Tectonic evolution, volcanic features and geochemistry of the Paleoproterozoic Salla belt, northern Fennoscandia: From 2.52–2.40 Ga LIP stages to ca. 1.92–1.90 Ga collision
Köykkä a, *, R. Lahtinen b, T. Manninen a
a Geological Survey of Finland, P.O. Box 77, FI-96101 Rovaniemi, Finland
b Geological Survey of Finland, P.O. Box 96, FI-02151 Espoo, Finland
* Corresponding author. E-mail address: juha.koykka@gtk.fi (J. Köykkä)
Text and figures extracted and modified from:
Köykkä, J., Lahtinen, R., Manninen, T. 2022. Tectonic evolution, volcanic features and geochemistry of the Paleoproterozoic Salla belt, northern Fennoscandia: From 2.52 to 2.40 Ga LIP stages to ca. 1.92–1.90 Ga collision. Precambrian Research 371, 106597. https://doi.org/10.1016/j.precamres.2022.106597
Introduction
The Fennoscandian Shield is the main component of the Fennoscandia crustal segment that forms the northern part of the (proto) Baltica or the East European Craton (Fig. 1a). It is composed of an Archean core in the NE and progressively younger Proterozoic crustal domains towards the SW. The East European Craton was formed between 2.0 and 1.7 Ga by the successive collision of Fennoscandia, Sarmatia and Volgo–Uralia crustal segments or blocks. The bedrock of northern Finland is mainly composed of 3.5–2.5 Ga Archean basement and 2.5–1.9 Ga Paleoproterozoic supracrustal cover, which mainly form the rim of the Central Lapland granitoid complex and several different Archean basement complexes (Fig. 1b). The main Paleoproterozoic orogenic evolution of Fennoscandia has been divided into the Lapland-Kola (1.94–1.86 Ga) and the composite Svecofennian (1.92–1.79 Ga) orogenies (see Lahtinen et al., 2018).
In the Fennoscandian Shield, 2.52–2.40 Ga LIP-related within-plate volcanic rocks were developed in the Kola and Karelian cratons in several major magmatic pulses and events (Fig. 1b). The main intrusion-related events were at 2.53, 2.50, 2.45, 2.40 Ga and 2.33–2.31 Ga (e.g., Stepanova et al., 2015; Huhma et al., 2018; Bayanova et al., 2019; Davey et al., 2020), which also correlates with the volcanic rocks shield-wide. Probably the best documented Early Paleoproterozoic shield-wide magmatic event took place in several cratons at ca. 2.45/2.44 Ga (Fig. 1c), which produced an LIP with both mafic and silicic intrusions, diabase dykes and coeval volcanic rocks (e.g. Vuollo and Huhma, 2005; Lauri et al., 2012; Bogina et al., 2018; Bayanova et al., 2019; Ernst et al., 2019). The final 2.40 Ga event in the Fennoscandian Shield mostly included dyke systems in Russian Karelia (Bayanova et al., 2019) and in northeastern Finland (Huhma et al., 2018). In NNE Finland, high-Mg magmas with a wide areal distribution could probably be considered as part of the dyke-related 2.43–2.42 Ga magmatism, which can be found in the Salla belt, NNE Finland (2424 ± 5 Ma, Huhma, et al., 2018).
Traditionally, volcanic and intrusive events in the Fennoscandian Shield can be divided into time intervals following the main Karelian time stratigraphic units and events: the Sumi (2505–2430 Ma), Sariola (2430–2300 Ma), Jatuli (2300–2060 Ma), Ludicovi (2060–1960 Ma) and Kaleva (1960–1900 Ma) systems (Hanski, 2013; Hanski and Melezhik, 2013). This paper focuses on the Sumi–Sariola volcanic systems and intrusive events between 2.52 and 2.40 Ga in the Paleoproterozoic Salla belt and its correlative volcanic units in the Kuusamo belt, in NNE Finland (i.e Salla and Kuusamo group volcanic rocks). This study also compares the Sumi–Sariola volcanic events between NNE Finland, Russian Karelia and the Kola Peninsula and proposes a tectonomagmatic scenario and locations at 2.51–2.40 Ga of Archean crustal blocks in Fennoscandia.
Fig 1. a) Simplified geological map of Fennoscandia. b) Archean crust covered by Proterozoic rocks in Fennoscandia. Black frame = study area. Dotted blue lines outline the least deformed main Archean blocks separated by Paleoproterozoic sutures and major rifts. The dotted red line outlines the CLGC. SB = Salla belt, KB = Kuusamo belt, CLB = Central Lapland belt, A = Akanvaara; B = Burakovka, J = Junttilanniemi, K = Koitelainen, Ke = Kemi, Ko = Koillismaa, M = Matinvaara, Pe = Penikat, T = Tsokkoaivi. c) Matachewan LIP reconstruction modified after Söderlund et al. (2010) and Ciborovski et al. (2015).
Volcanology and geochemistry
A total of 491 selected whole-rock analyses from the Salla and Kuusamo belts, five from the Kainuu belt (Finland) and 93 from Kola–Karelia (Russia) were used to determine and correlate the Sumi–Sariola volcanic systems and characteristics in the Salla belt area (see Table 1; Figs. 2a-d). In the Salla belt, the magmatism included at least two major events, which initiated at ca. 2.45–2.44 Ga and were followed at ca. 2.43–2.40 Ga, extending over an interval of ca. 300–400 Ma. Tectono-magmatic evolution shows enrichment in LILE elements, indicating a continental crustal contamination, in an intracratonic rift related setting, characterized by a well-preserved dynamic and multiphase stratigraphic architecture and volcanic processes with related successions.
In the Salla belt, the Salla group of the Sumi system mainly includes subaerial amygdaloidal intermediate lava flows, and acid lapilli tuffs and welded ash-flow tuffs, whereas the Kuusamo group of the Sariola system includes subaerial–subaqueous intermediate to ultrabasic magmatism that has volcanic structures related to continental flood basalts and/or pahoehoe tube-type lava flows. Both systems indicate, for instance, lava cooling, gas expansion and escape processes, and vapour differentiation processes and overall devolatilization of lava (Figs. 3a-h). Based on the calc-alkaline to tholeiitic affinity, it is possible that Sumi–Sariola volcanism in the Salla belt resulted from the content of the core-related fluids in the plume heads.
Table 1. Selected average and range variation of element ratios from volcanic rocks of the Salla and Kuusamo groups in SB and KB (major elements in %; trace elements in ppm). r. = range, a. = average, Mg# = [Mg/(Mg+Fe2] x 100; AC = acid, IM = intermediate, BA = basic, (U)BA = (ultra)basic; and = andesite, bas = basalt, band = basaltic andesite, dac = dacite, mg-bas = high-Mg basalt, rhy = rhyolite, (b)ta = (basaltic) trachy-andesite.
GeoUnit |
RockType |
SiO2 |
TiO2 |
Al2O3 |
Fe2O3 |
MnO |
MgO |
CaO |
Na2O |
K2O |
P2O5 |
Cr |
Mg# |
|
Salla gp (Sumi) |
||||||||||||||
Petservaara fm |
IM (band, and, (b)ta) |
r. |
51.3-69.7 |
0.53-1.34 |
11.3-16.1 |
7.66-16.45 |
0.02-0.28 |
0.95-10.5 |
0.38-11.4 |
1.13-6.49 |
0.07-9.25 |
0.1-0.39 |
17-542 |
21.24-27.92 |
n=209 |
a. |
58.21 |
0.88 |
13.66 |
10.68 |
0.16 |
4.14 |
5.32 |
3.87 |
1.98 |
0.18 |
91 |
24.58 |
|
AC (dac, rhy) |
r. |
60.2-77.1 |
0.57-1.24 |
10-14.2 |
2.52-13.37 |
0.01-0.21 |
0.09-5.11 |
0.17-5.85 |
0.73-5.8 |
0.47-6.35 |
0.12-0.41 |
13-104 |
5.3-14.1 |
|
n=112 |
a. |
67.15 |
0.82 |
12.11 |
8.29 |
0.09 |
1.28 |
2.65 |
3.02 |
3.44 |
0.23 |
33 |
10.98 |
|
Kuntivaara fm |
IM (band, (b)ta) |
r. |
53.3-61.7 |
0.5-1.48 |
13.6-16.2 |
6.69-12.2 |
0.06-5.33 |
0.16-7.42 |
0.65-7.26 |
3.66-5.75 |
0.3-4.92 |
0.06-0.36 |
51-273 |
1.32-42.53 |
n=12 |
a. |
56.18 |
0.74 |
14.61 |
8.78 |
0.99 |
4.44 |
3.75 |
4.58 |
2.26 |
0.14 |
131 |
29.15 |
|
AC (dac, rhy) |
r. |
63.5-70.9 |
0.37-1.33 |
10.9-15.7 |
2.14-8.64 |
0.02-1.52 |
0.03-1.81 |
0.64-4.3 |
1.01-5.51 |
2.68-7.5 |
0.13-0.28 |
13-25 |
1.09-18.11 |
|
n=7 |
a. |
67.54 |
0.87 |
13.90 |
4.62 |
0.56 |
0.58 |
1.80 |
3.54 |
4.41 |
0.21 |
19 |
8.21 |
|
Purkkivaara fm |
AC (dac, rhy) |
r. |
65.31-75.2 |
0.57-0.96 |
11.1-12.1 |
5.61-10.53 |
0.03-0.14 |
0.21-2.73 |
0.29-3.64 |
3.22-4.97 |
0.48-3.94 |
0.06-0.35 |
18-30 |
2.36-26.48 |
n=8 |
a. |
69.46 |
0.71 |
11.80 |
7.66 |
0.09 |
0.94 |
2.21 |
3.62 |
2.89 |
0.18 |
24 |
9.19 |
|
GeoUnit |
RockType |
SiO2 |
TiO2 |
Al2O3 |
Fe2O3 |
MnO |
MgO |
CaO |
Na2O |
K2O |
P2O5 |
Cr |
Mg# |
|
Kuusamo gp (Sariola) |
||||||||||||||
Kuntijärvi fm |
BA (mg-bas) |
r. |
47.5 |
0.41 |
9.29 |
10.56 |
0.18 |
15.7 |
8.08 |
0.73 |
0.86 |
0.06 |
1725 |
56.18-56.18 |
n=1 |
a. |
56.18 |
||||||||||||
IM (band) |
r. |
49.9-51.6 |
0.53-0.73 |
13-15.1 |
10.19-12.45 |
0.08-0.23 |
6.66-9.15 |
4.64-7.68 |
0.44-5.06 |
0.27-1.95 |
0.09-0.13 |
258-565 |
31.57-43.64 |
|
n=4 |
a. |
50.95 |
0.64 |
14.00 |
11.52 |
0.17 |
7.72 |
6.16 |
2.81 |
0.86 |
0.10 |
350 |
36.64 |
|
Mäntyvaara fm |
BA (mg-bas) |
r. |
44.5-51 |
0.3-0.64 |
7.15-19.3 |
9.71-12.4 |
0.15-0.2 |
5.49-23.6 |
3.96-9.74 |
0.01-4.12 |
0.01-2.04 |
0.04-0.14 |
162-3570 |
32.77-67.25 |
n=17 |
a. |
47.31 |
0.49 |
10.94 |
11.04 |
0.18 |
15.49 |
7.04 |
1.63 |
0.60 |
0.08 |
1843 |
53.40 |
|
IM (band, (b)ta) |
r. |
48.8-58.3 |
0.39-0.57 |
8.42-16.7 |
6.78-12.76 |
0.11-0.22 |
5.57-15.7 |
4.85-12.4 |
0.63-5.58 |
0.06-2.18 |
0.06-0.11 |
112-1950 |
34.51-60.42 |
|
n=45 |
a. |
53.90 |
0.48 |
12.54 |
8.97 |
0.16 |
9.46 |
8.51 |
2.96 |
0.69 |
0.09 |
547 |
47.10 |
|
Esikkovaara fm |
(U)BA (mg-bas) |
r. |
40.3-50.6 |
0.2-2.54 |
6.63-12.8 |
7.35-18.59 |
0.13-0.25 |
4.48-21.8 |
6.35-18.7 |
0.17-5.6 |
0.01-2.49 |
0.05-0.27 |
107-2750 |
17.2-62.55 |
n=22 |
a. |
46.29 |
0.66 |
8.86 |
12.07 |
0.18 |
15.41 |
8.41 |
1.88 |
0.48 |
0.09 |
1709 |
51.00 |
|
IM (band, (b)ta) |
r. |
50.54-59.8 |
0.35-1.68 |
8.14-14.7 |
6.68-12.63 |
0.08-0.28 |
2.76-12.3 |
5.09-12.9 |
3-6.16 |
0.1-1.96 |
0.1-0.49 |
24-1160 |
17.13-50.81 |
|
n=28 |
a. |
54.84 |
0.83 |
11.96 |
10.35 |
0.14 |
7.37 |
7.81 |
4.07 |
0.94 |
0.15 |
442 |
37.53 |
|
Matsokkaselkä fm |
BA (mg-bas) |
r. |
45.2-47.7 |
0.31-0.54 |
6.47-10.7 |
10.24-10.85 |
0.16-0.18 |
14-21.7 |
7.79-8.27 |
0.76-1.46 |
0.02-0.69 |
0.05-0.09 |
1240-2690 |
53.7-63.29 |
n=45 |
a. |
46.53 |
0.46 |
8.96 |
10.52 |
0.17 |
17.13 |
8.03 |
1.04 |
0.36 |
0.08 |
1940 |
58.03 |
|
IM (band) |
r. |
51-56.7 |
0.58-0.87 |
9.79-14.8 |
8.27-10.88 |
0.13-0.18 |
4.84-9.78 |
7.32-10.1 |
2.25-4.87 |
0.05-1.45 |
0.1-0.15 |
80-790 |
29.22-45.27 |
|
n=19 |
a. |
53.73 |
0.70 |
12.84 |
9.70 |
0.16 |
6.75 |
8.53 |
3.20 |
0.90 |
0.13 |
390 |
37.11 |
|
Kuusijärvi fm |
BA (mg-bas) |
r. |
49.3-51.2 |
0.68-2 |
12.9-13.9 |
10.07-13 |
0.03-0.2 |
7.01-10.7 |
5.25-8.84 |
3.38-4.42 |
0.3-3.25 |
0.1-0.1 |
155-209 |
31.74-47.82 |
n=2 |
a. |
50.25 |
1.34 |
13.40 |
11.54 |
0.11 |
8.86 |
7.05 |
3.90 |
1.77 |
0.10 |
182 |
39.78 |
|
IM (band) |
r. |
51.6 |
1.93 |
12.8 |
15 |
0.24 |
4.17 |
6.75 |
2.88 |
0.95 |
0.26 |
66 |
19.33-19.33 |
|
n=1 |
a. |
19.33 |
Fig. 2. Total alkali vs. SiO2 plot (TAS) and mantle-primitive-normalized spider diagrams for the Salla (a,b) and Kuusamo groups (c,d). Dashed lines = main clustering. Spider diagrams (b,d) based on average values for each unit rock type. Upper Continental Crust (UCC), Middle Continental Crust (MCC) and Lower Continental Crust (LCC). For references see Köykkä et al., 2022.
Fig. 3. Photographs of outcrops from the Salla belt Sumi system (Salla group = a-d) and Sariola system (Kuusamo group = e-h). Salla group – Sumi system: a) A small pipe vesicles (keys = 6 cm). b) Elongated flow stretched vesicles (scale = 15 cm). c) Pumice fragments floating in a fine-grained tuff matrix. g) Roundish to elongated lithophysae (originally vapour cavities), the size varying from 1–2 cm up to 20–35 cm. Kuusamo group – Sariola system: e) Hyaloclastic material in a basaltic lava flow. f) A mattress-shaped pillow in basaltic lava flow with hyalotuff interbeds. e) A grooved feature in the top of the lava flow representing a ropy lava structure. h) Columnar jointing in a basaltic lava flow.
Tectonic evolution and shield-wide correlations at 2.52–2.40 Ga
According to this study, the tectonic setting of different rock units at 2.52–2.40 Ga in Fennoscandia follows a framework for the plumbing system of continental large igneous provinces (LIPs) associated with mantle plumes (Ernst et al., 2019). This study also combines the LIP record from the dykes and layered intrusions and propose a new model where the 2.45–2.44 Ga represents the plume arrival, and both radiating swarm and the circumferential stages. In this model the 2.43–2.40 Ga more primitive magmatic stage indicates a final gravitational collapse of the LIP mantle plume and intrusion in and through the pre-existing structures formed mainly during the 2.45–2.44 Ga LIP stage. An occurrence of a new plume head at 2.40 Ga is also possible as proposed by Davey et al. (2020). In Fig. 4 the least extended and shortened main Archean blocks in Fennoscandia are based on the existence of preserved Paleoproterozoic 2.51–2.40 Ga basins with a rift axis and approximately similar-aged dykes having coherent trends.
Based on new structural observations and geochemistry, this study adapts the Large Igneous Province (LIP) and mantle plume model for the 2.51–2.49 Ga and 2.45–2.44 Ga magmatic stages in the northern Fennoscandian Shield, where the former corresponds to the Mistassini LIP and the latter correlates with the Matachewan LIP (Ernst and Bleeker, 2010; Kulikov et al., 2010). This study also supports model of the break-up of Archean Fennoscandia into the Kola, Norrbotten, Pudasjärvi and Karelia blocks at 2.15–1.98 Ga with later reassembly at 1.92–1.90 Ga during the Svecofennian and Lapland–Kola orogenies (Fig. 4a).
Table 2 summarizes the shield-wide correlations at 2.51–2.40 Ga. Mantle plume location A in Fig. 4b would make the Fedorovo-Pansky intrusion (F) an intrusion ringing the plume centre, with Tshokkoaivi an intrusion along the dyke (T), and the Liinakhamari dykes forming radiating dykes (Li). Mantle plume location B in Fig 4.b is based on the paleomagnetic pole of the 2.51 Ga Shalskiy dykes. Model B would imply that the Fedorovo-Pansky intrusion is an intrusion along the dyke, the Liinakhamari dykes are circumferential dykes, and the granites are circumferential granites. Kola and Karelia show similar paleomagnetic poles at ca 2.45 Ga, indicating that they have been on the same latitude and probably attached together at that time (Salminen et al., 2021 and references therein). The ca. 2.45–2.43 Ga layered intrusions (e.g. Huhma et al., 2018; Bayanova et al., 2019) and granites (e.g. Lauri et al., 2012) form intrusions ringing the plume center (Fig. 4b). This would favor the occurrence of a LIP, as proposed earlier (Ernst and Bleeker, 2010), and indicate that the plume centre has been close to the present NNW part of Fennoscandia. In model presented this paper, the WNW-trending and SW-trending 2.40 Ga dykes have intruded in the 2.45–2.43 Ga circumferential crustal weak zones (Fig. 4b). There is an also change from basaltic andesite–andesite-dominated Sumi volcanism to more primitive, partly komatiitic Sariola basalts at 2.43–2.40 Ga. Based on the age of 2424 ± 5 Ma from the Lehtomaa dyke, considered comagmatic with the Kuusamo group basalts, the 2412 ± 17 Ma age of Sariola basalt in Lehkta (Myskova et al., 2012), and 2407 ± 6 Ma (Puchtel et al., 2016) and 2405 ± 5 Ma (Mezhelovskaya et al., 2016) ages from the Vetreny belt (see Table 2), we consider that volcanism was active at least from 2.42 to 2.40 Ga. The 2.40 Ga dykes in the Fennoscandian Shield could be considered as the aftermath of this event (see Table 2).
In overall, the emplacement of the 2.42–2.40 Ga rocks follows the pre-existing structures formed during the 2.45–2.44 Ga LIP stage (Fig. 4b). The giant radiating dyke swarms were generated during domal uplift above a mantle plume. The subsidence and associated quicker transport of mantle melts could indicate that this stage is a final gravitational collapse stage of the 2.45–2.44 Ga mantle plume, or the significant subsidence might be due to a new plume head temporarily ponding below the 660-km phase-change boundary. The change in magmatism to a more primitive nature could be due to material coming from the hotter interior of the plume head or plume tail, or the rise of a new plume. The basin subsidence and the rapid uplift of rift margins indicates dynamic interaction of lithospheric and surface processes due to plume-lithosphere interactions, which can be seen as distinct geological record and stratigraphic patterns (see Friedrich et al., 2018; Buchan and Ernst, 2021). This can explain the extensive erosional period between the deposition of the Sumi and Sariola system rocks, as well as the exhumation of the 2.44 Ga layered intrusions.
Fig. 4. a) A sketch of the least deformed Archean blocks in Fennoscandia. Note that areas between the outlined Archean blocks include both Archean and Paleoproterozoic rocks in zones that exemplify both break-up and collisional processes. The rotation of the Pudasjärvi block is from Davey et al. (2020) and other rotations are by the authors. Swarm trend terminology from Ernst et al. (2019). b) Stars A and B are alternative models for 2.51-2.49 Ga plume centre (see text). Supracrustal belts: Ve = Vetreny; Le = Lehkta; Sh = Shombozero; Ku = Kuusamo; Pa = Paanajärvi; Ko = Kukasozero; Sa = Salla; V = Vuotso; Pe = Pechenga; IV = Imandra–Vardzuga. Intrusions and dykes: B = Burakovka, J = Junttilanniemi; Nä = Näränkävaara, TK = Tornio–Kukkola; Ke = Kemi; O = Oulanga, A = Akanvaara; K = Koitelainen; T = Tsokkoaivi, Tr = Troms, So = Sorvaranger; Li = Liinakhamari, Mt = Mt. Generalskaya, M = Monchegorsk/ Monchetundra, F = Fedorovo-Pansky, I = Imandra. b) Sketch of Fennoscandia at 2.51–2.49 Ga, 2.45-2.44 Ga (Sumi) and 2.43-2.40 Ga (Sariola). S = Shalskiy, J-To = Junttilanniemi–Topozersky, Ke-O = Kemi–Oulanga, On = Onkamonlehto.
Table 2. Summary of the U-Pb, Sm-Nd and Re-Os geochronological data. All ages in Ma. epsNd(T) value is based on U-Pb zircon dating, except for Salla gp / Petservaara fm (geological correlations). See references from Köykkä et al, 2022 App. CLB = Central Lapland belt, SB = Salla belt and KB = Kuusamo
Geological unit |
Lithology |
Area |
U-Pb age |
Sm-Nd age |
epsNd(T) |
TDM |
Re-Os age |
Ref. |
SUMI SYSTEM LIP MAGMATISM 2.51-2.49 Ga |
||||||||
Ahvenselkä suite |
granite (porphyritic) |
FI / CLB |
2524 ± 8 |
-1.9 |
2809 |
12, 15, 18 |
||
Pomokaira complex |
felsic gneiss |
FI / CLB |
2506 ± 6 |
-1.0 |
2895 |
13, 15, 26 |
||
Pomokaira complex |
gneiss (quartz-feldspar) |
FI / CLB |
2501 ± 5 |
12, 15, 18 |
||||
Salla gp / Rookkiaapa fm |
felsic volcanic breccia |
FI / CLB |
2505 ± 5 |
-3.2 |
2930 |
13, 17 |
||
Silisjoki suite |
granodiorite |
FI / CLB |
2504 ± 10 |
13, 15, 18 |
||||
Tshokkoaivi intrusion |
gabbro |
FI / CLB |
2499 ± 11 |
-1.8 |
2458 |
13 |
||
Varttasaari suite |
tonalite |
FI / CLB |
2520 ± 9 |
-1.4 |
2814 |
12, 15, 18 |
||
Vuotso complex |
gneiss (arkosic) |
FI / CLB |
2509 ± 8 |
12, 15 |
||||
Fedorovo-Pansky massif |
orthopyroxenite |
RU |
2526 ± 6 |
2521 ± 42 |
-1.7 |
7, 27, 29 |
||
Fedorovo-Pansky massif |
olivine gabbro |
RU |
2516 ± 7 |
2516 ± 35 |
-1.4 |
7, 27, 29 |
||
Fedorovo-Pansky massif |
magnetite gabbro |
RU |
2498 ± 5; 2500 ± 10 |
3, 7, 25 |
||||
Fedorovo-Pansky massif |
gabbronorite |
RU |
2491 ± 1.5; 2501 ± 1.7; 2500 ± 3 |
2487 ± 51 |
-2.1 |
1, 2, 7, 21 |
||
Liinahamari dyke |
qtz dolerite |
RU |
2508 ± 6 |
30 |
||||
Monchetundra |
plagiopyroxenite |
RU |
2502 ± 5.9 |
7, 25 |
||||
Monchetundra |
gabbronorite |
RU |
2504 ± 7.4 |
7, 25 |
||||
Monchetundra |
gabbronorite |
RU |
2501 ± 8; 2505 ± 6 |
3, 7 |
||||
Mt. Generalskaya |
gabbronorite |
RU |
2496 ± 10; 2505 ± 1.6 |
2453 ± 42 |
1, 5, 7 |
|||
Mt. Generalskaya |
Dunite block, dike |
RU |
2505 ± 1.7 |
7, 22 |
||||
Mt. Generalskaya |
Mt. Travyanaya, norite |
RU |
2507 ± 9 |
6, 7 |
||||
Mt. Generalskaya |
Dunite block, gabbronorite dike |
RU |
2506 ± 10; 2496 ± 14 |
6, 7 |
||||
Mt. Generalskaya |
Nyud Terrace, gabbronorite |
RU |
2500 ± 5 |
4, 7 |
||||
Mt. Generalskaya |
Nyud Terrace, gabbronorite |
RU |
2493 ± 7; 2504 ± 1.5 |
2492 ± 31 |
-1.4 |
1, 5, 7, 31 |
||
Mt. Generalskaya |
Nyud Terrace, gabbronorite |
RU |
2503.5 ± 4.6 |
7, 21 |
||||
Mt. Generalskaya |
Monchepluton, gabbronorite |
RU |
2498.2 ± 6.7 |
7, 21 |
||||
Mt. Generalskaya |
Vurechuaivench foothills, gabbronorite |
RU |
2497 ± 21; 2498 ± 6.7 |
6, 7 |
||||
Mt. Generalskaya |
Olenegorsk deposit, qtz diorite |
RU |
2495 ± 13 |
6, 7 |
||||
Shalskiy dyke |
gabbronorite |
RU |
2608 ± 56 |
-1.2 |
19 |
|||
Geological unit |
Lithology |
Area |
U-Pb age |
Sm-Nd age |
epsNd(T) |
TDM |
Re-Os age |
Ref. |
SUMI SYSTEM LIP MAGMATISM 2.45-2.44 Ga |
||||||||
Akanvaara intrusion |
gabbro |
FI / CLB |
2436 ± 6 |
13, 23 |
||||
Koitelainen intrusion |
granophyre |
FI / CLB |
2434 ± 5 |
13 |
||||
Salla gp / Rookkiaapa fm |
felsic volcanite |
FI / CLB |
2438 ± 11 |
-8.1 |
3520 |
13 |
||
Salla gp / Petservaara fm |
felsic tuff |
FI / SB |
2438 ± 49 |
-4.4 |
3101 |
11 |
||
Salla gp / Petservaara fm |
felsic tuff |
FI / SB |
2432 ± 26 |
-3.1 |
2944 |
11 |
||
Salla gp / Purkkivaara fm |
rhyolite |
FI / SB |
2441 ± 2 |
-2.3 |
2843 |
13 |
||
Imandra–Varzuga / Seidorechka |
rhyodacite |
RU |
2448 ± 8 |
-2.8 |
2864 |
8 |
||
Shombozero |
andesite |
RU |
2439 ± 21 |
-3.8 |
24 |
|||
Geological unit |
Lithology |
Area |
U-Pb age |
Sm-Nd age |
epsNd(T) |
TDM |
Re-Os age |
Ref. |
SARIOLA SYSTEM MAGMATISM 2.42-2.40 Ga |
||||||||
Uolevinlehto dyke |
gabbro |
FI |
2400 ± 12 |
9 |
||||
Kuusamo gp / Kuntijärvi fm |
felsic cgl clast |
FI / KB |
2428 ± 3 |
-2.8 |
13 |
|||
Kuusamo gp / Mäntyvaara fm |
komatiitic basalt |
FI / SB |
-2.4 |
13 |
||||
Lehtomaa dyke |
gabbro |
FI / SB |
2424 ± 5 |
-3.4 |
13, 16 |
|||
Onkamolehto dyke |
diabase |
FI / SB |
2403 ± 3 |
-0.7 |
13 |
|||
Troms |
gabbronorite |
NO |
2403 ± 3 |
-1.5, -1.8 |
10, 14 |
|||
Lehkta |
andesite |
RU |
2412 ± 17 |
-3.4 |
3102 |
24 |
||
Vetreny belt |
komatiitic basalt |
RU |
2407 ± 6 |
10, 28 |
||||
Vetreny belt |
komatiitic basalt |
RU |
2405 ± 5 |
20 |
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