-ICPMS). Especially significant is the development Sveconorwegian belts in Scandinavia host the lithologies of detrital zircon provenance studies in clastic sediments. that are interpreted to represent the western margin of U-Pb dating of detrital zircons, in conjunction with Baltica exposed to erosion during the Neoproterozoic and other characterization of the zircons (inclusions, trace Phanerozoic (Fig. 1). This publication offers an updated element composition, Lu-Hf and O isotope signatures) compilation of U-Pb geochronological data as regards and their host rocks, thus provides information on both magmatic events in these two belts. The objectives are possible provenance areas for the sedimentary basins (1) to facilitate access to available geochronological and maximum ages for sedimentation (Fedo et al. 2003; literature, (2) to display the distribution of magmatism Morton et al. 2005; Veevers et al. 2005). along the western margin of Baltica, and (3) to support 268 Bingen, B. & Solli, A. NORWEGIAN JOURNAL OF GEOLOGY

Fig. 1. Sketchmap of the Sveco- norwegian and Caledonian belts with location of the main tecto- nostratigraphic entities discussed in the text.

Z

interpretations of detrital zircon provenance studies in large magmatic bodies were selected as well as data on North Atlantic regions. small bodies (dykes, sills, pegmatites) and leucosomes with enough magma segregation to be sampled separately. Literature sources include journal articles, Method geological survey reports, and a few PhD theses forming part of the commonly cited literature (e.g. Berglund U-Pb geochronological data recording magmatic events 1997). A few classical abstracts, the contents of which in magmatic rocks or metamorphosed magmatic rocks have been presented during field excursions or recorded were compiled from the literature listed in Table 1 (see on geological maps are also included (e.g. Dahlgren et al. electronic supplement at www.geologi.no/njg). The 1990a; Handke et al. 1995; Zwaan & Tucker 1996). Some compilation includes ca. 650 selected samples of (meta) pioneering studies have been omitted or only partially plutonic and (meta)volcanic rocks in the Sveconorwegian listed, if the data are superseded or considered unreliable and Caledonian belts, as updated in July 2009. Data on following today’s standard (discordant zircon analyses, NORWEGIAN JOURNAL OF GEOLOGY Geochronology of magmatism in the Caledonian and Sveconorwegian belts of Baltica 269 few analyses/ samples, alternative interpretations during the Mesoproterozoic, whilst models featuring possible; Daly et al. 1991; O’Nions & Baadsgaard 1971; terrane accretion during the Sveconorwegian orogeny Welin et al. 1982; Wielens et al. 1981; Wilson et al. 1983). are equally possible (discussion in Bingen et al. 2008c). A few Lu-Hf, Re-Os and Sm-Nd dates are listed in Table 1 The Sveconorwegian orogeny is bracketed between ca. for completeness. Samples of clastic (meta)sediments for 1140 and 900 Ma and has been divided into four main which detrital zircon analyses are available are compiled phases (Bingen et al. 2008c). The Arendal phase is in Table 2 (see electronic supplement at www.geologi.no/ interpreted as a local collision between the Telemarkia njg), using the same general method. and Idefjorden Terranes and involved granulite-facies metamorphism in the Bamble Terrane at 1145-1124 Ma Localisation of the easternmost extent of Sveconorwegian (Bingen et al. 2008b; Cosca et al. 1998). The Agder phase deformation is a matter of discussion (Wahlgren et al. corresponds to the main Sveconorwegian continent- 1994). Consequently, all samples located along a broad continent collision and saw tectonic imbrication and zone corresponding to the Sveconorwegian Frontal major crustal thickening between ca. 1050 and 980 Ma. Deformation Zone (SFDS, north of lake Vättern) The Falkenberg phase corresponds to final convergence and Protogine Zone (PZ, south of lake Vättern) were in the belt, as testified by eclogite-facies metamorphism compiled together with samples located west of these in the Eastern Segment at 972 ±14 Ma (Johansson structures (Fig. 2). Samples of the Sveconorwegian-aged et al. 2001; Möller 1998). Convergence was followed Blekinge-Dalarna Dolerites are listed in Table 1, though by relaxation and gravitational collapse of the belt. generally situated east of the Sveconorwegian belt. For the Unroofing and extension is recorded up to ca. 870 Ma Caledonian belt, the Caledonian Front is unambiguously (Mulch et al. 2005). defined (Roberts & Gee 1985). The Barents Sea Region was compiled as part of the Caledonides. The ca. 350 km wide Caledonian belt results from Paleozoic closure of the Iapetus Ocean followed by the Table 1 includes for each entry the accepted or most Scandian collision between Baltica and Laurentia, partly reasonable tectonostratigraphic unit hosting the dated reworking the Sveconorwegian belt. The Caledonian belt rock, a short characterization of the lithology and has a nappe architecture (Roberts & Gee 1985; Roberts locality, some key data descriptors (mineral analysed, 2003). The nappes are traditionally grouped into four best age selection method, analytical method) and the main tectonostratigraphic levels, the Lower, Middle, sample coordinates. In Sweden, the coordinates are Upper and Uppermost Allochthons (Figs. 1, 2). The listed in the Swedish National grid (RT90), if reported Lower and Middle Allochthons are regarded as endemic in this way by the authors. Otherwise they are listed, to Baltica, while the Upper and Uppermost Allochthons converted or estimated in the UTM(WGS84) projection. All are exotic and accreted during the Caledonian orogeny. coordinates are converted in latitude-longitude (decimal Two of the large nappe complexes have disputed degrees). The precision of the coordinates is described by ancestries. These are the Kalak and Seve Nappes variably a qualifier. Tables 1 and 2 are illustrated in sketchmaps attributed to the Middle and Upper Allochthons (Corfu (Figs. 2, 3, 8; fig.8: see electronic supplement at www. et al. 2007; Gee et al. 2008; Kirkland et al. 2007b; Roberts geologi.no/njg) and age cumulative probability diagrams 2007). For the purpose of clarity, they are compiled (Figs. 4-7). separately in Table 1. Windows of crystalline rocks below the nappes are exposed along the whole length of the Caledonides and interpreted as parautochthonous Tectonostratigraphic framework exposure of the Fennoscandian Shield basement (e.g. Olesen et al. 1997). The Caledonian orogeny took place The Sveconorwegian and Caledonian belts have distinct between ca. 505 and 390 Ma. Several Cambro-Ordovician architectures, partly as a result of the distinct present- amphibolite- to eclogite-facies tectonometamorphic day level of exposure and erosion. The ca. 550 km wide events are detected in the Seve Nappes and the Upper Sveconorwegian belt is the product of polyphase collision to Uppermost Allochthons between ca. 505 and 435 between Baltica and another major continental plate at Ma and record progressive closure of the Iapetus ocean the end of the Mesoproterozoic. The belt is divided into and accretion of microcontinents to the margin of five continental blocks, separated by steep, approximately Baltica or Laurentia (Barnes et al. 2007; Brueckner & orogen-parallel, shear zones. These blocks are the Van Roermund 2007; Corfu et al. 2003b; Essex et al. parautochthonous Eastern Segment in the east, and 1997; Mørk et al. 1988; Yoshinobu et al. 2002). The four allochthonous terranes towards the west, namely main Scandian continent-continent collision involved the Idefjorden, Kongsberg, Bamble and Telemarkia subduction of the Baltica basement to high and ultra- Terranes (Fig. 1; recent reviews in Bingen et al. 2008a, high pressure eclogite-facies conditions between 430 and c; Bogdanova et al. 2008). The large Telemarkia Terrane 400 Ma (Bingen et al. 2004; Cuthbert et al. 2000; Glodny is further divided into several “sectors”: the Rogaland- et al. 2008; Griffin & Brueckner 1985; Root et al. 2004; Vest Agder, Suldal, Hardangervidda, and Telemark Terry et al. 2000; Tucker et al. 2004) and thrusting of sectors. Though most available evidence supports the nappes (e.g. Fossen & Dunlap 1998). After ca. 400 Ma, view that the four terranes were part of Fennoscandia high-pressure rocks were exhumed, the stress regime 270 Bingen, B. & Solli, A. NORWEGIAN JOURNAL OF GEOLOGY

Fig. 2. Tectonostratigraphic sketchmap of the Sveconorwegian and Caledonian belts following Koistinen et al. (2001) with distribution of dated magmatic rocks compiled in Table 1. NORWEGIAN JOURNAL OF GEOLOGY Geochronology of magmatism in the Caledonian and Sveconorwegian belts of Baltica 271 having switched to extensional and intermontane Paradoxically, comparatively little of the typical sedimentary basins developed in the hanging wall of Svecofennian orogenic magmatism is documented in detachment shear zones (Andersen 1998; Kylander-Clark the Caledonian windows. In the Lofoten, Vesterålen et al. 2008; Osmundsen & Andersen 2001). There is and Rombak windows, a few plutons, including a abundant literature to document these processes. charnockitic pluton, are dated between 1940 and 1860 Ma (Fig. 4e; Corfu 2004a; Romer et al. 1991). The bulk of the felsic magmatism in the Nordland, Lofoten Review of U-Pb data on magmatic events and Rombak windows occurred during a short-lived magmatic event dated between 1805 and 1770 Ma (Figs. Archaean (>2500 Ma) 3a, 4e; Corfu 2004a; Skår 2002). This plutonism is coeval to the Revsund granites, forming extensive outcrops east The Fennoscandian shield is build around an Archaean of the Caledonian Front, and generally considered to core exposed in the northeast as the Karelian and be part of the Transcandinavian Igneous Belt (Högdahl Murmansk cratons (Daly et al. 2006; Gorbatschev & et al. 2004). Southwards, this pulse is recorded in the Bogdanova 1993; Gaal & Gorbatschev 1987; Hölttä et Central Norway Basement Window (1818-1795 Ma; al. 2008). This core is surrounded by Palaeoproterozoic Schouenborg et al. 1991), and northwards in the West to Mesoproterozoic orogenic domains, increasingly Troms Basement Complex and Fagervik Complex younger towards the southwest (Bogdanova et al. 2008; underlying the Kalak Nappes (1792-1767 Ma; Corfu Korja et al. 2006). The crystalline basement windows et al. 2003a; Kirkland et al. 2008; Kullerud et al. 2006). in the Caledonides mirror this general trend. Archaean Circa 1800-1776 Ma felsic plutonism is also detected rocks and Archaean protoliths are positively identified in the Akkajaure, Blaik and Skárjá (Seve) nappes (Figs. in coastal windows in the northern Caledonides in 4b, c). These are interpreted as crystalline sheets of the Vesterålen islands and the West Troms Basement Fennoscandia basement transported in Lower and Complex (Figs. 1, 3a, 4e). Mainly tonalitic gneisses in Middle Allochthon positions (Greiling et al. 2002; these areas range from 2885 to 2635 Ma (Bergh et al. Rehnström & Corfu 2004). 2007; Corfu 2007; Zwaan & Tucker 1996). Southwards, in the Central Norway Basement Window Palaeoproterozoic (2500-1600 Ma) and the West Norway Gneiss Complex, the main felsic crust-forming magmatism is significantly younger and The Archaean core of the Fennoscandian shield hosts defines a narrow interval between 1686 and 1621 Ma Palaeoproterozoic mafic magmatic suites dated between with a frequency maximum at 1660 Ma (Fig. 4d; Skår & ca. 2510 and 2440 Ma in the Kola penisula and in Karelia Pedersen 2003; Tucker et al. 1990b). Coeval magmatism, (Amelin et al. 1995). In the Caledonian windows, slightly between 1694 and 1630 Ma is widespread in the Middle younger mafic dykes, dated at 2403 Ma, are exposed in Allochton Jotun and Dalsfjord Nappes (Figs. 3a, 4c; the Archaean West Troms Basement Complex (Kullerud Corfu & Andersen 2002; Lundmark et al. 2007; Schärer et al. 2006). They are followed by mafic sills at 2221 1980), and locally detected in the Seve Nappes (Fig. 4b; Ma (Fig. 4e; Bergh et al. 2007). No significant felsic Zachrisson et al. 1996). magmatism is recorded in the Fennoscandian Shield between ca. 2500 and 2100 Ma (e.g. Claesson et al. 1993) In the Eastern Segment and the easternmost marginal and it is equally undetected in the Caledonian windows. zone of the Sveconorwegian belt, Palaeoproterozoic, mainly felsic magmatism ranges from 1855 to 1601 After the 2200-2060 Ma Lomagundi-Jatuli carbon isotope Ma with the largest number of dates recorded between event (Melezhik et al. 2007), the Svecofennian orogenic 1797 and 1640 Ma and distributed in three major period corresponds to the voluminous formation of pulses peaking at 1795, 1690 and 1675 Ma (Figs. 3a, 4i; continental crust, accretion of microcontinents and Appelquist et al. 2008; Bingen et al. 2008c; Connelly et volcanic arcs, and continental collision in Fennoscandia, al. 1996; Möller et al. 2007; Rimša et al. 2007; Söderlund between 1920 and 1790 Ma (Korja et al. 2006; Lahtinen et al. 1999; 2002; 2008b). The Eastern Segment is et al. 2008; Nironen 1997). Active margin magmatic interpreted as a Sveconorwegian parautochthonous activity started at around 2020 Ma, and magmatism domain exposing reworked lithologies of the peaked at around 1910-1870 Ma. Post-collisional granite Transcandiavian Igneous Belt (Möller 1998; Möller et al. magmatism took place between 1820 and 1750 Ma. 2007; Persson et al. 1995; Söderlund et al. 1999; Wahlgren Overlapping in time with this event, voluminous, mainly et al. 1994). Sveconorwegian deformation gradually felsic alkali-calcic magmatism of the N-S trending increases westward from localised deformation along Transcandinavian Igneous Belt (TIB; Fig. 1), reflects shear zones in the Sveconorwegian Frontal Deformation renewed active margin activity along the western margin Zone and the Protogine Zone to penetrative amphibolite- of the Svecofennian belt (review in Högdahl et al. 2004). to granulite-facies deformation. Magmatism attributed to the Transcandinavian Igneous Belt is episodic and ranges from ca. 1850 to 1650 Ma. A linkage between the Eastern Segment of the Sveconorwegian belt and the West Norway Gneiss 272 Bingen, B. & Solli, A. NORWEGIAN JOURNAL OF GEOLOGY

Fig. 3a. Distribution of dated magmatic rocks compiled in Table 1, color-coded for important age groups: a) rocks older than 1400 Ma NORWEGIAN JOURNAL OF GEOLOGY Geochronology of magmatism in the Caledonian and Sveconorwegian belts of Baltica 273

Fig. 3b. Distribution of dated magmatic rocks compiled in Table 1, color-coded for important age groups: b) rocks younger than 1400 Ma. 274 Bingen, B. & Solli, A. NORWEGIAN JOURNAL OF GEOLOGY

Fig. 4. Cumulative Phanerozoic Neoproterozoic Mesoproterozoic Palaeoproterozoic Archaean probability diagrams for magmatic rocks Upper-Uppermost Allochthons in the Caledonian A 106 magmatic rocks belt (A-E) and Sveco- norwegian belts (F-I). Data sources in Table 1. For the purpose of Kalak-Seve Nappes presentation, a mini- B 45 magmatic rocks mum nominal error of 2 Ma is used in this figure for samples younger than 1000 Ma and 4 Ma for Lower-Middle Allochthons C 40 magmatic rocks older samples.

Basement windows in Caledonides, South: Central Norway Basement Window + West Norway Gneiss Complex D 48 magmatic rocks

Basement windows in Caledonides, North Nordland, Rombak, Lofoten, Vesterålen + West Troms Basement Complex E 46 magmatic rocks

Telemarkia terrane F 114 magmatic rocks

Bamble + Kongsberg terranes G 16 magmatic rocks

Idefjorden terrane H 100 magmatic rocks

robability

e p Eastern Segment + Sveconorwegian Frontal Deformation Zone + Protogine zone I 119 magmatic rocks

Cumulativ

0 500 1000 1500 2000 2500 Ma

Complex in the Caledonides has been suggested for Calymmian (1600-1400 Ma) a long time (Gorbatschev & Bogdanova 1993). Data The Idefjorden Terrane, west of the Mylonite Zone, available today, though not extremely abundant for hosts abundant plutonic and volcanic rocks with calc- the West Norway Gneiss Complex, demonstrate alkaline geochemical signatures typical of active margin Palaeoproterozoic magmatism in the two domains geotectonic settings (Brewer et al. 1998). They range with overlapping pulses at 1690-1685 Ma and 1675- from 1659 to 1517 Ma with a general younging trend 1660 Ma, and consequently support this link (Figs. 4d, towards the west within this terrane (Andersen et al. i). Nevertheless, the 1650-1600 Ma magmatism is not 2004a; Bingen et al. 2005b; Åhäll & Connelly 2008). common in the Eastern Segment while it is common in Four significant modes at ca. 1610, 1590, 1555 and the West Norway Gneiss Complex. 1545 Ma are apparent, the two first ones including the Åmal volcanic suite and the Göteborg plutonic suite and the two others the Hissingen plutonic suite (Fig. 3a, 4h; Åhäll & Connelly 2008). These rocks were assembled at the margin of Fennoscandia during the NORWEGIAN JOURNAL OF GEOLOGY Geochronology of magmatism in the Caledonian and Sveconorwegian belts of Baltica 275

Gothian orogeny. Though geochronological data give Ma, called the Jönköping Anorthositic Suite, is described evidence for only one Gothian high-grade metamorphic by Brander and Söderlund (2009). phase at ca. 1540 Ma (Bingen et al. 2008b; Åhäll & Connelly 2008), a variety of models has been proposed Ectasian (1400-1200 Ma) for the Gothian orogeny, ranging from one to several accretionary events (Andersen et al. 2004a; Åhäll et Most geologic models picture Fennoscandia in an al. 2000; Åhäll & Connelly 2008). The typical Gothian extensional stress regime between ca. 1400 and 1200 orogenic magmatism is lacking in the Eastern Segment. Ma. The shield is the location of episodic continental One exception to this observation is the extensive magmatism of moderate volume (Fig. 3b). In the Eastern monzogranitic Hinneryd pluton dated at 1548 ±10 Ma, Segment of the Sveconorwegian belt, a suite of granite the significance of which is poorly understood (Lindh to charnockite plutons intruded between 1399 and 1359 1996). Ma, for example the Varberg charnockite suite at 1399 Ma (Fig. 4i; Andersson et al. 1999; Christoffel et al. 1999; To the west of the Oslo rift, the comparatively small Åhäll et al. 1997). In the Idefjorden Terrane, a distinctly Bamble and Kongsberg Terranes are characterized younger bimodal plutonic suite, called the Kungsbacka by plutonic suites formed between 1572 and 1460 suite, is dated, between 1366 and 1304 Ma (Fig. 4h; Ma (Fig. 4g; Andersen et al. 2004a; deHaas et al. 2002; Austin Hegardt et al. 2007; Kiel et al. 2003), possibly Starmer 1991). West of them, the Telemarkia Terrane including younger 1294 Ma dolerites (Söderlund et al. is characterized by a main crust-forming magmatic 2008a). In the Telemarkia Terrane, a dolerite dyke at 1347 event between 1555 and 1459 Ma, peaking at exactly Ma records an uncommon event of mafic magmatism 1500 Ma (Figs. 3a, 4f; Bingen et al. 2005b). The 1500 coeval with the Kungsbacka suite (Corfu & Laajoki Ma magmatism includes a large sequence of bimodal 2008). volcanic rocks, the Rjukan Group and correlative supracrustal rocks (Bingen et al. 2005b; Dahlgren et al. The extensive Central Scandinavian Dolerite Group 1990a; Dons 1960; Laajoki & Corfu 2007), as well as a defines three mafic magmatic pulses in the interval variety of felsic plutonic rocks commonly displaying between 1271 and 1247 Ma in continental Fennoscandia calc-alkaline geochemical signatures. (Söderlund et al. 2006). Coeval mafic gabbro/dolerite magmatism, but also felsic plutonism, is recorded in Between ca. 1470 and 1420 Ma, Fennoscandia was the West Norway Gneiss Complex (1255-1251 Ma; Fig. affected by orogenic events known as the Hallandian 4d; Austrheim et al. 2003; Robinson et al. 2008), and in the Eastern Segment (Hubbard 1975; Möller et al. Middle Allochthon Jotun and Lindås nappes (1257-1237 2007) and the Danopolonian east and south of the Ma; Fig. 4c; Bingen et al. 2001b; Lundmark et al. 2007). Protogine Zone (Bornholm and concealed basement In the Telemarkia Terrane, overlapping 1285-1259 Ma of Lithuania and Poland; Bogdanova et al. 2008). The bimodal plutonism and volcanism (Sæsvatn-Valldal dynamics of these events are poorly understood. In the and Iveland-Gautestad complexes) are associated with Eastern Segment, felsic pegmatites and leucosomes the formation of small scale sedimentary basins (Fig. are common. They are dated between 1473 and 1409 4f; Bingen et al. 2002; Pedersen et al. 2009). A younger Ma and are linked to Hallandian crustal melting (Fig. bimodal magmatic event between 1221 and 1204 Ma is 4i; Christoffel et al. 1999; Söderlund et al. 2002). spatially related to the Protogine Zone (Fig. 4i; review in Magmatism in the 1470-1420 Ma interval over Söderlund & Ask 2006). Fennoscandia is reviewed by Brander and Söderlund (2009). East and south of the Protogine Zone, this Stenian (1200-1000 Ma) – Tonian (1000-850 Ma) magmatism includes monzogranite to granite plutons typified by the 1445 ± 11 Ma synkinematic Karlshamn Stenian-Tonian magmatism is described relative to granite pluton in SE Sweden (Cecys & Benn 2007; Sveconorwegian orogenic phases (Fig. 5; Bingen et Kornfält & Vaasjoki 1999). In the Eastern Segment and al. 2008c). The Bamble Terrane hosts the 1198-1178 the Protogine Zone, a few coeval granite plutons were Ma Tromøy gabbro-tonalite complex, interpreted emplaced between 1458 and 1442 Ma (Fig. 4i; Cecys et as the remnants of a pre-Sveconorwegian island arc al. 2002; Johansson et al. 1993b). Northwards, outside accreted at an early stage of the Sveconorwegian of the area affected by the Hallandian-Danopolonien orogeny (Fig. 4g; Andersen et al. 2004a; Knudsen & orogenies, 1466-1455 Ma continental magmatism is Andersen 1999). In the Telemarkia Terrane, abundant mafic in composition (Söderlund et al. 2005). It is mainly pre-Sveconorwegian felsic plutonism between 1228 made up of mafic dykes and gabbroic plutons exposed in and 1184 Ma was followed by bimodal plutonism and the Eastern Segment (Brander & Söderlund 2009), the volcanism in the interval between 1169 and 1134 Ma Idefjorden Terrane (Åhäll & Connelly 1998), and also (Figs. 3b, 4f; Andersen et al. 2007b; Bingen et al. 2003; in the Caledonides in the West Norway Gneiss Complex Heaman & Smalley 1994; Laajoki et al. 2002; Pedersen window and in the Jotun and Dalsfjord Nappes of the et al. 2009; Zhou et al. 1995). In the Telemark sector,the Middle Allochthon (Figs. 4c, d; Corfu & Emmett 1992; bimodal volcanism is associated with sedimentary basins Corfu & Andersen 2002). One anorthosite suite at 1455 showing common unconformities (Laajoki & Lamminen 276 Bingen, B. & Solli, A. NORWEGIAN JOURNAL OF GEOLOGY

Fig. 5. Cumulative probability diagrams for magmatic rocks between 1400 and t 900 Ma in the entire Sveconorwegian belt, S v e c o n o r w e g i a n Frontal Deforma- tion Zone (SFDZ) and Protogine zone, relative to Sveco- norwegian orogenic events. Data sources in Table 1.

2006). This magmatism terminated at 1130 Ma with Terrane (Fig. 4c). In the West Norway Gneiss Complex, the intrusion of the alkaline Morkheia monzonite suite, large post-collisional Sveconorwegian granite plutons close to the Bamble-Telemark boundary (Heaman & as well as minor pegmatites and felsic dykes crystallized Smalley 1994). The 1169-1134 Ma bimodal magmatism between 976 and 942 Ma (Fig. 4d; Corfu 1980; Skår & and associated sedimentary basins possibly record Pedersen 2003; Tucker et al. 1990b). These are situated extensional or transtensional regimes, and have been southwest of a conceptual line (SF in Fig. 1, NW-SE variably interpreted in the context of a continental arc, trending but not corresponding to any known field continental back-arc or Basin and Range setting (Bingen structure) that has been inferred as the northeasternmost et al. 2003; Brewer et al. 2004). limit of Sveconorwegian overprint and a possible extension of the Sveconorwegian Frontal Deformation Sveconorwegian orogenic or syn-collisional magmatism Zone. In the Middle Allochthon Lindås and Jotun (Fig. 5) is represented by the 1051-1049 Ma high-K calc- nappes, anorthosite-mangerite suites are dated between alkaline Feda suite, in the Telemarkia Terrane (Bingen 965 and 951 Ma and pegmatites range from 950 to 892 et al. 1993; Bingen & van Breemen 1998). It possibly Ma (Fig. 4c; Bingen et al. 2001b; Lundmark et al. 2007; reflects a final subduction episode and was followed Lundmark & Corfu 2008). by granodioritic to granitic magmatism between 1035 and 1023 Ma in the Telemarkia Terrane (Fennefoss Importantly, minor granitic plutons, intruded between augen gneiss and other granitoids) and by rare-mineral 981 and 973 Ma, have been reported recently in the pegmatites in the Idefjorden Terrane (Figs. 4 f-h; Bingen lower part of the Kalak Nappes (Fig. 4b; Kirkland et al. 1993; Bingen & van Breemen 1998; Möller et al. et al. 2006). These rocks attest to Sveconorwegian- 2002; Pedersen et al. 2009; Romer & Smeds 1996). Syn- Grenvillian magmatism in the northern Caledonides. collisional magmatism was followed by post-collisional Interpretation of these rocks and their correlation with magmatism (Fig. 5). The oldest dated but arguably known Sveconorwegian-Grenvillian suites in Laurentia post-collisional pluton is the 989 ±9 Ma Grimstad and Baltica is a matter of speculation (Corfu et al. 2007; granite in the Bamble Terrane (Kullerud & Machado Kirkland et al. 2006). 1991). Post-collisional plutonism in the Idefjorden, Telemarkia and Bamble Terranes ranges in age from Cryogenian (850-635 Ma) - Ediacaran (635-542 Ma) 971 to 914 Ma (Figs. 4 f-I; Andersen et al. 2007b; Bingen et al. 2006; Hellström et al. 2004; Pasteels et al. 1979) It is one of the intrinsic characteristics of Fennoscandia and includes the prominant 932-920 Ma anorthosite- to be poor in Cryogenian to Ediacaran magmatism. mangerite-charnockite suite in Rogaland (Schärer et al. After the Sveconorwegian orogeny, Fennoscandia was in 1996). East of the Sveconorwegian belt, the 978-946 Ma extension. In the Sveconorwegian belt, dated magmatic Blekinge-Dalarna dolerites form a dyke swarm parallel rocks are the 616 Ma Egersund dolerites (Bingen et al. to the Sveconorwegian Frontal Deformation Zone 1998) and the 583 Ma Fen carbonatite province (40Ar/39Ar (Söderlund et al. 2005). They are clearly related to the age of 583 ±15 Ma not listed in Table 1; Meert et al. 1998). Sveconorwegian post-collisional evolution. Poorly dated dolerite dykes are well known in the Middle Allochthon Särv nappes (Claesson & Roddick 1983). Sveconorwegian magmatic rocks are detected at different Cryogenian to Ediacaran magmatic and metamorphic tectonostratigraphic levels in the Caledonides. In the events are increasingly documented in the Seve and Middle Allochthon of mid-Norway, a characteristic Kalak Nappes. In the upper part of the Kalak Nappes, 1190-1189 Ma augen gneiss sheet is exposed (Handke minor granite and pegmatite bodies and leucosomes et al. 1995), demonstrating northward extension of the formed between 876 and 825 Ma and between 711 and 1228-1184 Ma magmatism typical of the Telemarkia 680 Ma (Figs. 3b, 4b; Corfu et al. 2007; Kirkland et al. NORWEGIAN JOURNAL OF GEOLOGY Geochronology of magmatism in the Caledonian and Sveconorwegian belts of Baltica 277

2006; 2008). These features have been put forward as an Allochthons. The only notable exception is the Halti argument for an exotic origin of the Kalak Nappes (Corfu Igneous Complex in northern Norway and Finland et al. 2007; Kirkland et al. 2007b). Also in the upper part dated between 457 and 434 Ma (Andréasson et al. 2003; of the Kalak Nappes, the large Seiland Igneous Province Vaasjoki & Sipilä 2001) and controversially attributed corresponds to a short-lived, mainly gabbroic magmatic to the Kalak Nappes (Andréasson et al. 2003). Ignoring event between 571 and 561 Ma (Roberts et al. 2006), this exception, the distribution of magmatism implies followed by syenite pegmatites at 531-523 Ma (Figs. 3b, that Scandian thrusting of the Upper and Uppermost 4b; Pedersen et al. 1989). In the Seve nappes, an 845 Allochthons onto the Baltica margin postdates the end Ma granite pluton is reported (Paulsson & Andréasson of the Cambro-Silurian magmatism. The youngest dated 2002) and a sheeted dyke complex, dated at 608 Ma, is plutons are the 431 ±4 Ma Olaberget trondhjemite for traditionally taken as a landmark for opening of the the Upper Allochthon (Fig. 6 b, Trondheim Nappes; Iapetus ocean along the Neoproterozoic thinned passive Nilsen et al. 2007) and a 424 ±1 Ma porphyritic granite in margin of Baltica (Svenningsen 2001). the Uppermost Allochthon (Fig. 6 a; Helgeland Nappes; Barnes et al. 2007). Cambrian (542-488 Ma) – Ordovician (488-444 Ma) – Silurian (444-416 Ma) Devonian (416-359 Ma)

Cambrian to Silurian magmatism is abundant in the One of the remarkable features of the Caledonian belt is Upper and Uppermost Allochthons of the Caledonides the lack of significant syn- to post-collisional Scandian (Figs. 3b, 4a, 6). This magmatism is varied and includes magmatism, though minor pegmatite bodies and felsic not only supra-subduction ophiolite complexes and dykes are common (Figs. 4b-e). They range from 436 to oceanic volcanic arc magmatism, but also anatectic 391 Ma in the Kalak, Seve and Jotun Nappes (Lundmark (S-type) granites (e.g. Grenne et al. 1999; Pedersen & & Corfu 2007; Nordgulen et al. 2002), and from 409 to Dunning 1997; Slagstad 2003). It reflects the formation 390 Ma in the Caledonian windows, where they are of oceanic basins and microcontinents in the Iapetus generally associated with extensional structures (Krogh ocean. In the Upper Allochthon, it ranges from 495 to in Robinson et al. 2008; Tucker et al. 2004). 431 Ma with a main age group peaking at 438 Ma and two age groups at 495-470 and 461-456 Ma (Fig. 6b; Carboniferous (359-299 Ma) – Permian (299-251 Ma) Corfu et al. 2006; Dunning & Pedersen 1988; Kirkland et al. 2005; Meyer et al. 2003; Nilsen et al. 2007; Formation of the Oslo rift was initiated in the late Roberts et al. 2002). In the Uppermost Allochthon, it Carboniferous at around 310 Ma and developed during extends between 497 and 424 Ma (Fig. 6a; Barnes et the Permian up to ca. 250 Ma (Olaussen et al. 1994). It al. 2007; Nordgulen et al. 1993; Yoshinobu et al. 2002). is coeval with intrusion of dolerites and basalts in SW The youngest known ophiolite complex, the Solund- Sweden (e.g. Hunneberg basalts) and Skagerrak. The Stavfjorden ophiolite, records the formation of a late oldest recorded event of mafic volcanism in the Oslo oceanic basin in Iapetus at 443 ±3 Ma (Dunning & rift is dated at 300 Ma (Corfu & Dahlgren 2008). Three Pedersen 1988). The Cambro-Silurian magmatism is younger plutonic complexes are dated between 299 and a distinguishing feature of the Upper and Uppermost 277 Ma (Dahlgren et al. 1996; Pedersen et al. 1995).

Fig. 6. Cumulative probability diagrams Carboniferous Devonian Silurian Ordovician Cambrian Ediacaran for magmatic rocks 430 479 in the Uppermost 448 Allochthon (a) and 497 ±2 Ma Uppermost Allochthon 424 ±1 Ma Upper Allochthon (b) A 41 magmatic rocks of the Caledonides. Data sources in Table 1.

Scandian 438

robability Phase

495 ±3 Ma Upper Allochthon B 64 magmatic rocks 431 ±4 Ma

Cumulative p

300 350 400 450 500 550 Ma 278 Bingen, B. & Solli, A. NORWEGIAN JOURNAL OF GEOLOGY

Discussion previously undated magmatic suites are characterized (e.g. Kirkland et al. 2006), episodic events of magmatism Limitations become increasingly apparent and defined with improved accuracy. Available data carry five inherent limitations for characterizing the geochronology of magmatism and The compilation illustrates important differences the distribution of magmatic sources for detrital zircons. in the distribution of magmatism between the (1) As is apparent from the distribution map (Fig. 2), Sveconorwegian and Caledonian belts (Figs. 7 g, h). The vast areas of the exposed (onshore) Caledonian and Sveconorwegian orogeny reworked the southwestern Sveconorwegian belts remain under-explored, especially margin of Baltica at the end of the Mesoproterozoic. away from the coast. These areas constitute obvious It affected continental crust that grew during the targets for important future work. (2) Only a minority of Palaeoproterozoic and Mesoproterozoic mainly during published geochronological studies have been aimed at three major magmatic events of regional importance, all providing a balanced evaluation of exposed rock volumes of them probably reflecting active continental margin (e.g. Tucker et al. 1990b). Process-oriented research settings. These are the polyphase Transcandinavian commonly focuses on small magmatic bodies providing Igneous Belt magmatism mainly between 1805 and information on specific geologic or tectonic events (e.g. 1640 Ma, the 1660-1520 Ma magmatism assembled Lundmark & Corfu 2007). This scrutiny means that during the Gothian orogeny, and the 1550-1460 Ma comparatively minor and young magmatic rocks tend to magmatism forming the Telemarkia Terrane. This be overrepresented in the compilation. (3) For improved crust was the location for intermittent magmatism evaluation of source areas, a quantification of the rock over the entire time span between 1473 and 1130 Ma. volume represented by each (group of) data point(s) and The Sveconorwegian orogeny was a warm orogeny. of the amount of detrital zircon potentially liberated by Metamorphism has a high-temperature signature in the erosion of this rock volume should be performed. This western half of the belt (review in Bingen et al. 2008b, quantification is difficult to implement in any objective c) and abundant orogenic/syn-collisional (1051-1023 fashion at this stage of data coverage. Large magmatic Ma) and post-collisional (971-914 Ma) magmatism was bodies may be thin or zircon poor (e.g. anorthosites; generated (Fig. 5). Available geochronological data thus Schärer et al. 1996), and small magmatic bodies may demonstrate that erosion of magmatic rocks exposed reflect an important magmatic event unexposed today. in the Sveconorwegian belt can have produced a whole Strictly speaking, zircon-free mafic magmatism dated range of Palaeoproterozoic to Mesoproterozoic detrital by means of baddeleyite U-Pb geochronology is not a zircons ranging in age from ca. 1800 to 900 Ma (Figs. 5, source for detrital zircons. Nevertheless, the argument 7h). The only clear gap in the record matches the start of can be made that most magmatic events are associated the Sveconorwegian orogeny (Arendal phase) between with zircon-bearing felsic facies. (4) In typical detrital 1130 and 1060 Ma (Figs. 5, 7h). zircon studies, between 10 and 100 analyses of zircons are performed, each crystal being analysed once. If an The Caledonian orogeny reworked an overlapping analysis is reasonably concordant (typically <10%), it segment of the same margin of Baltica. The basement is validated and interpreted to represent the magmatic of this margin is exposed in windows and in tectonic source of this crystal. The accuracy of this estimate slivers in the Lower to Middle Allochthon. It includes is not equivalent to the accuracy generally obtained Archaean crust and Palaeoproterozoic felsic crust on magmatic rocks when the age is derived from a produced during two main magmatic events related to pool of analyses. So, and despite all other statistical the Transcandinavian Igneous Belt between 1805 and considerations (Andersen 2005; Morton et al. 1996), 1770 and between 1686 and 1621 Ma. Mesoproterozoic direct links between clastic material and magmatic intrusions are rare while Sveconorwegian intrusions sources are difficult to demonstrate geochronologically ranging from 976 to 892 Ma are present in the south with methods generally applied today. (5) Last but not of the belt. The Caledonian orogeny took place after least, only one data point is sufficient to establish the the Neoproterozoic era, which was characterized by existence of a magmatic event, whereas the absence of an little continental growth along this margin. Some event is difficult to demonstrate. Neoproterozoic magmatism ranging from 981 to 561 Ma is present in the Kalak and Seve Nappes of Episodic magmatism disputed ancestry. Caledonian continental growth was significant. It involved accretion of Ediacaran to Silurian The compilation illustrates the episodic nature of microcontinents formed in the Iapetus ocean. These are magmatism along the western margin of Baltica. exposed in the Upper and Uppermost Allochthons and Publication of geochronological U-Pb datasets are characterized by Cambro-Silurian magmatism (Fig. commonly concludes that known magmatic events are 6). The Caledonian orogeny was a cold orogeny involving shorter-lived than estimated previously or divisible into high- to ultrahigh-pressure metamorphism in the Baltica short-lived pulses (e.g. Roberts et al. 2006; Söderlund basement (Cuthbert et al. 2000; Griffin & Brueckner & Ask 2006). Consequently, as data accumulate and as 1985) and absence of voluminous post-collisional NORWEGIAN JOURNAL OF GEOLOGY Geochronology of magmatism in the Caledonian and Sveconorwegian belts of Baltica 279

Fig. 7. Cumulative probability dia- grams for detrital zircons (concordance 90-110%) compa- red with the ones for magmatic primary zircon sources in the Caledonian and Sve- cononorwegian belts. s (A) Data from Mor- ton et al. (2008). (B) Data from Barnes et al. (2007). (C) Data from Kirkland et al. (2007b; 2008). (D) Data from Bingen et al. (2005a). (E) Data from Kirkland et al. (2008) and Bergh et al. (2007). (F) Data 1 sources listed in Table 2. (G, H) Data sour- ces in Table 1. SFDZ: Detrital zircons in basement S v e c o n o r w e g i a n windows Troms-Finnmark Frontal Deformation 2 sedimentary rocks, 78 analyses Zone. (I) Histogram of some 7170 detrital zircons from 40 major Detrital zircons in Sveconorwegian belt rivers, Australian 28 metasedimentary rocks dunes and Antarctic 566 analyses Palaeozoic sediments compiled and selec- ted by Campbell and Allen (2008).

magmatism. As a consequence of these characteristics, Palaeoproterozoic (2500-1940 Ma), Mesoproterozoic and erosion of magmatic rocks exposed in the Caledonides Neoproterozoic (Fig. 7g). provides a discontinuous distribution of detrital zircons, very distinct from those emanating from the Multicyclism Sveconorwegian belt. This distribution is characterized by a number of discrete modes ranging from Archaean The main obstacle to defining regional detrital zircon to Devonian, and reveals large gaps in the early signatures is multicyclic sedimentation of zircons. 280 Bingen, B. & Solli, A. NORWEGIAN JOURNAL OF GEOLOGY

Zircons are liberated from their primary magmatic of Scotland, supporting a Laurentian ancestry for these source rocks by erosion. They are robust to weathering sequences and the Uppermost Allochthon hosting them. and consequently can be transported and sedimented more than once before being captured in a sediment The earliest record of syn- to post-Caledonian erosion is sample collected for analysis. The link between clast and preserved in Devonian intermontane basins (Osmundsen source can be devious. & Andersen 2001; Osmundsen et al. 2006). Erosion of the Caledonian belt sampled various sediment sequences The Sveconorwegian belt exposes a variety of clastic in addition to the magmatic rocks. An evaluation of the sedimentary rocks, mainly in the Idefjorden and present-day discharge from Fennoscandia is presented in Telemarkia Terranes, deposited in Pre-Sveconorwegian Morton et al. (2008). Detrital zircon data from modern basins and in basins formed in the aftermath of the first sediments in rivers sourced in the Caledonides are Sveconorwegian orogenic phase (e.g. Heddal group). characterized by multimodal age distributions (Fig. 7a). Sveconorwegian post-collisional basins or foreland The frequency of detrital zircons in the interval between basins are unknown. Detrital zircons are dated in at least 1600 and 900 Ma is much higher than the frequency 28 samples distributed over this stratigraphy (Fig. 7f; of 1600-900 Ma magmatic rocks exposed today in the Åhäll et al. 1998; 2008; Andersen & Laajoki 2003; 2004a; Caledonides (Fig. 7g). The overall distribution shows a Andersen et al. 2004b; Bingen et al. 2001a; 2002; 2003; clear resemblance to the pooled distribution of samples 2005b; deHaas et al. 1999; Knudsen et al. 1997). Their from the Kalak Nappes (Kirkland et al. 2007b; 2008). ages largely overlap with those of magmatic rocks in the These observations reinforce the conclusion reached by Sveconorwegian belt. Nevertheless, on average, they are Morton et al. (2008) that erosion of the Caledonian belt older and major Archaean to Palaeoproteroic modes are is dominated by multicyclic zircons, sourced in (meta) recorded between 3250 and 2620 Ma (7.5%) and between sediment sequences in the Caledonian Allochthons. 2060 and 1840 Ma. As a result, erosion of these sediments will tend to shift the signature of the Sveconorwegian belt Archaean detrital zircons towards older ages, as defined exlusively by magmatic sources. In order to improve sedimentological models for Mesosoic to Cenozoic North Atlantic continental The Caledonian Allochthons are dominated by (meta) shelves, offshore sediment sequences are important sedimentary rocks. The Lower to Middle Allochthons targets for detrital zircon studies (Fonneland et al. 2004; contain thick Neoproterozoic sandstone sequences Morton et al. 1996, 2005; Røhr et al. 2008). One of the (Kumpulainen & Nystuen 1985; Nystuen et al. 2008) specific objectives of these studies is to test for Laurentia while the Upper and Uppermost Allochthons host vs. Baltica provenances in the sediments and if possible abundant Neoproterozoic to Palaeozoic sandstone to to be more specific. The two continents are known to shale sequences (Barnes et al. 2007; Grenne et al. 1999; have parallel geological evolutions (Bogdanova et al. Melezhik et al. 2002). Characterization of detrital 2008; Davidson 2008; Gorbatschev & Bogdanova 1993). zircons in these sequences is uneven. It includes one It is also known that the two continents collided during Neoproterozoic sample from the Osen-Røa Nappe the Caledonian orogeny. The Uppermost Allochthon, Complex in the Lower Allochthon (Bingen et al. 2005a), preserved today on the Baltica side of the Atlantic eleven Neoproterozoic samples in the Kalak Nappes ocean, has an accepted Laurentia ancestry (Roberts (Kirkland et al. 2007b; 2008), two samples from the 2003). Consequently, it is not a trivial task to distinguish Seve Nappes (Williams & Claesson 1987) and twelve between these two provenances. Neoproterozoic to Palaeozoic samples in the Helgeland Nappes in the Uppermost Allochthon (Barnes et A commonly used criterion for Laurentian provenances al. 2007). The sample from the Osen-Røa Nappe is is the presence of Archaean zircons, presumably shed dominated by Mesoproterozoic zircons with a main from Archaean cratons exposed in Greenland (Hölttä et mode at 1480 Ma (Fig. 7d). The samples from the Kalak al. 2008; Thrane 2002). On the Baltica side, the innermost Nappes are characterized by a few Archaean zircons, boundary fault system of post-Caledonian rifting (Mosar Palaeoproterozoic populations with a main mode at et al. 2002) corresponds approximately to the present day ca. 1650 Ma and a wide range of Mesoproterozoic water divide in Scandinavia. It can be considered as a first zircons with main modes at ca. 1520 and 1160 Ma (Fig. approximation to a minimum eastern boundary for the 7c). Detrital zircon populations in these samples are post-Caledonian catchment for clastic material drained compatible with partial sourcing in the Sveconorwegian to the North Atlantic shelves. The compilation of Table belt or other Grenvillian belts (Kirkland et al. 2007b; 1 shows that within this area, Archaean magmatic rocks 2008). The three Neoproterozoic sandstone samples from are present in the basement windows in the northern the Helgeland Nappes show a major Archaean mode Caledonides (Vesterålen and West Troms Basement (17% peaking at ca. 2740 Ma), and Palaeoproterozoic to Complex). In these windows, local Palaeoproterozoic Mesoproterozoic populations with a main mode at 1070 sedimentary rocks contain dominant populations of Ma (Fig. 7b). Barnes et al. (2007) point to the similarity Archaean detrital zircons (West Troms Basement and between these samples and the Dalradian Supergroup Fagervik complexes; Fig. 7e; Bergh et al. 2007; Kirkland et NORWEGIAN JOURNAL OF GEOLOGY Geochronology of magmatism in the Caledonian and Sveconorwegian belts of Baltica 281 al. 2008). As a consequence, post-Caledonian sequences contains a whole spread of Palaeo- to Mesoproterozoic offshore the northern Caledonides, i.e. in the Barents magmatic rocks ranging from ca. 1800 to 900 Ma, with and Nordland shelves, could host a significant Archaean three main felsic crust-forming events at 1797-1640 Ma component derived from Baltica. It is important to note (Eastern Segment), 1659-1517 Ma (Idefjorden Terrane) that the basement windows may not have been exposed and 1555-1459 Ma (Telemarkia Terrane) and only one shortly after the Caledonian orogeny. Nevertheless, clear quiescence between 1130 and 1060 Ma. the Lower and Middle Allochthons include slivers of orthogneiss that are coeval to gneisses exposed in the Magmatism recorded in the Caledonian belt is windows at similar latitudes (Figs. 4 c-e). Elsewhere in discontinuous in time. It includes mainly Archaean the Caledonian and Sveconorwegian belts, Archaean to Palaeoproterozoic magmatism in the reworked magmatic rocks are lacking. Archaean detrital zircons Fennoscandian crust (mainly 1805-1770 and 1686- are nevertheless abundant in Neoproterozoic sediments 1621 Ma), Neoproterozoic magmatism in the Seve and of the Uppermost Allochthon (Fig. 7b; Barnes et al. 2007) Kalak Nappes (mainly 571-560 Ma), and Cambro- and in Mesoproterozoic sediments from the Telemarkia Silurian magmatism in Iapetan oceanic basins and Terrane (Fig. 7f). These zircons are potentially recycled microcontinents accreted during the Caledonian in younger sediments. orogeny (497-424 Ma), and located in the Upper and Uppermost Allochthons. Erosion of the Caledonian belt The Mesoproterozoic testimony is dominated by erosion of Neoproterozoic to Silurian metasediment sequences exposed in the Allochthons, Detrital zircons collected in major rivers draining thus producing a polycyclic detrital zircon signature. modern continents and sand dunes worldwide show an age distribution with six modes corresponding to Paucity of Archaean detrital zircons remains a safe the presumed formation of supercontinents (Fig. 7i; general working hypothesis for Baltica provenances, Campbell & Allen 2008). These include Nuna between though a growing body of Archaean dates demonstrates 1950 and 1600 Ma, Rodinia between 1250 and 1000 Ma, the existence of Archaean crust (2885-2635 Ma) in Gondwana between 650 and 450 Ma and Pangea between the basement windows in the northern Caledonides 350 and 150 Ma. These modes can be interpreted as (Vesterålen and West Troms Basement Complex). planetary maxima of magmatic activity or as maxima in preservation (or any combination of these two factors; Tables and figure in electronic supplement: Campbell & Allen 2008; Hawkesworth et al. 2009). The Sveconorwegian orogeny contributed to the formation Table 1. Selection of U-Pb, Re-Os, Lu-Hf and Sm-Nd geochronolo- of Rodinia (Bogdanova et al. 2008; Li et al. 2008) while gical data recording magmatic events in the Sveconorwegian and Caledonian belts. the Caledonian orogeny contributed to the formation of Laurussia, one of the main blocks of Pangea (Cocks Table 2. Selection of clastic (meta)sediments, with published detrital & Torsvik 2006). The compilation in Table 1 shows that zircon U-Pb data. the Sveconorwegian belt hosts important magmatism at odds with the worldwide record (Figs 7 h-i). The Fig. 8. Tectonostratigraphic sketchmap of the Sveconorwegian and Mesoproterozoic magmatism peaking between 1610 Caledonian belts with offshore extrapolation, following Koistinen et and 1545 Ma in the Idefjorden Terrane and around 1500 al. (2001) and Sigmond (2002). The map shows the location of sam- Ma in the Telemarkia Terrane is younger than the main ples of dated magmatic rocks listed in Table 1, keyed with their entry mode of Palaeoproterozoic (Nuna-related) magmatism number in Table 1. (1950-1600 Ma). The Sveconorwegian belt thus carries an uncommon testimony of Mesoproterozoic continental growth. On a global scale, the Mesoproterozoic history is Acknowledgements the most specific signature of the Sveconorwegian belt P. Robinson and D. Roberts contributed to verify the compilation of data. A number of authors provided details about their sampling. C. G. (Bingen et al. 2005b), and this history should be recorded Barnes and A. Morton are thanked for constructive reviews and P. T. in detrital zircon populations derived from this belt. Osmundsen for editorial handling.

Conclusions References An updated compilation of geochronological data in the Sveconorwegian and Caledonian belts is a fundamental Åhäll, K.I. 1991: An investigation of the Proterozoic Stenungsund granitoid intrusion, southwest Sweden; conflicting geochrono- tool for picturing the distribution of magmatism and logical and field evidence. In: C.F. Gower, T. Rivers & B. Ryan, Eds. evaluating primary magmatic sources for detrital Mid-Proterozoic Laurentia-Baltica., 38, p. 117-129. Geological zircons along the western margin of Baltica. Association of Canada, special paper 38. Åhäll, K.I., Persson, P.O. & Skiöld, T. 1995: Westward accretion of the The Sveconorwegian belt carries a rich testimony of Baltic Shield: implications from the 1.6 Åmål-Horred Belt, SW Mesoproterozoic magmatism and continental growth. It Sweden. Precambrian Research 70, 235-251. 282 Bingen, B. & Solli, A. NORWEGIAN JOURNAL OF GEOLOGY

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