The Karlshamn pluton which intruded at ca. 1.45 Ga in southern Fennoscandia contains two major coeval suites. Both of these have A-type affinity and consist of metaluminous, ferroan, alkali-calcic, and very-high K (shoshonitic) granitic rocks. The two suites are geographically separated within the pluton, and form (semi)parallel trends on Harker-type diagrams. The Eastern suite comprises quartz monzodiorite, quartz monzonite and granite while the Western suite mainly consists of monzogranites. Both suites exhibit similar chondrite-normalized REE patterns with relatively steep LREE and flat HREE. Aluminium-in-hornblende barometric and zircon-saturation thermometric estimates show that both suites were crystallized at relatively high temperatures of 850-900 degrees C and low pressures of 0.33-0.43 GPa. Ion microprobe zircon dating from a monzonite of the Eastern suite yielded concordant to nearly concordant U-Pb isotopic compositions. The weighted average 207Pb/206Pb age is 1445 f 11 Ma (2 sigma, MSWD 1.2), interpreted to date magmatic crystallization. The complex zircons from a monzogranite in the Western suite showed somewhat more scatter and slightly younger ages, however, there are no signs of older inherited materials and no significant age differences between the core-like domains and the overgrowths. The cores yielded a weighted average 207Pb/206Pb age of 1431 f 20 Ma (2 sigma, MSWD 1.5) and the rims an age of 1424 f 19 Ma (2 sigma, MSWD 4.2). The overall age of the zircons from the Western suite is 1426 f 11 Ma (2 sigma, MSWD 2.6). The two major suites as well as related leucogranites and mafic enclaves that are present mainly in the Western suite have indistinguishable initial epsilon Nd values of-2.2 to-2.7.The Rb-Sr system shows some disturbances, however, initial 87Sr/86Sr ratios of undisturbed samples from the two major suites vary between 0.703 and 0.706. Both suites originated either by partial melting of pre-existing mafic rocks within the lower crust or by mixing of mantle-derived magma with crustal melts derived from partial melting of older country rocks. The mafic enclaves are interpreted as cumulates formed along the walls of the feeder conduits by fractional crystallization caused by the temperature gradient across the feeder walls. The presence of these mafic enclaves in the Western but not the Eastern suite may indicate that they were formed from the Eastern suite magma and subsequently were picked up and engulfed in the later Western suite magma, using the same magma conduits. Major element geochemical modeling indicate that the Eastern suite intruded first (in accordance with age determinations) and that the remaining magma experienced around 20 % of plagioclase fractionation before it intruded to form the Western suite. The vicinity of the Karlskrona deformation zone may have influenced the intrusion of the pluton.

The paper “A dynamic 2000—540 Ma Earth history: From cratonic amalgamation to the age of supercontinent cycle” that was recently published in Earth-Science Reviews by Li et al. (2023) is an impressive piece of work, putting together data for the Proterozoic supercontinent cycle into a coherent model including both maps and animations. Nevertheless, as they write themselves, there will no doubt be room for improvements of their model, some of which I hope to contribute with in this comment from my Baltica perspective, in particular when it comes to the relations between Baltica, Amazonia and West Africa.

A-type granites are typically formed in stable intra-plate, back-arc or postcollisional settings and are characterized by highly ferroan and potassic major element compositions, and by strong enrichment in incompatible trace elements. Unlike I-, S- and M-type granites, where the letters denote the dominant source material (igneous, sedimentary or mantle derived), there is no consensus on the source and processes giving rise to A-type magmas. In this contribution, a conceptual model for the origin of A-type granitoids, using the Bornholm A-type granitoid complex in southern Fennoscandia as an example, is presented. In this model, underplated mantle-derived basaltic magma may develop into intermediate and siliceous A-type magma, which is ferroan, potassic and highly enriched in incompatible trace elements, through a combination of fractional crystallization leading to cumulate formation, and partial melting and crustal assimilation, in a process akin to zone refining in metallurgy. The key factor is a relatively stable tectonic environment (postcollisional, anorogenic, or extensional), where there is little or no replenishment of more primitive basaltic magma to the system, allowing it to attain more evolved, enriched and extreme compositions. The A-type granitoids may then be viewed as a more evolved counterpart of subduction-related I-type granitoids.

A total of 4344 magmatic U-Pb ages in the range 2300 to 800 Ma have been compiled from the Great Proterozoic Accretionary Orogen along the margin of the Columbia / Nuna supercontinent and from the subsequent Gren-villian collisional orogens forming the core of Rodinia. The age data are derived from Laurentia (North America and Greenland, n = 1212), Baltica (NE Europe, n = 1922), Amazonia (central South America, n = 625), Kalahari (southern Africa and Dronning Maud Land in East Antarctica, n = 386), and western Australia (n = 199). Laurentia, Baltica, and Amazonia (and possibly other cratons) most likely formed a ca. 10 000-km-long external active continental margin of Columbia from its assembly at ca. 1800 Ma until its dispersal at ca. 1260 Ma, after which all cratons studied were involved in the Rodinia-forming Grenvillian orogeny. However, the magmatic record is not smooth and even but highly irregular, with marked peaks and troughs, both for individual cratons and the combined data set.& nbsp;Magmatic peaks typically range in duration from a few tens of million years up to around hundred million years, with intervening troughs of comparable length. Some magmatic peaks are observed on multiple cratons, either by coincidence or because of paleogeographic proximity and common tectonic setting, while others are not. The best overall correlation, 0.617, is observed between Baltica and Amazonia, consistent with (but not definitive proof of) their being close neighbours in a SAMBA-like configuration at least in Columbia, and perhaps having shared the same peri-Columbian subduction system for a considerable time. Correlation factors between Laurentia and Baltica, or Laurentia and Amazonia, are below 0.14. Comparison between the Grenville Province in northeastern Laurentia and the Sveconorwegian Province in southwestern Fennoscandia (Baltica) shows some striking similarities, especially in the Mesoproterozoic, but also exhibits differences in the timing of events, especially during the final Grenville-Sveconorwegian collision, when the Sveconorwegian evolution seems to lag behind by some tens of million years. Between the other cratons, the evolution before and during the final Grenvillian collision is also largely diachronous. After 900 Ma, magmatic activity had ceased in all areas investigated, attesting to the position of most of them within the stable interior of Rodinia.

The mid-Proterozoic (ca. 1850–850 Ma) is a peculiar period of Earth history in many respects: ophiolites and passive margins of this age are rare, whereas anorthosite and A-type granite suites are abundant; metamorphic rocks typically record high thermobaric (temperature/pressure) ratios, whereas ultrahigh pressure (UHP) rocks are rare; and the abundance of economic mineral deposits features rare porphyry Cu-Au and abundant Ni-Cu and Fe-oxide Cu-Ag (IOCG) deposit types. These collective observations have been used to propose that a stagnant-lid, or single-lid, tectonic regime operated at this time, between periods of plate tectonics in the Paleoproterozoic and Neoproterozoic. In our reappraisal of the mid-Proterozoic geological record, we not only assess the viability of the single-lid hypothesis for each line of evidence, but also that of the plate tectonic alternative. We find that evidence for the single-lid hypothesis is equivocal in all cases, whereas for plate tectonics the evidence is equivocal or supporting. We therefore find no reason to abandon a plate tectonic model for the mid-Proterozoic time period. Instead, we propose that the peculiarities of this enigmatic interval can be reconciled through the combination of two processes working in tandem: secular mantle cooling and the exceptionally long tenure and incomplete breakup of Earth's first supercontinent, where both of these phenomena had a dramatic effect on lithospheric behaviour and its resulting imprint in the geological record.

The concealed basement of the Mid-Lithuanian domain (MLD) is considered to be part of a larger Precambrian unit within the western East European Craton (EEC), the Mid-Baltic belt (MBB), established by Bogdanova et al. (2015). New data on rock chemistry, U-Pb ages, and the Sm-Nd and Rb-Sr isotopic systems allow to subdivide the MLD into distinct parts, discuss their origin and correlate them with similar units on the Swedish side. The MLD can be subdivided into two parts: NW and SE. The NW MLD magmatic rocks crystallized from 1.86 to 1.83 Ga and were subsequently intruded by 1.81-1.80 Ga granitoids and charnockitoids. The NW MLD samples have SiO2 contents between 48 and 71 wt.% but have similar initial εNd values at -1 to -2, while their initial Sr isotope ratios scatter. Nd isotope data suggest either an enriched mantle source, or a mantle magma that was mixed with older crustal material. The SE MLD magmatic rocks originated from a slightly depleted mantle source from 1.87 to 1.82 Ga. At 1792±9 Ma, they were intruded by gabbronorites which in turn were crosscut by thin veinlets of microgabbronorite at 1758±11 Ma. The SE MLD rocks have positive εNd (+1 to +3) and undisturbed Rb/Sr systems suggesting mantle-derivation, with the variation in composition (mafic to felsic) due to fractionation rather than crustal contributions. The SE MLD magmatic series with oceanic island arc affinity correlate well with the ca 1.85 Ga Fröderyd metavolcanics of the Vetlanda-Oskarshamn belt (Salin et al., 2021) in SE Sweden, while the NW MLD rocks are similar to the TIB-0 (1.86-1.85 Ga) Askersund granitoids (cf. Salin et al., 2021) in the southern Bergslagen area. The younger (1.81-1.79 Ga) intrusives in both areas are time-equivalents of the TIB-1 magmatism on the Swedish side. Thus, the MLD as well as its counterparts on the Swedish side of the Baltic Sea, the TIB-0 magmatism in the southern Bergslagen area and the Vetlanda-Oskarshamn belt, may be assigned to the same Mid-Baltic Belt, representing an active, south-facing continental margin established at ca. 1.86 Ga. The shape and outline of the Belt was affected by the Fennoscandia-Sarmatia collision at ca. 1.82-1.80 Ga, the 1.81-1.76 Ga TIB-1 magmatism, as well as by later Mesoproterozoic intraplate magmatism. Bogdanova, S. et al., 2015. Precambrian Research 259, 5–33. Salin, E. et al., 2019. Precambrian Research 328, 287–308. Salin, E. et al., 2021. Precambrian Research 356, 106134

The concealed basement of the Mid-Lithuanian domain (MLD) is considered to be part of a larger Precambrian unit within the western East European Craton (EEC), the Mid-Baltic belt (MBB), established by Bogdanova et al. (2015). New data on rock chemistry, U-Pb ages, and the Sm-Nd and Rb-Sr isotopic systems allow to subdivide the MLD into distinct parts, discuss their origin and correlate them with similar units on the Swedish side. The MLD can be subdivided into two parts: NW and SE. The NW MLD magmatic rocks crystallized from 1.86 to 1.83 Ga and were subsequently intruded by 1.81-1.80 Ga granitoids and charnockitoids. The NW MLD samples have SiO2 contents between 48 and 71 wt.% but have similar initial εNd values at -1 to -2, while their initial Sr isotope ratios scatter. Nd isotope data suggest either an enriched mantle source, or a mantle magma that was mixed with older crustal material. The SE MLD magmatic rocks originated from a slightly depleted mantle source from 1.87 to 1.82 Ga. At 1792±9 Ma, they were intruded by gabbronorites which in turn were crosscut by thin veinlets of microgabbronorite at 1758±11 Ma. The SE MLD rocks have positive εNd (+1 to +3) and undisturbed Rb/Sr systems suggesting mantle-derivation, with the variation in composition (mafic to felsic) due to fractionation rather than crustal contributions. The SE MLD magmatic series with oceanic island arc affinity correlate well with the ca 1.85 Ga Fröderyd metavolcanics of the Vetlanda-Oskarshamn belt (Salin et al., 2021) in SE Sweden, while the NW MLD rocks are similar to the TIB-0 (1.86-1.85 Ga) Askersund granitoids (cf. Salin et al., 2021) in the southern Bergslagen area. The younger (1.81-1.79 Ga) intrusives in both areas are time-equivalents of the TIB-1 magmatism on the Swedish side. Thus, the MLD as well as its counterparts on the Swedish side of the Baltic Sea, the TIB-0 magmatism in the southern Bergslagen area and the Vetlanda-Oskarshamn belt, may be assigned to the same Mid-Baltic Belt, representing an active, south-facing continental margin established at ca. 1.86 Ga. The shape and outline of the Belt was affected by the Fennoscandia-Sarmatia collision at ca. 1.82-1.80 Ga, the 1.81-1.76 Ga TIB-1 magmatism, as well as by later Mesoproterozoic intraplate magmatism. Bogdanova, S. et al., 2015. Precambrian Research 259, 5–33. Salin, E. et al., 2019. Precambrian Research 328, 287–308. Salin, E. et al., 2021. Precambrian Research 356, 106134

New zircon U-Pb age measurements, whole rock major and trace element geochemistry, and Sr and Nd isotopic analyses of samples from fourteen deep drill holes that penetrated the hidden Precambrian basement of the southernmost Baltic Sea and the coastal area of northern Poland (Pomerania), make it possible to identify a two episodes of Proterozoic magmatism in that area. The basement consists of late Palaeoproterozoic deformed calc-alkaline, magnesian, I-type to A-type diorites to granites of volcanic arc affinity. U-Pb zircon geochronology documents their magmatic crystallization ages to be between 1791 +/- 8 Ma and 1750 +/- 5 Ma, with an episode of syn- to late-magmatic deformation recorded in thin overgrowths on zircons at about 1740 Ma. These rocks from Pomerania and its offshore area broadly correlate with the bedrock of Blekinge in southern Sweden, where most of the crust was formed at 1.77-1.75 Ga. They may thus be part of the same geological domain, extending on both sides of the present-day southern Baltic Sea, formed along a late Palaeoproterozoic active continental margin. A subordinate suite of undeformed, significantly younger A-type granites was emplaced at 1477 +/- 6 Ma, 1449 +/- 7 Ma and 1450 +/- 9 Ma. This time interval is concurrent with emplacement of A-type granitoids on the Danish island of Bornholm as well as in Blekinge and other parts of southern Fennoscandia. However, their geochemical and isotopic data highlight a genetic diversity of these granites.

Ten samples of felsic plutonic rocks from the Eastern Segment of the Sveconorwegian Orogen in southern Sweden, previously dated by ID-TIMS on zircon, have been dated anew using SIMS spot analysis of individual zircon grains, leading to more reliable and in most cases also more precise revised magmatic crystallization ages. A gneissic monzonite within the Protogine Zone in Småland yields a revised U-Pb age of ca. 1725 Ma, four samples of orthogneiss from Skåne all yield revised ages between 1700 and 1690 Ma, while two samples of coarse-grained granitic gneiss in the same region yield ages between 1690 and 1680 Ma. These revised ages are between 15 and 250 m.y. older than previously obtained TIMS ages. Two samples of the Gumlösa-Glimåkra granite along the Protogine Zone in northern Skåne and one sample of related syenite yield ages around 1220 Ma, similar but more precise compared to the previous ages. The U-Pb zircon data have been complemented by Hf isotope analysis by LA-ICP-MS on the same grains, and previously obtained initial Sr and Nd whole-rock isotope data have been recalculated to the revised crystallization ages. The Sr isotope data scatter, while the revised initial εNd values fall between +1 and +2 for the older rocks, and close to 0 for the younger intrusives along the Protogine Zone. Initial εHf in magmatic undisturbed zircons shows relatively little spread within each sample, between 2 and 4 Epsilon units, disregarding a few outliers, with average values for the 1725 to 1680 Ma rocks between +3 and +5.5 and for the 1220 Ma rocks at ca. +1.5. Covariation between initial εNd and initial εHf in the older rocks suggests either mixing between two isotopically distinct magma sources or one magma source which was isotopically heterogeneous. The isotopic signatures of the 1220 Ma intrusive rocks along the Protogine Zone are indicative of juvenile mantle input to their magmas, rather than pure crustal melting.

The Shaitian granite complex (SGC) spans more than 80 Ma of crustal growth in the Arabian–Nubian Shield in southeast Egypt. It is a voluminous composite intrusion (60 km2) comprising a host tonalite massif intruded by subordinate dyke-like masses of trondhjemite, granodiorite and monzogranite. The host tonalite, in turn, encloses several, fine-grained amphibolite enclaves. U-Pb zircon dating indicates a wide range of crystallization ages within the SGC (800 ± 18 Ma for tonalites; 754 ± 3.9 Ma for trondhjemite; 738 ± 3.8 Ma for granodiorite; and 717 ± 3.2 Ma for monzogranite), suggesting crystallization of independent magma pulses. The high positive εNdi (+6–+8) indicate that the melting sources were dominated by juvenile material without any significant input from older crust. Application of zircon saturation geothermometry indicates increasing temperatures during the generation of melts from 745 ± 31 °C for tonalite to 810 ± 25 °C for trondhjemite; 840 ± 10 °C for granodiorite; and 868 ± 10 °C for monzogranite. The pressure of partial melting is loosely constrained to be below the stability of residual garnet (<10 kbar) as inferred from the almost flat HREE pattern ((Gd/Lu)N = 0.9–1.1), but >3 kbar for the stability of residual amphibole as inferred from the significantly lower NbN and TaN compared with LREEN and the sub-chondrite Nb/Ta ratios exhibited by the granitic phases. The inverse relation between the generation temperatures and the ages estimates of the granitoid lithologies argue against a significant role of fractional crystallization. The major and trace element contents indicate the emplacement of the SGC within a subduction zone setting. It lacks distinctive features for melt derived from a subducted slab (e.g. high Sr/Y and high (La/Yb)N ratios), and the relatively low MgO and Ni contents in all granite phases within the SGC suggest melting within the lower crust of an island arc overlying a mantle wedge. Comparison with melts produced during melting experiments indicates an amphibolite of basaltic composition is the best candidate as source for the tonalite, trondhjemite and granodiorite magmas whereas the monzogranite magma is most consistent with fusion of a tonalite protolith. Given the overlapping Sm-Nd isotope ratios as well as several trace element ratios between monzogranite and tonalite samples, it is reasonable to suggest that the renewed basaltic underplating may have caused partial melting of tonalite and the emplacement of monzogranite melt within the SGC. The emplacement of potassic granite (monzogranite) melts subsequent to the emplacement of Na-rich granites (tonalite-trondhjemite-granodiorite) most likely suggests major crustal thickening prior arc collision and amalgamation into the over thickened proto-crust of the Arabian-Nubian shield. Eventually, after complete consolidation, the whole SGC was subjected to regional deformation, most probably during accretion to the Saharan Metacraton (arc–continent collisions) in the late Cryogenian -Ediacaran times (650–542 Ma).

A Mid-Lithuanian Domain (MLD) was distinguished by Bogdanova et al. (2015) as part of the large Mid-Baltic Belt (MBB) in the western East European Craton. Zircon U-Pb dating by SIMS, Sr- and Nd-isotope systematics and a detailed geochemical study have allowed to subdivide the MLD into two parts: NW and SE. The NW magmatic rocks have been emplaced at 1.86 to 1.83 Ga from either an enriched mantle source or from a mantle magma with presence of older crustal material. The SE MLD magmatic rocks originated from a slightly depleted mantle source at 1.87 to 1.82 Ga. At 1.79 Ga, they were intruded by gabbronorites which at 1.76 Ga were crosscut by thin veinlets of microgabbronorite. The SE MLD magmatic series with their oceanic island arc affinity correlate well with the contemporaneous Fro center dot deryd metavolcanics of the Vetlanda-Oskarshamn belt in Sweden, while the NW MLD rocks are similar to the TIB-0 Askersund granitoids in the southern Bergslagen area. The younger (1.81-1.79 Ga) intrusives in both areas are time-equivalents of the TIB-1 magmatism on the Swedish side. Thus, the MLD as well as its counterparts on the Swedish side of the Baltic Sea may belong to the same MidBaltic Belt, representing an active, south-facing continental margin established at ca. 1.86 Ga. The shape and outline of the belt was affected by the Fennoscandia-Sarmatia collision at ca. 1.82-1.80 Ga, as well as by later magmatism.

The Hedesunda granite complex covers a rectangular area of ca 800 km2 within the Bergslagen lithotectonic unit of the Paleoproterozoic Svecofennian orogen in east-central Sweden. It is dominated by coarse porphyritic and generally undeformed granitoids whose position within the Svecofennian orogenic evolution has been controversial. New U–Pb SIMS dating of zircon confirms earlier TIMS results, showing that it is a composite intrusion made up of an older phase at ca 1865 Ma, forming the bulk of the massif, and a younger phase at ca 1785 Ma, forming a circular intrusion in the north-central area and an elongated body further west. The two generations have very different geochemistry. The older Hedesunda I intrusion ranges from diorite through tonalite and granodiorite to granite in composition, is dominantly metaluminous, calc-alkaline, magnesian, I-type and volcanic arc-related, and probably formed by melting of juvenile Svecofennian lower crust due to basaltic underplating during an extensional ‘intra-orogenic’ phase shortly after the main subduction-related early-orogenic Svecofennian magmatism. The younger Hedesunda II intrusions are purely granitic, dominantly peraluminous, alkali-calcic, K-rich, and ferroan, with A-type and within-plate-type characteristics, and formed penecontemporaneously with post-collisional shoshonitic intrusions in southern Finland, again presumably by crustal melting due to basaltic underplating in an extensional setting towards the end of the Svecofennian orogeny.

The Herräng mafic dykes form an E-W-trending dyke swarm within the Bergslagen lithotectonic unit of the Svecofennian orogen in east-central Sweden. They intrude the Svecofennian supracrustal rocks and early-orogenic granitoids, but are themselves cut by late Svecofennian pegmatites, and have undergone Svecofennian amphibolite-facies metamorphism, leading to their classification as “intraorogenic” Svecofennian dykes. They can be assigned an age between 1870 and 1850 Ma, with metamorphism of the dykes dated at 1848 ± 13 Ma by U-Pb in titanite. Their current mineralogy is dominated by metamorphic plagioclase and amphibole, with variable amounts of quartz and biotite, and minor to accessory titanite, apatite, epidote, pyrite, magnetite, ilmenite and zircon. Textures range from massive to strongly foliated. Twenty samples of dyke rocks from three subareas in the Roslagen region, including the Herräng type area, range in composition from basaltic to andesitic with 47 to 60 wt% SiO2, broadly similar to the Dannemora dykes and the Avesta-Östhammar gabbros and diorites. Initial 87Sr/86Sr ratios (at 1870 Ma) varies between 0.7026 and 0.7038, corresponding to initial εSr between +5 and +21, and initial εNd between −0.4 and +1.3, suggesting a slightly enriched to mildly depleted mantle source, similar to other Svecofennian mafic rocks. The dykes dominantly show a calc-alkaline volcanic arc signature related to subduction. They formed during an extensional episode, possibly related to incipient back-arc spreading or subduction roll-back following the main early-orogenic subduction-related Svecofennian magmatism, but penecontemporaneous with amphibolite-facies metamorphism in the area.

A sample of fine-grained grey Stockholm granite from the Frescati area just north of central Stockholm, east-central Sweden, earlier dated to 1803 (+23)/(-19) Ma by the U-Pb zircon method using TIMS on multigrain fractions, has been reanalyzed using the Nordsim ion microprobe. The new age obtained, 1792 +/- 4 Ma, is more precise, and replaces the earlier highly discordant date. It agrees well with other ages for the formation of the Stockholm-type granites and related pegmatites, indicating an age of around 1.79 Ga for this late-orogenic Svecofennian granite magmatism. The Stockholm granite thus formed toward the end of the 1.83-1.79 Ga late Svecofennian metamorphic phase, and crosscuts earlier formed migmatitic gneiss structures in a brittle manner at the present-day level of exposure.

The earliest Svecofennian magmatism in southern Finland has been dated at 1.90-1.88Ga. As an example of this, the Orijärvi (ca. 1.89Ga) and Enklinge (ca. 1.88Ga) volcanic centres comprise bimodal plutonic batholiths surrounded by volcanic rocks of comparable ages and chemical compositions. Here, we report geochemical and Sm-Nd isotope data from intrusive and extrusive samples, combined with zircon U-Pb and Lu-Hf isotopes for granodiorites from both study areas. The samples range from gabbros to granites and indicate a subduction-related continental margin setting. The zircons from the Orijärvi granodiorite define an age of 1892±4Ma whereas the Enklinge granodiorite yields an age of 1882±6Ma. Several inherited ages of 2.25-1.95Ga as well as younger ages of 1.86-1.80Ga were found in the Enklinge granodiorite. The initial εNd values from the mafic rocks from both locations fall in the range +1.1 to +2.9 whereas the felsic rocks exhibit initial εNd values of -0.4 to +1.2. The magmatic zircons from the Orijärvi and Enklinge granodiorites show average initial εHf values of -1.1 (at 1892Ma) and zero (at 1882Ma), respectively, each with a spread of about 7 ε-units. The initial εHf values for the inherited zircons from Enklinge range from +3.5 to +7.6 with increasing age. The Sm-Nd data indicate that the mafic rocks were derived from a “mildly depleted” mantle source while the felsic rocks show larger crustal contribution. Also, the variation in εHf values indicates minor mixing between mildly depleted mantle derived magmas and crustal sources. U-Pb ages and Hf isotopes for inherited zircons in the Enklinge granodiorite suggest the presence of juvenile Svecofennian “proto-crust” at depth.

This work is a review of Boris Choubert's paper (1935), which was published in French under the rather devalorizing title: "Research on the Genesis of Palaeozoic and Precambrian Belts." Despite its innovative content, this article had no impact either at the time of its publication or even later. It begins with the construction of a remarkable fit of the circum-Atlantic continents. This was based on the - 1.000 meters isobath instead of the shoreline. Thirty years before Bullard et al. (1965), it demonstrated in an indisputable way the reality of the continents motion on the surface of the Earth. Therefore, Choubert designated Wegener's "continental drift" as the main cause of tectonics. Even going beyond Wegener's theory, he argued that this mechanism was efficient well before the formation of the Triassic Pangaea, during the whole Palaeozoic to result in the building of the Caledonian and Hercynian mountains. Although he was still encumbered by the vocabulary of the time regarding geosynclines, Boris Choubert described tectonics based on the horizontal mobility of the Precambrian continental blocks. Oddly enough, he did not apply this model to the Precambrian structures, which he attributed to the effects of the Earth's rotation on the continental crust during its solidification. At the time of its publication, this paper was a very important step towards understanding global tectonics. Unfortunately, Choubert's contemporaries did not generally recognize its significance.

The Palaeoproterozoic (2.0–1.8 Ga) Svecokarelian orogen in central Sweden consists of a low-pressure, predominantly medium-grade metamorphic domain (central part of Bergslagen lithotectonic unit), enclosed to the north and south by low-pressure migmatite belts. Two periods of metamorphism (1.87–1.85 and 1.83–1.79 Ga) are known in the migmatite belts. In this study, new U–Th–Pb ion microprobe data on zircon and monazite from twelve samples of locally migmatized gneisses and felsic intrusive bodies determine both protolith and metamorphic ages in four sample areas north of Stockholm, inside or immediately adjacent to the medium-grade metamorphic domain. Two orthogneiss samples from the Rimbo area yield unusually old protolith ages of 1909 ± 4 and 1908 ± 4 Ma, while three orthogneisses from the Skutskär and Forsmark areas yield more typical protolith ages between 1901 ± 3 and 1888 ± 3 Ma. Migmatized paragneiss samples from this and two earlier studies contain a significant detrital component sourced from this 1.9 Ga magmatic suite. They are interpreted to be deposited contemporaneously with or shortly after this magmatism. Migmatization of the paragneiss at Rimbo was followed by intrusion of leucogranite at 1846 ± 3 Ma. Even in the other sample areas to the north (Hedesunda-Tierp, Skutskär and Forsmark), metamorphism including migmatization is constrained to the 1.87–1.85 Ga interval and penetrative ductile deformation is limited by earlier studies in the Forsmark area to 1.87–1.86 Ga. However, apart from a metamorphic monazite age of 1863 ± 1 Ma, precise ages were not possible to obtain due to the presence of only partially reset recrystallized domains in zircon, or highly discordant U-rich metamict and altered metamorphic rims. Migmatization was contemporaneous with magmatic activity at 1.87–1.84 Ga in the Bergslagen lithotectonic unit involving a mantle-derived component, and there is a spatial connection between migmatization and this magmatic phase in the Hedesunda-Tierp sample area. The close spatial and temporal interplay between ductile deformation, magmatism and migmatization, the P–T metamorphic conditions, and the continuation of similar magmatic activity around and after 1.8 Ga support solely accretionary rather than combined accretionary and collisional orogenic processes as an explanation for the metamorphism. The generally lower metamorphic grade and restricted influence of the younger metamorphic episode, at least at the ground surface level, distinguishes the central part of the Bergslagen lithotectonic unit from the migmatite belts further north and south.