(Redirected from Fennoscandian Shield)The 'Baltic Shield' (sometimes referred to as the 'Fennoscandian Shield') is located in
Fennoscandia (
Norway,
Sweden and
Finland), northwest
Russia and under the
Baltic Sea. The Baltic Shield is defined as the "exposed" Precambrian northwest segment of the
East European Craton. It is composed mostly of
Archean and
Proterozoic gneisses and
greenstone which have undergone numerous deformations through
tectonic activity. The Baltic Shield contains the oldest rocks of the
European
continent with a thickness of 250–300 km. During the Pleistocene epoch, great continental ice sheets scoured and depressed the shield's surface, leaving a thin covering of glacial material and innumerable lakes and streams. The Baltic Shield is still rebounding today from the thick glacials during the
Quaternary Period.
Provinces and Blocks
The 'Baltic Shield' is divided into five ''provinces'': the 'Svecofennian' and 'Sveconorwegian' (or 'Southwestern gneiss') provinces in Fennoscandia, and the Karelian, Belomorian and Kola
provinces/
cratons in Russia. The latter three are divided further into several ''blocks'' and ''complexes'' and contain the oldest of the rocks, at 2.5–3.4 Ga. The Vodlozero block in south-eastern Karelia has been dated to 3.4 Ga. The youngest rocks belong to the Sveconorwegian province, at 900–1700 Ma old. Sometimes included as part of the Baltic Shield is the 'East European Platform' (or 'Russian Platform'), an area of western Russia covered by 3 km of
sedimentary rock.
Regolith
Thought to be formerly part of an ancient continent, the Baltic Shield grew in size through collisions with neighbouring crustal fragments. The mountains created by this tectonic processes have since been eroded to their bases, the region being largely flat today. Through five successive
Pleistocene glaciations and subsequent retreats, the Baltic Shield has been scoured clean of its overlying sediments, leaving expansive areas (most within Scandinavia) exposed. It is therefore of importance to
geophysicists studying the geologic history and dynamics of eastern Europe.
The scouring and compression of the Baltic Shield by
glacial movements created the area's many lakes and streams, the land retaining only a thin layer of sandy sediment collected in depressions and
eskers. Most soil consists of
moraine, a grayish yellow mixture of sand and rocks, with a thin layer of
humus on top. Vast forests, featuring almost exclusively the three species pine, spruce and birch, dominate the landscape, clearly demarcating its boundaries. The soil is acidic and has next to no carbonates such as
limestone. The scouring by the ancient glaciers and the acidity of the soil have destroyed all palaentologically interesting materials, such as fossils.
Belomorian and Karelian provinces
The Archean segment of the Baltic/Fennoscandian shield is divided into the Karelian, Belomorian and Kola provinces. The Karelian province is a
granite-
greenstone province reworked during the Proterozoic. The North Karelian greenstone belt sequence (NKGBS) is dominated by
volcanics of
calc-alkaline series,
diorite-
plagiogranitic batholith, and
xenoliths of
ultramafic to
andesite-
dacite composition.
According to a study by Slabunov (1999): "The Belomorian Province is a mobile belt that evolved in a polycyclic manner. A lateral sequence of Late Archean tectonic units has been revealed in the Belomorian Province and in the eastern part of the Karelian Province. The collision events in the Belomorian Province are represented by high pressure (6–12 kbar) and high temperature (500–700°C)
kyanite-
facies metamorphism,
granitoid magmatism, and the formation of folded
nappe structure and granite gneiss domes. The time of collision is estimated at 2.7–2.74 Ga. This stage of evolution in the NE part of Karelian Province is accompanied by the generation of North Karelian greenstone belt (NKGB).
The Belomorian Belt is a tectonic pile of meta
sedimentary, metavolcanic and meta
plutonic rocks which has been folded and metamorphosed several times. According to a study by Bibikova et al. (1999), the earliest metamorphic event took place ca. 2.8 Ga. "
Sm-Nd isotope studies of whole rock metasediment samples have constrained their mean
protolith ages to between 3.00 and 2.86 Ga, indicating a short prehistory....
Zircons were separated from different localities and at various levels of the Belomorian tectonostratigraphical column. We have recognized three age groups of ancient cores at 3.2–3.1 Ga, 3.00–2.97 Ga and 2.93–2.90 Ga. The plus 3.1 Ga cores were obtained solely from localities in the northern part of the Belt. It has also been possible to distinguish three groups of
metamorphic grains and overgrowths which are 2.84–2.80 Ga, 2.72–2.68 Ga and ca. 2.61 Ga old. The data presented confirm the absence of detrital material older than 3.2 Ga in the Belomorian metasediments. This differs from the adjacent
Karelian craton where crustal rocks of about 3.4 Ga have been recorded. If these ages are representative of the rocks discussed, our data suggest that the Belomorian Belt represents a Neoarchaean
accretionary environment in the vicinity of the Karelian craton." (Bibikova et al., 1999).
From NE to SW the Baltic shield consists of the following structural-formational zones: 1) the Central Belomorian
mafic zone (CBMZ) dominantly formed by mafic and ultramafic rocks, 2) the
Chupa Paragneissic Belt (ChPB) composed of deep and repeatedly
metamorphosed metagraywackes (mainly high-
alumina gneisses), 3) the North Karelian system of greenstone belts (NKGB) dominated by volcanics of calc-alkaline series, and 4) the North Karelian
diorite-
plagiogranitic batholith (NKB) and
xenoliths of ultramafic to andesite-dacite composition that occur in it. The CBMZ is dominated by metabasalts (
amphibolites) with widespread meta
ultrabasic rocks (meta
peridotites,
serpentinites and
apoultramafic amphibolites), and extremely rare acid metavolcanics. The chemical composition of metabasalts in the CBMZ is similar to that of
mid-oceanic ridge basalts (MORB). The
isotopic age of the
rhyolite-dacites is 2.887 Ga. This association is interpreted as a fragment of a Late Archean
ophiolitic complex. The CBMZ marks a collision suture. The supracrustal strata of NKGBS consist of metabasalts, meta
komatiites and
felsic to intermediate metavolcanics. Metaandesites-metarhyolites make up a considerable portion of the sequence. The age of these volcanics is estimated at 2.877–2.820 Ga. Between the NKGB and the CBMZ there lies the ChPB which consists of metagraywackes (
garnet-
biotite kyanite-bearing gneisses. This lateral series indicates the Late Archean (3.0–2.8 Ga)
subduction stages in the evolution of the eastern Baltic shield. During the first stage, the oceanic
lithosphere subducted from NE to SW under the subcontinental crust. In the second stage it subducted under the continental crust of the Karelian plate." (Slabunov, 1999)
Kola province
The
Archaean Kolmozero-Voronja greenstone belt is located on the Kola Peninsula between Murmansk, Central Kola and the Keivy terrains of Upper Archaean. Four suites are distinguished in the greenstone belt: Ljavozerskya (lower terrigenous formation), Polmostundrovskya (
komatiite-
tholeiite), Voronjatundrovskya (basalt-andesite-dacite) and Chervurtskya (an upper terrigenous formation).
Zircon in the
quartz of the upper part of the Voronjatundrovskya suite yield
U-Pb age of 2.8 G. This is interpreted as
intrusive emplacement of
quartz porphyry during the final stage of the belt development.
Ovoid plagioamphibolites are present among
shistosed
plagioamphibolites of the Polmostundrovsky suite and have been dated at ~2.6 Ga, indicative of
andalusite-
sillimanite facies metamorphism. Toumalinr granites are found all over the Kolmozero-Voronja belt occurring among volcano-genic sedimentary rock with good correlation dating of 2520±70 Ma. (Kudryashov, 1999).
The geochronological data show long and complicated evolution of the belt: 3.0–2.9 Ga formation of mafic volcanic sequence and its probable
magmatic analogue, ~2.9 Ga old
gabbro, 2.9–2.8 Ga formation of intermediate and felsic volcanites with an upper age limit of ~2.83 Ga, 2.7–2.6 Ga
granodiorite intrusions and their vein analogues, and 2.6–2.5 Ga intrusion of post
kinematic tourmaline and
microcline granites. (Kudryashov, 2001).
Within the Murmansk block, from west to east, there is an increase in the
rare earth elements (REE) content in the initial melts, a change in composition of protoliths from tholeiite with the highest content of REE to the subalkaline basalt, and in the eastern part of the Murmansk block the REE content is even higher. The origin of
tonalites and
trondhjemites (TT) is most likely the result of partial melting of mafic sources. The increase of
alkalinity in the protoliths of TT-gneiss correlates with the abundance of the Late Archean peralkaline (2750±50 Ma) and alkaline (2760±60 Ma) granite
massifs here. (Turkina and Vetrin, 1999).
Within the Murmansk block, from west to east, there is an increase in the REE content in the initial melts, a change in composition of protoliths from tholeiite with the highest content of REE to the subalkaline basalt, and in the eastern part of the Murmansk block the REE content is even higher. The origin of tonalites and
trondhjemites (TT) is most likely the result of partial melting of mafic sources. The increase of alkalinity in the protoliths of TT-gneiss correlates with the abundance of the Late Archean peralkaline (2750±50 Ma) and alkaline (2760±60 Ma) granite
massifs here. (Turkina and Vetrin, 1999).
Northeastern Baltic Shield
The Keivy complex in the NE Baltic shield consists mainly of sheet-like peralkaline granite bodies,
granosyenite dykes and some
nepheline syenite fault-type
intrusions in the total exposed ~2500 km. square area.
According to a study by Bayanova and Zozulya (1999), the emplacement ages for peralkaline granite
magmatic vary from 2610 Ma for the White Tundra
massif to 2670 Ma for the Western Keivy
massif and are spatially confined to voluminious
gabbro-
anorthosite magmatism of 2.66–2.68 Ga. The predominantly "juvenile"
Sm-Nd isotopic signatures from most suites of Keivy complex suggest that they must be of
mantle derivation or else have has short-lived crustal precursors. "The granites are
petrologically and geochemically similar to
Phanerozoic A-type granitoids, presumably emplaced into noncompressive or extensional environments. The distinct tectonic regime of such type of granites indicates that the Keivy peralkaline granite
magmatism can be regarded as a consequence of post-collisional events. Collision in the region has possibly taken place earlier than 2.74 Ga. The granites studied were formed after the Late Archaean Keivy-Voronja greenstone belt evolution." (Bayanova, 1999). The above model suggests that the NE
Archaean portion of the Baltic shield was dominated by
plume tectonics.
The Laplandian Granulite Belt is in the central northeast section of the Baltic shield. Garnet plagiogranitoids occur in the northeastern part, crystallised from melting of host rock acid granulites. The absence of stratification in the north part of the Lapland Granulite Belt are related to the E-W extension at the final period of thrusting. This deformation stage was characterised by persistently high temperatures and increasing water activity. (Kozlov and Kozlova, 1999).
Southeastern Baltic Shield
The Sumozero-Kenozero greenstone belt in the southeastern section of the Baltic shield is ~400 km long and up to 50 km wide. It comprises a 5-km thick oceanic
plateau sequence of submarine komatiite-basalt
lava and volcanic sediments. The belt is
intruded and overlain by an
island arc-like sequence of intermediate-felsic volcanic rocks including andesitic basalts, andesites, dacites and rhyolites. According to a study by Hofmann et al. (1999): "The komatiites were derived from a liquid containing ~30% MgO. This liquid was initiated at depths of 300–400 km in a mantle plume that was some 250°C hotter than the ambient mantle. Both komatiites and basalts of the lower sequence are strongly depleted in LREE, have high
Nd(T) of +2.7±0.3, relatively unradiogenic Pb isotope compositions (µ m1 = 8.7±0.2) and show Nb-maxima (Nb/Nb
★ = 1.2±0.2, Nb/U = 43±6)." These parameters are found in a number of other early Precambrian greenstones and in recent Pacific OFB. "They are regarded as plume source characteristics and provide further evidence for the existence of certain Nb-excess in the Archaean mantle due to the early extraction of large volumes of continental crust with low Nb/U ratios. The intermediate-felsic volcanic and subvolcanic rocks of the upper unit are enriched in LREE, depleted in HFSE, but have positive Nd(T) values of +2.5±1.2. They represent both mantle wedge-derived basalt-andesite-dacite-rhyolite (BADR), and slab-derived (adakite) melts, erupted in the inner and frontal parts of an intraoceanic island arc." U-Pb zircon ages for the felsic volcanic rocks are 2875±2 Ma, and Pb-Pb and Sm-Nd ages of 2892±130 and 2916±117 Ma for the komatiites-basalts.
Vodla Block
The Sumozero-Kenozero greenstone belt displays fragments of unsubductable oceanic crust, represented by the lower mafic-ultramafic volcanic sequence, and also displays the products of subduction-related magmatism. This implies that the thick plume-derived oceanic crust reached an intraoceanic convergent plate boundary and was intruded and overlain by felsic melts coming from both a subducting slab and an overlying mantle wedge. Later, the oceanic plateau, together with the volcanic arc complex built on top of it, were accreted to and obducted onto the continental crust of the Vodla block. (Hofmann et al., 1999)
Economic geology
The Baltic Shield yields important industrial minerals and ores, such as those of iron, nickel, copper and platinum group metals. Because of its similarity to the Canadian Shield and cratons of southern Africa and Western Australia, the Baltic Shield had long been a suspected source of diamonds and gold. Currently, especially the Central Lapland Greenstone Belt in the north is considered to be an unexplored area that has the potential to hold exploitable gold deposits.
Recent exploration by De Beers and others has revealed a significant number of diamond-bearing kimberlites in the Kola Peninsula, and (possibly extensive) deposits of gold in Finland. In Sweden, Alcaston Diamond NL is presently conducting a diamond exploration project, claiming some 9,550 km².
Baltic Shield relation to Baltic plate
There is considerable misunderstanding in the literature with the use of the term "Baltic Shield." A shield in any craton is the area of exposed crystalline crust while the other part of a craton is a “platform” where the crystalline crust or basement is overlaid by younger sedimentary cover. Thus the crustal segments comprise both the shield areas and parts of the platform basement. Do not confuse the Baltic Shield with the Baltic Plate. The Baltic, Ukrainian shields and the Voronezh Massif are the present-day geomorphological highs which were formed much later, even in the Cenozoic. Geomorphologically the Baltic Shield is only one segment/region of the East European craton. The East European craton as a whole was a part of Neoproterozoic-Early Palaeozoic Baltica.
References
★ Bayanova, Tamara, and Dmitry Zozulya (1999) "Discrimination Between Plume and Plate Tectonics in Late Archaean of NE Baltic Shield from the Study of the Keivy A-Granite Complex." Journal of Conference Abstracts, Vol. 4, No. 1, Symposium A08, Early Evolution of the Continental Crust.[1]
★ Bibikova, Elena V., Svetlana Bogdanova, Stefan Claesson and Torbjorn Skiold. (1999) "NORDSIM Ages on Provenance and Metamorphic Zircon Material in Belomorian Metasediments of the Baltic Shield." Journal of Conference Abstracts, Vol. 4, No. 1, Symposium A08, Early Evolution of the Continental Crust.[2]
★ Evans, Paul. 1999. Precambrian evolution of the major Archaean blocks of the Baltic Shield. University of Oulu, Dept. of Geology, Finland. [3]
★ Hofman, Albrecht, Igor Puchtel, Alexander Samsonov, and Andrey Shchipansky. (1999) "Combined Hotspot-Island Arc Model for the Formation of the 2.9 Ga Sumozero-Kenozero Greenstone Belt, SE Baltic Shield." Journal of Conference Abstracts, Vol. 4, No. 1, Symposium A08, Early Evolution of the Continental Crust.[4]
★ Kozlov, Nikolai Ye, and Natalia Ye Kozlova. (1999) "Relation between Garnet Plagiogranitoids and Acid Granulites in Laplandian Granulite Belt." Journal of Conference Abstracts, Vol. 4, No. 1, Symposium A08, Early Evolution of the Continental Crust.[5]
★ Kudryashov, Nikolay. (1999) "Archean Kolmozero-Voronja Greenstone Belt: U-Pb Zircon and Sphene Data." Journal of Conference Abstracts, Vol. 4, No. 1, Symposium A08, Early Evolution of the Continental Crust.[6]
★ Kudryashov, Nikolay. (2001) "On Archean Evolution of the Kolmozero-Voronja Greenstone Belt (Kola Peninsula, Russia) U-Pb and Pb-Pb Dating." EUG XI Symposium LS07, Origin and Significance of Major Boundaries in the Deep crust and Continental Lithosphere. Online Abstract:[7]
★ Slabunov, Alexander. (1999) "Late Archaean Subduction and Collision Events in the Crustal Evolution of the Eastern Fennoscandian/Baltic Shield." Journal of Conference Abstracts, Vol. 4, No. 1, Symposium A08, Early Evolution of the Continental Crust.[8]
★ Turkina, Olga M. and Valeri R. Vetrin. (1999) "Composition of Tonalite - Trondhjemite Protoliths from the Kola Superdeep Borehole (KSDB) and on the Surface." Journal of Conference Abstracts, Vol. 4, No. 1, Symposium A08, Early Evolution of the Continental Crust.[9]
External links
★ Rb-Sr Data for Diamond-Bearing Kimberlite and Alkaline Massives in NE Fennoscandia
★ Precambrian evolution of the major Archaean blocks of the Baltic Shield (Google cached file)
★ Geology of Fennoscandia
★ Why does the East European Platform has (sic) 3 km of sediments? Insights from lithospheric structure, thermal regime, and composition (PDF file)
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