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Transactions of the Karelian Research Centre of the Russian Academy of Sciences No. 2. 2020. P. 18-33 DOI: 10.17076/geo1185
Труды Карельского научного центра РАН № 2. 2020. С.18-33
УДК 551.242.5:551.71/.72 (474.2)
THE EVOLUTION OF THE ESTONIAN PRECAMBRIAN BASEMENT: GEOLOGICAL, GEOPHYSICAL AND GEOCHRONOLOGICAL CONSTRAINTS
A. Soesoo1, S. Nirgi12, J. Plado1
1 University of Tartu, Institute of Ecology and Earth Sciences, Department of Geology, Estonia
2 Geological Survey of Estonia
The Estonian Precambrian crystalline basement, which consists of Paleo- to Meso-Proterozoic metamorphic and igneous rocks, is covered by a 100-780 m thick deposit of Paleozoic sedimentary rocks. Thus, the basement is unavailable for direct observations from the surface, and our present knowledge is based on information from cores of deep drillings and interpretation of potential - gravity and magnetic - fields. Accordingly, the basement of Estonia is subdivided into two major geological units - North Estonian amphibolite and South Estonian granulite complexes. Further division includes six structural-petrological zones such as Tallinn, Alutaguse, Johvi, West-Estonian, Tapa and South-Estonian zones. This article provides an updated overview of the Estonian Precambrian basement, its rock types, geophysical fields, geochronology, metamor-phism and metallogenesis.
Keywords: Proterozoic; igneous and metamorphic rocks; geochronology; geophysics; metallogenesis; Estonian basement.
А. Соэсоо, С. Нирги, Ю. Пладо. ЭВОЛЮЦИЯ ЭСТОНСКОГО ДОКЕМ-БРИЙСКОГО КРИСТАЛЛИЧЕСКОГО ФУНДАМЕНТА: ГЕОЛОГИЧЕСКИЕ, ГЕОФИЗИЧЕСКИЕ И ГЕОХРОНОЛОГИЧЕСКИЕ ОГРАНИЧЕНИЯ
Докембрийский кристаллический фундамент Эстонии, состоящий из метаморфических и магматических пород от палео- до мезопротерозоя, перекрыт чехлом осадочных палеозойских отложений мощностью 100-780 м. Так как кристаллический фундамент недоступен для прямого изучения на поверхности Земли, наши нынешние знания основаны на данных глубинного бурения и геофизики (интерпретации гравитационного и магнитного полей). Кристаллический фундамент Эстонии делится на две крупные геологические единицы - Северо-Эстонский амфиболито-вый и Южно-Эстонский гранулитовый комплексы. Дальнейшее деление включает шесть структурно-петрологических зон, таких как Таллиннская, Алутагузе, Йыхви, Западно-Эстонская, Тапа и Южно-Эстонская. В данной статье представлен обновленный обзор докембрийского фундамента Эстонии, типов слагающих его горных пород, геофизических полей, геохронологии, метаморфизма и металлогенеза.
Ключевые слова: протерозой; магматические и метаморфические породы; геохронология; геофизика; металлогенез; кристаллический фундамент Эстонии.
Introduction
The Precambrian crystalline basement of Estonia is covered by a 100-780 m thick deposit of Paleozoic sedimentary rocks. The basement consists of Paleo- to Meso-Proterozoic metamor-phic and igneous rocks. Since there are no outcrops of the crystalline basement rocks, drill core material, geophysical and geochemical methods were used for geological reconstructions. More than sixty years of research have led to a number of publications and reports (before the 1990th, the publications were mostly in Russian), and one monograph [Puura et al., 1983], in addition to several regional geological maps [Grigelis and Puura, 1978; Puura, 1980; Koistinen, 1994]. Based on these investigations, the 1:400 000 scale geological map of the crystalline basement of Estonia was compiled [Koppelmaa, 2002]. The map was based on the results of integrated (petrograph-ical, petrophysical and geochemical) investigations of 32500 metres of drill-cores from ca 490 holes and data from gravimetric and magneto-metric surveys. In the 1990th, a number of articles dealing with general geology [Soesoo, 1991; Petersell and Levchenkov, 1994], geochronology [Petersell, 1991; Puura and Huhma, 1993], meta-morphism [Holtta and Klein, 1991], post-oroge-nic rocks [Soesoo and Niin, 1992; Soesoo, 1993; Kirs and Petersell, 1994; Ramo et al., 1996; Puura and Floden, 1996, 1999, 2000], and partial melting and migmatization [Soesoo et al., 2004a, b, 2006] were published. A special issue, compiling papers on a wide range of geological aspects of the Estonian Precambrian was published in 2004 (Proceedings of Estonian Academy of Sciences, Geology, No. 53, Editor: A. Soesoo).
In the uppermost section of the Estonian basement there is an ancient, dominantly kaolinitic (together with montmorillonite and illite) weathering crust with thickness ranging from a few meters to several tens of meters. Due to intense denudation during the late Proterozoic, the surface of the basement has turned into a pene-plane, which dips gently (average 0.10-0.20°, i. e. 2-3.5 m per km) southward (SSE - SSW; 150-200°). On Vaindloo Island (Gulf of Finland) the crystalline basement lies at a depth of 67.5 m, on Juminda Peninsula at 103.5 m and 629.0 m in Haademeeste (SW Estonia), and at 784.1 m on Ruhnu Island (Gulf of Riga). The relatively level surface of the basement is interrupted by erosion-al relief forms, escarpments generated by tectonic disturbances, dome-shaped uplifts such as Sonda - Uljaste, Assamalla in NE Estonia and Moniste Uplift in SE Estonia. The rim walls of the Kardla impact crater on Hiiumaa Island and Neugrund cra-
ter near Osmussaar Island also appear as positive landforms.
Based on the findings of geophysical and penological studies, the Estonian basement can be divided into two major geological units - the North Estonian amphibolite facies unit and the South Estonian granulite facies unit, which are separated from one another by a tectonic boundary - Pal-diski-Pskov tectonic (shear) zone (PPDZ; Fig. 1). The basement includes six structural-petrological zones such as Tallinn, Alutaguse, Johvi, West-Estonian, Tapa and South-Estonian zones (Fig. 1). These zones differ in rock composition, genesis, geophysical properties, and degree of metamor-phism. The aim of this paper is to present an updated overview of the Estonian Precambrian basement, its rock types, geophysical fields, geochro-nology and metamorphism.
History of Precambrian studies and the position of the Estonian basement within the Fennoscandian orogenic system
A. Opik [1942] was likely the first scientist to propose that the Estonian basement belongs to the Svecofennian orogenic system in the Fennoscandian Shield. From the 1950's to the 1990's, geologists departed from this idea and suggested that higher grade metamorphism, which is usually complemented by high geophysical anomalies, in South Estonia, Latvia, Lithuania and NW Belarus can be correlated to several other high-grade metamorphic complexes in East and NE Europe, and thus can be considered to be of Archaean age [Puura et al., 1976; Gorbatschev and Gaal, 1987]. Subsequent studies of Estonian crystalline rocks in the 1960's - 1980's [e. g., Puura et al., 1983 and references therein] have corroborated that at least the basement of North Estonia is a part of the large Archaean-Proterozoic Fennoscandian (Baltic) Shield (continuation of the Svecofennian orogenic zone). However, there was no direct evidence how far the shield rocks extend towards the south. Until the late 1980's, geologists believed that the granulitic rocks of the South Estonian complex were Archaean, or at least pre-Svecofennian in age [Puura et al., 1983; Gorbatschev and Gaal, 1987]. This assumption was based on lithological correlations of granulitic facies rocks with those of the Kola series [Bondarenko and Dagelaiskii, 1968] and on the idea that regional granulite facies rocks should be older than their lower grade counterparts.
However, the results of Sm-Nd and U-Pb isotopic studies [Huhma et al., 1991a, b; Puura and Huhma, 1993; Petersell and Levchenkov, 1994] suggested that the South Estonian granu-
Ку.Ч Rapakivi and Rapakivi-like granitoid plutons
Microcline granitoids H Dominant amphibolite metamorphic facies
ПИШИ Postorogenicplutons Low-grade amphibolite facies
Dominant granulite metamorphic facies High-grade amphibolite facies
I Retrograde metamorphic facies I---1 Tectonic (shear) zones
Fig. 1. (a) Position of the Estonian Precambrian basement within the Fennoscandian-Baltic tectono-geological crustal structure [as in: Bogdanova et al., 2015]. Two large units - magmatic-volcanic-sedimentary Bergslagen-Livonia "microcontinent" and a large sedimentary Al-gneisses block constitute the Estonian basement. The ages in the frames are those of the principal accretionary events in the indicated domains. The abbreviations for tectonic domains are: AL - Alutaguse, BB - Bothnian (Bothnia microcontinent), BS - Bergslagen (Bergslagen microcontinent), BPG - Belarus-Podlasie granulite belt, CE - Ciechanow, CFAS - Central Finland Arc Complex; CFGC-Central Finland Granitoid Complex (Keitele microcontinent), DO - Dobrzyn, ESL - East Smaland, JO - Johvi, KB - Keitele microcontinent, KZ - Kaszuby, LA - Latgalia, LEL-Latvian-East Lithuanian, LGB - Lapland Granulite Belt, LKO -Lapland-Kola orogen, LS - Ljusdal, MD-Mazowsze, MLD-Mid-Lithuanian domain, NB - Norrbotten, NO - Novgorod, OKL - Okolovo, OMIB - Osnitsk- Mikashevichi Igneous Belt, PM - Pomorze, SEG - South Estonian granulite domain, T - Tapa, TN - Tallinn, Uu - Uusimaa, VV-Vastervik, WE - West Estonian domain, WLG - West Lithuanian granulite domain. Deformation zones: HGZ-GR - Hagsta-Gavle-Rattvik Zone, HSZ - Hassela Shear Zone, KSZ - Karlskrona Shear zone; LLSZ - Linkoping-Loftahammar Shear Zone, MEFZ - Middle Estonian Fault Zone, PPDZ - Paldiski-Pskov Deformation Zone, SFSZ - South Finland Shear Zone, VNSZ - Vingaker-Nykoping Shear Zone, and for volcanic belts and sedimentary basins: H - Hame, Mk - Monki, O-J - Oskarshamn-Jonkoping, P - Pirkanmaa, Pc - Poceai, Sc -Salcia, Tm - Tampere; (b) Geological-structural zones of the Estonian Precambrian basement
lites are more likely early Proterozoic than Archean in age. The studied granulites yielded mantle extraction model ages of about 2 Ga, which is younger than Archaean, but somewhat older than typical Svecofennian rocks in southern Finland and Sweden.
Based on petrographic and geochemical similarities, the North Estonian amphibolite facies rocks were believed to belong to a section of Sve-cofennian rocks cropping out in Southern Finland. This view has remained unchanged. More studies were needed to establish the structural-geological position of the South Estonian granulites. Two case studies focusing on the metamorphism of granuli-te zones have been performed [Holtta and Klein, 1991; Kikas, 2001] and a compilation on the general features of metamorphism was produced [Puura et al., 2004]. New isotopic studies confirmed the Proterozoic ages of Estonian granulites [Soesoo et al., 2006].
Ideas about the magmatic and tectonic evolution of the Svecofennian Orogen have changed during the last decades. Hietanen [1975] proposed a model which explains rock variations in the Fen-noscandian Shield by opening of an oceanic basin, subduction and island arc magmatism. More recent and complex magmatic and tectonic models have been proposed by Baker et al. [1988], Gaal [1990], Park [1991], Lahtinen [1994], and Nironen [1997]. In the recent models, the evolution of the Svecofennian Domain is interpreted as multiple, time- and space-dependent subduction-re-lated collisions of several island-arc structures. It is thought that the 1.91-1.8 Ga magmatism and metamorphism were related to these collisions. A new advanced and detailed Trans-Scandinavian-Baltic compilation has been published by Bogdanova et al. [2015].
The nature of potential geophysical fields in Estonian territory has been studied since the early 1950's, when Fotiadi [1958] provided the structural zonation of the basement on the basis of magnetic and gravity fields. The rationale is that potential fields display the structure of the crystalline basement whereas the effect of the overlying sedimentary cover is minor. Ideas about the sources for different types of geophysical anomalies have, however, changed several times according to the incoming data from additional deep drillings [Puura, 1980; Puura et al., 1983; Ankudinov et al., 1994].
Geological features of geological zones of the Estonian Precambrian basement
The crystalline basement of Estonia comprises Palaeoproterozoic metamorphic and igneous
rocks, and a Subjotnian (late Palaeoproterozoic to early Mesoproterozoic) population of Rapaki-vi granite-type rock suites. The ca. 30 km wide, NW-trending PPDZ separates the structural domains in northern and north-eastern Estonia from those in the west and the south of Estonia (Fig. 1). It comprises two principal sub-parallel shear zones dipping between 65° and 75° SSW [All et al., 2004], features strong deformation, and contain slivers of both granulite- and amphibolite-facies rocks.
The PPDZ is well exhibited in gravity (Fig. 2) and magnetic (Fig. 3) fields by a combination of elongated local positive and negative anomalies. The structural domains north and south from the tectonic zone were, according to their anomaly patterns, initially [Fotiadi, 1958] named as North Estonian Geophysical Low and Baltic-Belarus Geophysical High, respectively. North of the tectonic zone, rocks with their relatively low density and magnetization cause local negative gravity and magnetic anomalies. Also, the fields are relatively smooth with rare short-wavelength anomalies. South of the tectonic zone, the high density and magnetization of granulites produce local positive anomalies and relatively high gradients, which are especially outstanding in magnetic field data (Fig. 3).
On the basis of previous geophysical and petrological studies, six geological zones are distinguished within these two units: Tallinn, Tapa, Alutaguse and Johvi zones (located north of the PPDZ), and the West-Estonian and South-Estonian zones (located south of the PPDZ; Fig. 1) [Puura et al., 1983; Koistinen, 1994; Soesoo et al., 2004a]. These zones mostly differ in rock assemblages (with metasedimentary or metavolcanic/-igneous origin), metamorphic grade and petrophysical properties of rocks, reflected in their potential fields.
The Tallinn Zone is characterised by negative free-air gravity and magnetic fields. The zone is bordered by a regional PPDZ in the southeast, which separates it from the West-Estonian Zone. Another less prominent tectonic disturbance zone separates the Tallinn Zone from the Tapa Zone in the east. The rocks of the Tallinn zone vary from mafic amphibolite facies metavol-canites to metasediments represented by amphibole gneisses, biotite-plagioclase gneisses, quartz-feldspar gneisses, mica gneisses, and minor sulphide-graphite gneisses and magnetite quartzites (Jagala complex). Migmatisation is generally common and locally strong. The Tallinn Zone may represent a volcanic arc that continues in the Uusimaa belt in Finland [Kahkonen, 2005].
East of the Tallinn Zone, the Alutaguse Zone and the smaller Johvi Zone are distinguished
Fig. 2. Free-air gravity anomaly model. The map is based on the Estonian Gravity Database that was recently published by Oja et al. [2019] (Fig. 11). Raw data include 31,850 high-quality gravity points covering mainland and islands. International cooperation and marine survey projects have resulted in additional 17,339 points
(Fig. 1). The Alutaguse zone is characterised by near-zero free-air gravity and slightly negative magnetic anomalies. Local positive anomalies appear in the area of Sonda - Uljaste and Assamalla dome-like structures, Haljala and Luusika [Dmitrie-va et al., 2018] area, which are associated with sulphide-graphite gneisses (black schists), quartz-ites, skarned carbonaceous rocks and pyroxene gneisses. The main rock types of the Alutaguse Zone are Al-rich gneisses (with biotite, cordierite, garnet, sillimanite) and biotite-plagioclase gneisses, less abundant are amphibole gneisses, amphi-bolites and quartz-feldspar gneisses. The rocks of the Alutaguse zone have metamorphosed under the amphibolite facies conditions. In some places (Sonda - Uljaste and Haljala) the rocks show evidence of granulite facies metamorphism. Migmati-sation is common and locally strong.
The mostly metasedimentary Alutaguse Zone may be a part of the Kalevian-age marginal basin, which extends to the vicinity of St. Petersburg in Russia and farther east to Lake Ladoga [Bogdanova et al., 2015]. The deposition of tur-bidites in that basin has been estimated to have taken place between 1.96 and 1.90 Ga [Lahtinen et al., 2010; Melezhik and Hanski, 2012]. However, the ages of deposition and metamorphism of the Alutaguse metasedimentary sequence
are still unknown. Bogdanova et al. [2015] has noted that similar turbidites may also occupy the Novgorod Zone in Russia. This zone is characterized by an irregular mosaic field of low magnetic anomalies, resembling that of the Bothnian area in the Fennoscandian Shield, and may thus be a representative of an ancient microcontinent [Peive et al., 1979].
The Tapa Zone is bordered by tectonic contacts from the Tallinn Zone in the west and Alu-taguse Zone in the east, while the southern contact with the West-Estonian Zone is not so clearly defined (Fig. 1). The zone is characterised by slightly positive gravity and frizzy magnetic anomalies. The main rock types comprise a sequence of alternating Fe- and S-rich garnet- pyroxene-bearing quartzites, high-Al garnet-cordierite-sillimanite gneisses, and Ca-rich and Ca-poor pyroxene-, amphibole- and biotite gneisses. Mineralogical assemblages indicate amphibolite and granulite facies metamorphism. Migmatisation has resulted in potassium-feldspar- and plagioclase-rich leu-cosomes and granitic veins and bodies, and char-nockitic veins in granulitic areas [Soesoo et al., 2006]. Generally, these rocks are mineralogically similar to those of the West-Estonian Zone (below). Also, the nature of their geophysical fields is similar to that in the West-Estonian Zone.
Aeromagnetic anomaly
Fig. 3. Aeromagnetic map of Estonia. It is based on campaigns between 1987 and 1992 (unpublished reports in the Depository of Geological Reports by the Geological Survey of Estonia, see [All et al., 2004] for detail)
The narrow Johvi Zone is separated from the South-Estonian Zone by the Alutaguse Zone amphibolite grade gneisses. The Johvi Zone (Fig. 1) is characterised by extremely strong (up to 20 000 nT in the Johvi magnetic anomaly) E - W trending magnetic anomalies and slight positive gravity anomalies. The complex consists of pyroxene gneisses, quartz-feldspar gneisses, bio-tite-plagioclase gneisses, amphibole gneisses, garnet-cordierite gneisses (Vaivara complex), and magnetite-rich quartzites and gneisses (Johvi magnetic anomaly). Migmatisation is widespread, resulting in the formation of plagioclase and potassium-feldspar porphyroblasts, occasionally leuco-somes and small granitoid veins and bodies with charnockitic and enderbitic compositions. Generally, these rocks have formed under the conditions of granulite facies metamorphism. The rocks of this zone have a high ore potential.
The West-Estonian Zone is bounded by the NW- trending PPDZ and the E-W striking Middle-Estonian tectonic zone (MEFZ). The zone is dominated by metasedimentary rocks in the am-phibolite to granulite facies, resembling somewhat the rocks in the southern part of the Bergslagen area in Sweden [Bogdanova et al., 2015]. The eastern part of the West-Estonian Zone is characterised by NW - SE striking strong linear magnetic anomalies, while the anomalies in the western part of the zone are mostly NE - SW or sub-N - S
striking (Fig. 3). The free-air gravity anomaly is slightly positive (Fig. 2). The West-Estonian zone is also cut by several Proterozoic tectonic zones, the largest of which is the Hiiumaa - Espoo shear zone. The main rock types in the West-Estonian Zone are medium- to fine-grained amphibolites, biotite-plagioclase gneisses, and quartz-feldspar gneisses with minor pyroxene gneisses. The mineral assemblage of these rocks points to the high-temperature amphibolite facies and in a number of places to the granulite facies metamorphism [Puura et al., 1983, 2004]. The latter often contains migmatites or small granitic bodies of enderbitic composition, otherwise plagioclase - K-feldspar leucosomes and granites prevail.
The South-Estonian Zone (Fig. 1) was thought to be a part of the approximately 1000 kilometres long Belarus-Baltic Granulite Belt [Puura et al., 1983; Soesoo et al., 2004a]. which comprises predominantly meta-igneous rocks and minor meta-sedimentary rocks. The South-Estonian Zone is characterised by a band of intensive gravity and magnetic anomalies (Figs. 2 and 3) embracing the southern part of Estonia and northern Latvia. The magnetic field is strongly differentiated, the anomalies are generally linear and trend E - W or N - S. The gravity field anomalies are coarsely mosaic. The boundary between the South-and West-Estonian zones generally follows the tectonic zones. The South-Estonian Zone contains
both mafic and felsic granulitic components - am-phibole-pyroxene and biotite-hypersthene gneisses, and quartz-feldspar gneisses. Both charnock-itic and granitic migmatisation is observed. Some charnockites belong to a calc-alkaline I-type series, likely generated due to the melting of lower crust under granulite facies conditions along with the emplacement of some mafic dykes [Soesoo et al., 2006; Bogdanova et al., 2015]. This is somewhat younger than the 1.81 Ga age of the granulite facies metamorphism in northern Latvia [Mansfeld, 2001]. In the southeast, the granulite continuation incorporates the large East Latvian block, which shows similarly a mosaic-type magnetic anomaly. The block is surrounded by linear anomaly belts and has previously been interpreted as an "Archaean" microcontinent [Bogatikov and Birkis, 1973] similar to the Novgorod domain [Bogdanova et al., 2015].
The evolution of the southern part of this zone commenced with metamorphism under amphibo-lite facies conditions, followed by peak (granulite facies) metamorphism under pressure and temperature conditions ranging between 740-760 °C at 7-8 kbar and 770-850 °C at 5.5-7 kbar [Taran and Bogdanova, 2001]. According to Bogdanova et al. [2015], the South-Estonian Zone is no longer the northern extension of the Belarus-Baltic granulite belt, but is truncated by the latter, which is now considered to associate with Sarmatia rather than Fennoscandia.
In conclusion, the rocks with granulite metamor-phic assemblages are found in a number of zones within the Estonian basement. In the South-Estonian and Jôhvi Zones, the granulite facies mineral assemblages are still preserved, while in the Tapa and West-Estonian Zones the rocks were mostly retrogressed under amphibolite facies conditions [Puura et al., 1983, 2004; Fig. 1].
Metamorphism of the Estonian Precambrian basement
Metamorphic rocks predominate in the Pre-cambrian basement of Estonia. Earlier mapping of the buried basement rocks was performed by combining regional potential geophysical field data and drill core studies of about 490 drill holes. These metamorphic belts belong to the uniform Svecofennian crustal domain spreading over 1 million km2 in the western corner of the East European Craton [Puura et al., 2004]. Within this domain, metamorphic zones from low- to high-grade metamorphism have been observed. Within the Estonian basement, the rocks of high-grade amphibo-lite to granulite facies dominate. Detailed studies, however, revealed that spatial variations in me-
tamorphic grade are widespread. Metamorphic gradients related to fault zones, roughly circular or belt-form areas of increasing metamorphic grade (metamorphic domes) feature the general highgrade metamorphic field.
The structural-geological zones distinguished in the basement of Estonia substantially vary also in metamorphic lithologies. Previous studies have revealed that in primary supracrustal suites, a large variety of mafic, intermediate and acidic volcanic rocks, as well as clastic sediments from clays to sands, occasionally with carbonate admixture, constitute the basement rock units [Koppelmaa et al., 1978; Puura et al., 1983; Klein, 1986]. Some information on the protoliths of metamorphic rocks has been obtained by studying the typologies of zircons [Konsa, 1986; Konsa and Puura, 1999].
The average mineral contents of different supracrustal rocks in these geological zones of the basement were reported by Puura et al. [2004]. For example, in Tallinn and Alutaguse zones, Al-rich garnet-, cordierite- and silli-manite-bearing-gneisses and biotite gneisses account for 25.4 vol% and 90.5 vol%, respectively, while biotite-plagioclase and K-feldspar-bearing gneisses constitute 24.4 % and 1 %, respectively. Biotite-plagioclase, hornblende-plagioclase, pyroxene-plagioclase gneisses and amphibolites constitute 50.2 vol% and 6.1 vol%, respectively [Klein, 1986].
In the South- and West-Estonian zones, pyroxene- or hornblende-bearing mafic metavolcanic rocks dominate, respectively, whereas metapelites and granitic gneisses are rare. Pre-metamorphic textural features in high-grade metamorphic rocks have been obliterated. However, occasionally graded bedding has been observed in metapelites. Sedimentary protoliths of metapelites in the Tallinn and Alutaguse zones are supported by findings of zoned zircons, whose rounded cores suggest their detrital origin [Konsa and Puura, 1999]. The distinction between sedimentary or volcanic origin of metamorphic suites, especially in cases of Ca-rich composition resembling mafic volca-nics, was drawnusing the bulk chemical composition and spatial relationships of metamorphic rock suites in metamorphic sequences [Puura et al., 1983].
Based on the mineral parageneses and chemical compositions of minerals (historical wet chemical analysis of garnet, biotite and amphibole fractions [Puura et al., 1983; Klein, 1986] and microprobe analyses [Kikas, 2001], the peak metamorphic conditions in the main structural zones of the Estonian basement were estimated. The data revealed that high temperature and moderate pressure amphibolite facies conditions do-
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minated in the Tallinn and Alutaguse zones. Geo-thermobarometry of biotite+garnet+/-sillimanite assemblage and cordierite suggests peak meta-morphic conditions at 600-700 °C and 3-5 kbar [Klein, 1986; Koistinen, 1996]. In South Estonia, the mineral parageneses of intermediate and mafic metavolcanics and Al-rich gneisses correspond to granulite facies. Widespread garnet and cordierite in these rocks formed by the breakdown of bio-tite and sillimanite, which indicates prograde metamorphism. However, in many places retrograde assemblages formed in the conditions of am-phibolite facies metamorphism. Holtta and Klein [1991] studied drill cores in the granulite rocks of South Estonia and gave pressure estimates close to 4-6 kbar and formation temperature at around 700-800 °C.
Kikas [2001] performed detailed studies of rock-forming mineral assemblages from rocks of the Konnu drill core (granulite facies, South-Estonian Zone) and the Valgu drill core (amphiboli-te facies, West-Estonian Zone). These drill cores were located close to the MEFZ (Fig. 1), virtually on its opposite sides. Traces of partial melting imply that melting was the prominent mechanism for dehydration of rocks in the Konnu and Valgu drill cores. In the granulitic rock, the occurrence of or-thopyroxene and hercynite, and a specific chemical composition of high-grade phases, such as high titanium content in biotite and high alumina content in orthopyroxene, are in accordance with geothermobarometric estimates, which suggests a peak temperature of formation over 800 °C and pressure of 5-6 kbar. In amphibolitic rock, geothermobarometric estimates suggest peak conditions at the upper amphibolite facies - temperature ~700 °C, and pressure ~4.5-5.5 kbar. These estimates show a difference in the meta-morphic stages and history between the West-Estonian and the South-Estonian zones leading to the general conclusion that the South-Estonian Zone shows a deeper erosion level.
Precambrian unmetamorphosed igneous rocks in the Estonian basement
Within the Estonian basement, post-orogenic (later than Svecofennian collisional processes) and anorogenic (independent from Svecofennian orogenic framework) magmatic rocks were recognized by drilling and from gravity and magnetic investigations back in the mid-20th century [Tikho-mirov, 1965; Bogatikov and Birkis, 1973; Kuuspa-lu, 1975; Puura et al., 1976, 1983; Velikoslavinsky et al., 1978; Kirs and Petersell, 1994; Ramo et al., 1996]. This rock group has been relatively well studied. Generally, the igneous rocks are widely
distributed in the Proterozoic basement of Estonia, however, they do not form large plutons. Granitic rocks are widespread and present in about 400 drill cores. The group of granitic igneous rocks also contains effusive varieties, which are found in more than 80 drill cores. Intermediate to basic and ultrabasic rocks are much less common - they are present in about 80 drill cores.
In the historical research, mostly based on drill core observations, the granitoids are traditionally divided into syn- and late-orogenic granites [Niin, 1997]. The synorogenic granitoids were described from about 50 drill cores, where hyperst-hene-bearing charnockites and enderbites predominate. Geochemically, synorogenic granites show type I characteristics and their genesis is related to granulitic metamorphism [Niin, 1997], although some authors have investigated them together with late-orogenic migmatite granites [Puura et al., 1997]. These granites are widely spread in the South-Estonian and Johvi granulitic zones, where they form veins, small lenses and bodies. The other group of synorogenic granitoids is represented by granodiorites and occasionally quartz diorites. These rocks show gneissic structure and occur mainly as small plutons. They are usually found in the Tallinn and Johvi zones.
The Estonian late-orogenic granitoids occur in more than 300 drill cores and are known in all geological zones, although less often in the South-Estonian and Johvi granulitic zones. In the mineral and chemical composition granites, granodiorites dominate, tonalites and adamel-lites occur less often, while quartz-diorites, quartz-monzonites and quartz syenites are recorded only in a few drill cores. Usually, they form veins, but migmatitic rock bodies are also frequent. These granites are mainly massive, pegmatoid texture is common, gneissic varieties are rare, while porphy-raceous texture occurs very seldom. Most of them probably have metasomatic or anatectic origin [Niin, 1997]. Most of the quartz-feldspar- and granitic-gneisses are considered to belong to acid metavolcanites [Niin, 1997] such as dacites, rhyo-lites, porphyries, etc. Acid metavolcanic rocks are the most common in the West-Estonian and Tallinn zones.
Intermediate rocks were described from about 40 drill cores, half of them from the West- Estonian Zone. The main types of intermediate igneous rocks are gabbroic diorites (meta? - gabbro-dio-rites) and diorites. The mafic, basic in composition, igneous rocks are found in more than 70 drill cores; again, half of them in the West-Estonian Zone [Niin, 2002]. However, most of them show metamorphism. The share of ultrabasic igneous rocks in the crystalline basement of Estonia is
(25)
small (four drill cores) and they have commonly been considerably altered during metamorphism and secondary processes [Niin, 2002].
Anorogenic rocks belong to the Fennoscandian Paleo - Mesoproterozoic Rapakivi Province [Kois-tinen, 1994; Puura and Floden, 1999] and include the huge composite Riga batholith, as well as at least five minor stock-like porphyritic K-granite plutons - Naissaare, Marjamaa (with its Kloostri satellite), Neeme, Ereda and a quartz-monzodi-oritic Abja stock in SW Estonia [Kuuspalu, 1975; Soesoo and Niin, 1992; Soesoo, 1993]. All the rock bodies, except for the Abja pluton, are situated in the northern part of Estonia (Fig. 1). Usually, these plutons are seen in strong but short-wavelength positive magnetic anomalies.
The anorogenic Riga pluton, which forms the southern part of Riga-Aland Rapakivi Subprovince [Puura and Floden, 1999], contains both mafic and silicic rocks, which are petrograph-ically and geochemically analogous to the typical members of the Fennoscandian Rapaki-vi-anorthositic suite. As in the case of other large rapakivi granite batholiths, a considerable effect of crustal thinning - at a scale of 10 km - has occurred in the Riga batholith area in connection with its formation [Puura and Floden, 1999, 2000]. Geophysical effects of the Riga pluton are expressed in low-gradient negative to near-zero gravity and magnetic fields in the Gulf of Riga, SW Saaremaa and the Courland Peninsula in Latvia (Figs. 1-3).
These small Rapakivi-like porphyritic potassium-granite intrusions in the Estonian mainland show up as small gravity and magnetic minima (Ereda, Neeme, Naissaare, Taebla, and Kloostri stocks), and comprise pink, medium- to coarsegrained, microcline-megacrystic, partly trachyt-oid biotite (in Marjamaa and Naissaare also bio-tite-hornblende) syeno- and monzogranitic rock, locally cut by aplitic and microsyenitic dykes [Kuuspalu, 1975; Kirs, 1986; Soesoo and Niin, 1992]. As an exception, Marjamaa pluton is more differentiated with an anomalously high-magnetic central part containing hybrid granodiorite with hastingsitic hornblende as the main mafic mineral. The major and trace element contents of these porphyritic potassium-granites are similar to or overlapping with those of typical Finnish rapakivi and comparable with the less differentiated granitic phases from the Wiborg and Laitila plutons [Kuuspalu, 1975; Soesoo and Niin, 1992; Kirs et al., 2004]. Marjamaa pluton is accompanied by a remarkable ellipsoidal magnetic high and an annular low (Fig. 3). A central weakly positive local gravity anomaly with a negative ring (Fig. 2) also associates with Marjamaa.
The Abja quartz- monzodioritic pluton in SW Estonia is strongly magnetic and consists of a dark gray, massive, medium-grained, partly weakly gneissose rock with abundant accessory apatite and titanomagnetite. It is intersected by veins of fine to medium-grained slightly porphyritic plagioclase-microcline granite. The Sigula intrusion in North Estonia consists of medium grained gabbro-monzonitic rock with ophitic texture and of massive structure. This rock is very rich in titanomagnetite (up to 10 %), apatite (2-4 %), and titanite. The other postorogenic body - Utria stock in NE Estonia, consists of medium-grained fresh, non-amphibolised gabbro-diorite with high titanite (3-5 %) content.
Geochronology of the Estonian basement
The first attempts to determine the isotopic age of the Estonian basement rocks were carried out in the 1970's [Puura, 1974]. Three groups of isotope systematics (K-Ar, Sr-Rb and U-Pb) were used in geochronological studies. In the early 1990's, Sm-Nd analyses on the granulitic gneisses from the South Estonian drill cores were carried out [Huhma et al., 1991b; Puura and Huhma, 1993]. These results along with new U-Pb zircon age determinations [Petersell, 1991, 1993; Petersell and Levchenkov, 1994; Ramo et al., 1996] eventually refuted the decades-long opinion of an Achaean age of South Estonian granulites and suggested a Palaeoproterozoic age for the granulite protolith.
The U-Pb zircon age of metavolcanic rocks of amphibolitic facies from northern Estonia (for example drill core F-164) yielded a range of ages within the 5 zircon fractions analysed - from 1889 Ma to 1844 Ma, while the isochrone age was 1918 ± 10 Ma [Petersell and Levchenkov, 1994]. Thirteen samples of granulitic metavolcanic rocks of the South-Estonian Zone yielded U-Pb zircon ages between 1833-1802 Ma and isochrone age groups of 1832 ± 22 and 1827 ± 7 Ma [Petersell and Levchenkov, 1994]. Al-rich gneisses of meta-sedimentary origin from the same rock complex (drill core F-502) showed a range of TIMS multi-grain U-Pb zircon ages between 1930 and 1841 Ma. Preliminary studies of zircons (drill core F-502) by the laser ablation ICP-MS technique also showed a range of ages - from 1900 to 1736 Ma [Soesoo et al., 2004a] (Table). The relatively large range of ages within the metasedimentary component probably points to mixed populations of zircons, where some older, but radiogenical-ly similar sedimentary material may be present. U-Pb monazite dating of an orthopyroxene-gar-net gneiss form the South-Estonian Zone yielded an age of 1778 ± 2 Ma [Puura et al., 2004].
Rock types, general geochronology, possible correlations and tectonic settings of the rock complexes of the Estonian
basement [modified after: Kirs et al., 2009]
Period (Ga) Isotopic age, Ga Rock types Geographical position Possible correlations Tectonic settings
<1.40 Late Calymmian erosion and intraplate processes
CALYMMIAN 1.60-1.40 Some uplift, extensional tectonics
1.59-1.54 quartz-porphyries, plagi-clase-porphyrites Rapakivi plutons of Riga-Aland subprovince: Riga pluton SW Finland and central Sweden Uplift Extension?
1.60
STATHERIAN 1.80-1.60 1.67-1.62 quartz-porphyries, plagi-clase-porphyrites, Rapakivi plutons of Wiborg subprovince: Märjamaa, Neeme, Ereda, Naissaare, Taebla plutons Suursaari, Gulf of Finland Block tectonics, extension? volcanism
shoshonites shoshonitic pluton: Abja S and SE Finland, Ladoga area Uplift, extension?
1.80 Amalgamation of Fennoscandian, Sarmatian etc. megablocks, Formation of Columbian Supercontinent
OROSIRIAN 2.05-1.80 1.83 post-orogenic shoshonites shoshonitic plutons: Virtsu, Taadikvere, Muhu S and SE Finland, Ladoga area Uplift, erosion, extensional collapse
1.84-1.80 granites, microcline granites, charnockites N and NW Estonia SE Sweden, Central and S Baltic area, S and SE Finland Processes at active margins, island arc & back-arc basins
1.93-1.88 granites, microcline granites, charnockites N and NW Estonia Finland, NW Russia Processes at active margins and back-arc basins
>2.05 Opening and spreading of the Svecofennian ocean
These ages are significantly younger than the ages of other mafic meta-igneous rocks from northern Estonia or granulite facies rocks in Finland [Huhma et al., 1991a].
Metavolcanites from the four SW Estonian drill cores demonstrated a Sm-Nd model age (TDM) of 2.08 to 2.18 Ga, while eNdT varied from +0.2 to +2.0 [Huhma et al., 1991b]. Partial melting
of granulitic rocks of the South-Estonian and Tapa zones has been studied by Soesoo et al. [2006]. Zircons extracted from the tonalite of the Tapa Zone yielded 1824 ± 26 Ma, while tonalite from the South-Estonian Zone yielded the age of 1788 ± 16 Ma. Charnockite from the Tapa Zone yielded 1761 ± 11 Ma [Soesoo et al., 2006]. These U-Pb crystallisation ages span over ca. 80 Ma,
suggesting a prolonged high-grade metamor-phism or several separate metamorphic/melting events. An attempt was made to compare zircon U-Pb and whole-rock Nd ages (Fig. 4). The Nd model age of partial melting of granulite facies mafic gneiss shows an intercept age of 1760 Ma, which is in good concordance with the U-Pb zircon age from the same charnockite sample - 1761 ± 11 Ma (Fig. 4).
Some new geochronological data just became available from the Johvi Zone. Zircons from the gneisses, which are associated with a large body of magnetite quartzites, represent three groups of ages. A majority of the zircons show 1826 ± 10 Ma, the youngest population is at 1789 ± 19 Ma, while the third population gives the isochrone age of 1874 ± 18 Ma (RITA project, unpublished data). These gneisses are migma-tised and the magnetite-quartzites are cut by mi-crocline granite veins. The granitic vein yielded an U-Pb zircon age of 1800 Ma, which may be the age of migmatization (A. Soesoo, unpublished data). The latter age is similar to the ages of late-and/or post-orogenic granites in southern Finland [Nironen, 2005; Kurhila et al., 2011].
The knowledge about the age of metamorphism is based on a few studies of U-Pb analysis of zircon and monazite and some other isotope studies of rocks and minerals [Puura et al., 2004; Soesoo et al., 2006]. The granulite metamorphism age is difficult to estimate directly, however monazite from an Estonian orthopyrexene-garnet gneiss (drill core F-300, South-Estonian Zone) yielded an age of 1778 ± 2 Ma [Puura et al., 2004]). This age is similar to that of gabbro-noritic dyke which cuts the same granulites - 1.774 ± 20 Ga (A. Soesoo,
15
-30 ------1----— - . -->-----------
0 500 1000 1500 2000 2500
Age Ma
Fig. 4. Evolution of Nd isotopic composition in the mafic gneiss and its partial melting product - charnockite - relative to the evolution of the Chondritic Uniform Reservoir (CHUR [Jacobsen and Wasserburg, 1980]) and depleted mantle (DM [Goldstein et al., 1984; Michard et al., 1985]). Note that the U-Pb zircon age of the charnockite is the same - 1761 ± 11 Ma [modified from: Soesoo et al., 2006]
unpublished data). The Sm-Nd age of garnets from this gneiss yielded 1728 ± 24 Ma, which can be interpreted as the age when the rocks cooled down to the closure temperature of garnets, i. e. ca. 650-700 °C. The associated tonalite from the South-Estonian Zone gave comparable U-Pb zircon ages - 1788 ± 16 Ma [Soesoo et al., 2006], similar to whole-rock Sm-Nd and U-Pb zircon ages of partial melting within the Tapa Zone (1760 Ma [Soesoo et al., 2006]; Fig. 4). Supposedly, the formation of tonalites and charnockites (likely conditions: 850 °C and 6 kbar) in Estonian granulites occurred at ca. 1788-1778 Ma. Then, the rocks cooled down, passing through the garnet closure temperature of ca. 650-700 °C at 1728 ± 24 Ma. Thus, the age of metamorphism of the Estonian granulites is lower than the metamorphic ages known from southern Finland, but it is similar to the age of metamorphism reported from the Belarus-Baltic Granulite Belt in Latvia.
The U-Pb and Sm-Nd isotopic studies on the Svecofennian granulite areas in Finland clearly show that there are two distinct granulite facies pulses, at ca. 1.88 Ga and at ca. 1.80-1.83 Ga. Migmatites from the Turku area have yielded U-Pb zircon ages of ca. 1.82 Ga [Vaisanen et al., 2002]. The West Uusimaa migmatites have yielded U-Pb ages on monazites from 1816 ± 2 Ma to 1832 ± 2 Ma, whereas Sm-Nd on garnet gives an average age of 1803 ± 6 Ma [Vaisanen et al., 2002].
The post-orogenic magmatism is represented by small monzonite-type mafic to felsic plu-tons of shoshonitic geochemical affinity, originating from enriched lithospheric mantle, and having been emplaced within the Estonian crust at 1830? - 1630 Ma [Soesoo and Hade, 2012]. Partly gneissic rocks of the Muhu quartz-monzonite and Taadikvere granodiorite plutons show an U-Pb isotope age of about 1830 Ma (V. Petersell, unpublished data), which is in a problematic position to metamorphism (Table). The shoshonitic Virtsu pluton yields, however, an U-Pb age of about 1610 Ma [Soesoo and Hade, 2012]. The quartz-mon-zonite of the Abja pluton shows a similar zircon U-Pb age - 1638 Ma. It is interesting to note that the granitic rocks emplaced into the Abja mafic pluton show zircon fractions with ages from 1610 to 1515 Ma with an isochrone age of 1622 ± 7 Ma [Kirs and Petersell, 1994] (Table).
In spite of age differences between the Muhu (1803 Ma), Abja and Virtsu (1606 and 1638 Ma, respectively) shoshonites, they all show similar chemical affinities. It is also interesting that some of the Virtsu and Muhu rock types (high-K varieties) are chemically similar to the Finnish rapakivi granites, while others are similar to shoshonites.
The Fennoscandian anorogenic anortho-site-rapakivi plutons developed in the time span of 1.67-1.45 Ga within the Svecofennian juvenile crust. Several igneous Rapakivi subprovinces consisting of mafic to felsic intrusive rocks and volcanic facies have been distinguished in the region. They can be divided into two large units: the Wi-borg Subprovince of 1670-1620 Ma and the Ca-lymmian Riga-Aland Subprovince of 1590-1540 Ma age. As Estonia is located in the central part of the Fennoscandian rapakivi province, granitoids temporally similar to both Rapakivi subprovinces are found here. Granodiorite of the Marjamaa plu-ton yields an U-Pb zircon age of 1650-1630 Ma [Ramo et al., 1996; A. Soesoo, unpublished data]. The Neeme granitoids yield an U-Pb zircon age of 1634 Ma and the Taebla rocks 1648 Ma, whereas the Ereda rocks show two age groups of 1642 and 1627 Ma (A. Soesoo, unpublished data).
The Calymmian granitoids in Estonia are so far known only from the Riga-Aland rapakivi Subprovince, on the islands of Saaremaa and Ruhnu. The basement beneath the Gulf of Riga as well as on Ruhnu Island and western Saaremaa Island is represented by the northern portion of the Riga batholith. Zircons from the Riga batholith yield ages of 1576-1584 Ma [Ramo et al., 1996]. Zircons from a subvolcanic biotite granite porphyry unit in Ruhnu Island (Riga batholith) yield an age of 1595 Ma [Soesoo and Hade, 2012] (Table).
Relying upon the available data it can be concluded that the Svecofennian orogenic structures in the Estonian basement formed during Paleo-Proterozoic time, 1.8-1.9 Ga and compose magmatic, volcanic and sedimentary components across both major structural zones. The granulite metamorphism and possibly the associated mafic magmatism (including crustal melting events) postdate these ages. It is not clear yet whether the age differences between granulitic (SW Estonia) and amphibolitic facies (NE Estonia) volcanic rocks hint at differences in the geotectonic position of these rocks or are explained by different exhumation sections, or both.
Metallogenesis of the Estonian Precambrian basement
Along with the fundamental studies describing the evolution of the crystalline basement, the signs of metallogeny have always been taken into account as potential economic resources. Moreover, during the crystalline basement mapping, a fair amount of the deep drill holes were drilled for exploration purposes to determine the geological features that are causing magnetic and gravimetric anomalies. As a result, several geochemical anomalies of high metal concentrations have been detected (Fig. 5).
Previous geochemical studies [Kivisilla, 1987] show that north-eastern Estonia together with
Fig. 5. Geochemical anomalies in the Estonian Precambrian basement. Anomaly symbol represents the most prominent metal of the mineralization
29
the Tallinn Zone differs from the crystalline basement in their higher concentration of chalcophile and si-derophile elements, making it relevant from metal-logeny and therefore the ore potential points of view.
Mn-rich magnetite quartzites are found in the Johvi Zone of the Vaivara rock complex, forming the Johvi iron ore deposit, and in Sakusaare, where comparable mineralization can be seen in the Jagala rock complex of the Tallinn zone [Luha, 1946; Erisalu and Arvisto, 1969; Petersell, 1976; Petersell et al., 1985].
First studies on Johvi magnetite quartzites were carried out in 1918-1939 [Luha, 1946]. As the magnetic anomaly is complex and produced by subvertical ore bodies, only 5 out of 17 holes drilled in the area of the anomaly intersected Fe-quartz-ites [Erisalu and Arvisto, 1969]. Fe-mineralization spreads in garnet-cordierite, amphibole- and pyroxene gneisses. Banded magnetite with occasional braunite inclusions and quartz interlayers is often seen together with pyrrhotite and pyrite [Puura and Kuuspalu, 1966; Petersell et al., 1985]. In rare occasions, magnetite is replaced by hematite and in some cases up to 10 % of the magnetite is replaced by goethite. Magnetite quartzites contain up to 45 % total iron per 1 metre interval. The total depth of the ore body exceeds 721 m, although the true thickness has not yet been determined.
Various concepts of ore genesis have been proposed for Johvi Fe-quartzites. A. Linari [1940] suggests the ore is skarn-like. Also, ore genesis through metasomatism has been proposed [Va-ganova and Kadorova, 1948], where Fe-quartz-ite was formed from mafic rocks during regional metamorphism while in contact with granites. Ti-homirov [1966] has described rocks as alternating layers of skarn, cummingtonite, biotite-sillimanite and other hornfels that are cut by granite veins. However, the most widely recognized is the concept of metamorphic rocks of volcanogenic-sedi-mentary origin [Puura and Kuuspalu, 1966; Erisalu and Arvisto, 1969].
Additionally, a slight amount of fine-grained magnetite along with hematite, pyrrhotite and pyrite may occur in small-grained cordierite-silli-manite-biotite metasedimentary alumo-gneisses throughout Estonia. In gabbroic intrusions, ilmen-ite-magnetite and magnetite-apatite mineralization has also been noted [Petersell et al., 1991].
Along with various iron-related minerals, significant anomalies of sidero-chalcophile sulphide-graphite-bearing mica gneisses occur in the Tallinn and Alutaguse zones [Vaher et al., 1962]. Areas of prominent mineralization produce distinct magnetic anomalies, e. g. Haljala, Assa-malla, Uljaste, where the total concentration of Cu, Pb and Zn can be as high as 5.6 %. Graphite con-
centration in graphite gneisses is highly variable, reaching up to 10-15 %. Moreover, in the Palamuse drill core, a 1.6 m thick fine-grained layer contains up to 36 % of graphite. Together with iron sulphides, polymetallic mineralization is observable. Pyrrhotite is the most common sulphide mineral, spreading dispersedly in up to a few cm-thick layers in the gneissic texture, and often replaced by pyrite. Iron sulphides have later been cut by sphalerite, chalcopyrite and galena [Vaher et al., 1964; Puura et al., 1967, 1983; Petersell, 1976; Petersell et al., 1985, 1991]. The second stage is more common for brecciated rocks with apparent cracks and caverns [Vaher et al., 1964]. Graphite gneiss formations are ultimately metamorphosed in the conditions of am-phibolite facies metamorphism.
Tonis Oja is acknowledged for providing gravity data.
We acknowledge the funding from the RITA programme by the European Regional Development Fund, the work programme "Metallogenesis of the Johvi area".
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СВЕДЕНИЯ ОБ АВТОРАХ:
Соэсоо, Алвар
профессор
Отделение геологии Института экологии и наук о Земле
Тартуского университета
50411, Тарту, Эстония
эл. почта: alvar.soesoo@gmail.com
Нирги, Сиим
геолог
Геологическая служба Эстонии 44314, Раквере, Эстония
аспирант
Отделение геологии Института экологии и наук о Земле Тартуского университета 50411, Тарту, Эстония эл. почта: siim.nirgi@egt.ee
Пладо, Юри
старший научный сотрудник
Отделение геологии Института экологии и наук о Земле Тартуского университета 50411, Тарту, Эстония эл. почта: juri.plado@ut.ee
Väisänen M., MänttäriI., Hölttä P. Svecofennian magmatic and metamorphic evolution in southwestern Finland as revealed by U-Pb zircon SIMS geochronolo-gy. Precambrian Res. 2002. Vol. 116. P. 111-127.
Received January 30, 2020
CONTRIBUTORS:
Soesoo, Alvar
Institute of Ecology and Earth Sciences Department of Geology Ravila Street 14A, 50411, Tartu, Estonia e-mail: alvar.soesoo@gmail.com
Nirgi, Siim
Geological Survey of Estonia
FR. Kreutzwaldi 5, 44314, Rakvere, Estonia
Institute of Ecology and Earth Sciences Department of Geology Ravila Street 14A, 50411, Tartu, Estonia e-mail: siim.nirgi@egt.ee
Plado, Jüri
Institute of Ecology and Earth Sciences Department of Geology Ravila Street 14A, 50411, Tartu, Estonia e-mail: juri.plado@ut.ee
