Mesoarchean kola-karelia continent
The Mesoarchean Kola-Karelia continent in the eastern Fennoscandian Shield includes three tectonic provinces, Kola, Karelia and Belomoria, that were formed by the Paleoarchean and Mesoarchean microcontinents. Traces of Mesoarchean tonalite-trondhjemite-granodiorite (TTG)-type early crust were docume...
Main Authors: | , , , , , , , |
---|---|
Format: | Article in Journal/Newspaper |
Language: | English |
Published: |
Geological Society of America
2020
|
Subjects: | |
Online Access: | https://openrepository.ru/article?id=255420 |
id |
ftneicon:oai:rour.neicon.ru:rour/255420 |
---|---|
record_format |
openpolar |
institution |
Open Polar |
collection |
NORA (National aggregator of open repositories of Russian universities) |
op_collection_id |
ftneicon |
language |
English |
topic |
Europium Feldspar Glass Granite Hydraulic structures Levees Metamorphic rocks Silicate minerals Structural geology Tectonics Fennoscandian Shields Greenstone belts High pressure metamorphism High temperature Ophiolite complex Slow-spreading ridges Southwest Indian Ridge Tectonic settings Gallium |
spellingShingle |
Europium Feldspar Glass Granite Hydraulic structures Levees Metamorphic rocks Silicate minerals Structural geology Tectonics Fennoscandian Shields Greenstone belts High pressure metamorphism High temperature Ophiolite complex Slow-spreading ridges Southwest Indian Ridge Tectonic settings Gallium Mints M.V. Dokukina K.A. Konilov A.N. Kaulina T.V. Belousova E.A. Dokukin P.A. Natapov L.M. Van K.V. Mesoarchean kola-karelia continent |
topic_facet |
Europium Feldspar Glass Granite Hydraulic structures Levees Metamorphic rocks Silicate minerals Structural geology Tectonics Fennoscandian Shields Greenstone belts High pressure metamorphism High temperature Ophiolite complex Slow-spreading ridges Southwest Indian Ridge Tectonic settings Gallium |
description |
The Mesoarchean Kola-Karelia continent in the eastern Fennoscandian Shield includes three tectonic provinces, Kola, Karelia and Belomoria, that were formed by the Paleoarchean and Mesoarchean microcontinents. Traces of Mesoarchean tonalite-trondhjemite-granodiorite (TTG)-type early crust were documented in all of the most ancient units of the Kola-Karelia continent. Ancient crust was revealed and dated in the Ranua and Iisalmi microcontinents, 3.5-3.4 Ga; Vodlozero and Khetolambina microcontinents, 3.25-3.15 Ga; Kuhmo-Segozero microcontinent, 3.0 Ga; Murmansk and Inari-Kola microcontinents, 2.93 Ga; and Kianta microcontinent, 2.83-2.81 Ga. In the older (>3.0 Ga) tectonic units and microcontinents, the ancient crust was possibly formed in brief bursts of endogenic activity. In younger microcontinents (3.0-2.93 Ga), these processes could continue until 2.8 and even 2.72 Ga. The tectonic settings in which early TTG crust has been produced are largely uncertain. The primary melt glassy inclusions with a glass phase in cores of prismatic zircon crystals from TTG gneisses provide evidence for the volcanic origin of gneiss protolith. Suggested genetic modeling of TTG-type complexes assumes that felsic K-Na melts with positive Eu anomaly are a product of dry high-temperature partial melting of the previously formed mafic-to-felsic crustal rocks and/or thick older TTG crust. Positive Eu anomaly in the eutectic is directly related to the predominance of plagioclase and K-feldspar in the melt. TTG-type crust melted to produce granitegranodiorite (GG) rocks. Earliest microcontinents are separated by Mesoarchean greenstone belts (mainly 3.05-2.85 Ga, in some cases up to 2.75 Ga), which are fragments of paleo-islandarc systems accreted to their margins: the Kolmozero-Voronya, Central Belomorian, Vedlozero-Segozero, Sumozero-Kenozero, and Tipasjärvi-Kuhmo-Suomussalmi belts; and the mature island arcs (microcontinents): Khetolambina and Kovdozero. These structural units are characterized by significant extent, close to rectilinear trend, localization along the boundaries between Archean microcontinents, and a specific set of petrotectonic assemblages (basalt-andesite-rhyolite, komatiite-tholeiite, and andesite-dacite associations). The recently discovered Meso-Neoarchean Belomorian eclogite province that is structurally linked with the Central Belomorian greenstone belt contains two eclogite associations distributed within TTG gneisses: the subduction-type Salma association and the Gridino eclogitized mafic dikes. The protolith of the Salma eclogites is thought to have been a sequence of gabbro, Fe-Ti gabbro, and troctolite, formed at ca. 2.9 Ga in a slow-spreading ridge (similar to the Southwest Indian Ridge). The main subduction and eclogite-facies events occurred between ca. 2.87 and ca. 2.82 Ga. Mafic magma injections into the crust of the active margin that led to formation of the Grigino dike swarm were associated with emplacement of a mid-ocean ridge in a subduction zone, beginning at ca. 2.87 Ga. Crustal delamination of the active margin and subsequent involvement of the lower crust in subduction 2.87-2.82 Ga ago led to high-pressure metamorphism of the Gridino dikes that reached eclogite-facies conditions during a collision event between 2.82 and 2.78 Ga. This collision resulted in consolidation of the Karelia, Kola, and Khetolamba blocks and formation of the Mesoarchean Belomorian accretionary-collisional orogen. To date, the subductionrelated Salma eclogites provide the most complete and meaningful information on the nature of plate tectonics in the Archean, from ocean-fl oor spreading to subduction and collision. The Kovdozero granite-greenstone terrain that separates the Khetolambina and Kuhmo-Segozero microcontinents is formed by TTG granitoids and gneisses hosting metasediments and metavolcanics of several greenstone belts, which belonged to the Parandovo-Tiksheozero island arc that existed from ca. 2.81 to 2.77 Ga. The Iringora greenstone belt includes the ophiolite complex of the same name with an age of 2.78 Ga. The collision of microcontinents resulted in the upward squeezing of the island arc and the obduction of its marginal portions onto surrounding structures. © 2015 The Geological Society of America. All rights reserved. |
format |
Article in Journal/Newspaper |
author |
Mints M.V. Dokukina K.A. Konilov A.N. Kaulina T.V. Belousova E.A. Dokukin P.A. Natapov L.M. Van K.V. |
author_facet |
Mints M.V. Dokukina K.A. Konilov A.N. Kaulina T.V. Belousova E.A. Dokukin P.A. Natapov L.M. Van K.V. |
author_sort |
Mints M.V. |
title |
Mesoarchean kola-karelia continent |
title_short |
Mesoarchean kola-karelia continent |
title_full |
Mesoarchean kola-karelia continent |
title_fullStr |
Mesoarchean kola-karelia continent |
title_full_unstemmed |
Mesoarchean kola-karelia continent |
title_sort |
mesoarchean kola-karelia continent |
publisher |
Geological Society of America |
publishDate |
2020 |
url |
https://openrepository.ru/article?id=255420 |
long_lat |
ENVELOPE(34.675,34.675,65.923,65.923) ENVELOPE(27.029,27.029,68.906,68.906) ENVELOPE(33.279,33.279,66.358,66.358) ENVELOPE(31.560,31.560,66.761,66.761) ENVELOPE(27.000,27.000,65.767,65.767) ENVELOPE(32.133,32.133,65.817,65.817) ENVELOPE(35.150,35.150,63.933,63.933) |
geographic |
Gridino Inari Indian Khetolambina Kovdozero Murmansk Ranua Salma Sumozero |
geographic_facet |
Gridino Inari Indian Khetolambina Kovdozero Murmansk Ranua Salma Sumozero |
genre |
Fennoscandian |
genre_facet |
Fennoscandian |
op_source |
Special Paper of the Geological Society of America |
op_relation |
https://doi.org/10.1130/2015.2510(02) https://openrepository.ru/article?id=255420 |
op_rights |
open access |
op_doi |
https://doi.org/10.1130/2015.2510(02 |
_version_ |
1765998769055203328 |
spelling |
ftneicon:oai:rour.neicon.ru:rour/255420 2023-05-15T16:13:10+02:00 Mesoarchean kola-karelia continent Mints M.V. Dokukina K.A. Konilov A.N. Kaulina T.V. Belousova E.A. Dokukin P.A. Natapov L.M. Van K.V. 2020-03-03T14:40:19Z https://openrepository.ru/article?id=255420 EN eng Geological Society of America https://doi.org/10.1130/2015.2510(02) https://openrepository.ru/article?id=255420 open access Special Paper of the Geological Society of America Europium Feldspar Glass Granite Hydraulic structures Levees Metamorphic rocks Silicate minerals Structural geology Tectonics Fennoscandian Shields Greenstone belts High pressure metamorphism High temperature Ophiolite complex Slow-spreading ridges Southwest Indian Ridge Tectonic settings Gallium Article 2020 ftneicon https://doi.org/10.1130/2015.2510(02 2020-07-21T12:21:22Z The Mesoarchean Kola-Karelia continent in the eastern Fennoscandian Shield includes three tectonic provinces, Kola, Karelia and Belomoria, that were formed by the Paleoarchean and Mesoarchean microcontinents. Traces of Mesoarchean tonalite-trondhjemite-granodiorite (TTG)-type early crust were documented in all of the most ancient units of the Kola-Karelia continent. Ancient crust was revealed and dated in the Ranua and Iisalmi microcontinents, 3.5-3.4 Ga; Vodlozero and Khetolambina microcontinents, 3.25-3.15 Ga; Kuhmo-Segozero microcontinent, 3.0 Ga; Murmansk and Inari-Kola microcontinents, 2.93 Ga; and Kianta microcontinent, 2.83-2.81 Ga. In the older (>3.0 Ga) tectonic units and microcontinents, the ancient crust was possibly formed in brief bursts of endogenic activity. In younger microcontinents (3.0-2.93 Ga), these processes could continue until 2.8 and even 2.72 Ga. The tectonic settings in which early TTG crust has been produced are largely uncertain. The primary melt glassy inclusions with a glass phase in cores of prismatic zircon crystals from TTG gneisses provide evidence for the volcanic origin of gneiss protolith. Suggested genetic modeling of TTG-type complexes assumes that felsic K-Na melts with positive Eu anomaly are a product of dry high-temperature partial melting of the previously formed mafic-to-felsic crustal rocks and/or thick older TTG crust. Positive Eu anomaly in the eutectic is directly related to the predominance of plagioclase and K-feldspar in the melt. TTG-type crust melted to produce granitegranodiorite (GG) rocks. Earliest microcontinents are separated by Mesoarchean greenstone belts (mainly 3.05-2.85 Ga, in some cases up to 2.75 Ga), which are fragments of paleo-islandarc systems accreted to their margins: the Kolmozero-Voronya, Central Belomorian, Vedlozero-Segozero, Sumozero-Kenozero, and Tipasjärvi-Kuhmo-Suomussalmi belts; and the mature island arcs (microcontinents): Khetolambina and Kovdozero. These structural units are characterized by significant extent, close to rectilinear trend, localization along the boundaries between Archean microcontinents, and a specific set of petrotectonic assemblages (basalt-andesite-rhyolite, komatiite-tholeiite, and andesite-dacite associations). The recently discovered Meso-Neoarchean Belomorian eclogite province that is structurally linked with the Central Belomorian greenstone belt contains two eclogite associations distributed within TTG gneisses: the subduction-type Salma association and the Gridino eclogitized mafic dikes. The protolith of the Salma eclogites is thought to have been a sequence of gabbro, Fe-Ti gabbro, and troctolite, formed at ca. 2.9 Ga in a slow-spreading ridge (similar to the Southwest Indian Ridge). The main subduction and eclogite-facies events occurred between ca. 2.87 and ca. 2.82 Ga. Mafic magma injections into the crust of the active margin that led to formation of the Grigino dike swarm were associated with emplacement of a mid-ocean ridge in a subduction zone, beginning at ca. 2.87 Ga. Crustal delamination of the active margin and subsequent involvement of the lower crust in subduction 2.87-2.82 Ga ago led to high-pressure metamorphism of the Gridino dikes that reached eclogite-facies conditions during a collision event between 2.82 and 2.78 Ga. This collision resulted in consolidation of the Karelia, Kola, and Khetolamba blocks and formation of the Mesoarchean Belomorian accretionary-collisional orogen. To date, the subductionrelated Salma eclogites provide the most complete and meaningful information on the nature of plate tectonics in the Archean, from ocean-fl oor spreading to subduction and collision. The Kovdozero granite-greenstone terrain that separates the Khetolambina and Kuhmo-Segozero microcontinents is formed by TTG granitoids and gneisses hosting metasediments and metavolcanics of several greenstone belts, which belonged to the Parandovo-Tiksheozero island arc that existed from ca. 2.81 to 2.77 Ga. The Iringora greenstone belt includes the ophiolite complex of the same name with an age of 2.78 Ga. The collision of microcontinents resulted in the upward squeezing of the island arc and the obduction of its marginal portions onto surrounding structures. © 2015 The Geological Society of America. All rights reserved. Article in Journal/Newspaper Fennoscandian NORA (National aggregator of open repositories of Russian universities) Gridino ENVELOPE(34.675,34.675,65.923,65.923) Inari ENVELOPE(27.029,27.029,68.906,68.906) Indian Khetolambina ENVELOPE(33.279,33.279,66.358,66.358) Kovdozero ENVELOPE(31.560,31.560,66.761,66.761) Murmansk Ranua ENVELOPE(27.000,27.000,65.767,65.767) Salma ENVELOPE(32.133,32.133,65.817,65.817) Sumozero ENVELOPE(35.150,35.150,63.933,63.933) |