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Temagami Greenstone Belt
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Temagami Greenstone Belt
The Temagami Greenstone Belt (TGB) is a small 2.7 billion year old greenstone belt in the Temagami region of Northeastern Ontario, Canada. It represents a feature of the Superior craton, an ancient and stable part of the Earth's lithosphere that forms the core of the North American continent and Canadian Shield. The belt is composed of metamorphosed volcanic rocks that range in composition from basalt to rhyolite. These form the east-northeast trend of the belt and are overlain by metamorphosed sedimentary rocks. They were created during several volcanic episodes involving a variety of eruptive styles ranging from passive lava eruptions to viscous explosive eruptions.
Part of the Canadian Shield, the TGB contains some of the oldest known rocks on Earth. The belt is made up of a number of geologic features such as batholiths, stocks, dikes, volcanic complexes, layered intrusions and deformation zones. These are situated in several geographical townships in the municipality of Temagami, including Chambers, Strathy, Strathcona, Briggs and possibly Best.
Geologists assume that greenstone belts were formed by many geological processes, such as tectonism, magmatism, metamorphism and sedimentation. They are important economically for large metal deposits, and for the insight they provide into crustal evolution and the tectonics of the early Earth. The TGB is 25 km (16 mi) wide and 32 km (20 mi) long. It contains the southernmost remnants of Archean intrusive and supracrustal rocks in Eastern Ontario, as well as some of the most ancient felsic magmatic events in this section of the Superior craton. Uranium-lead dating has established that the Iceland Lake Pluton, as well as an adjacent rhyolitic lava flow, is about 2,736 million years old. Therefore, at least some intrusions were likely formed during the first volcanic phases in the belt and may have been conduits for volcanic eruptions.
The variety of volcanic deposits and intrusions in the TGB indicates that magmatic activity played a significant part in its formation. Pillow lava is found throughout the belt, indicating lava erupted underwater. Its pyroclastic deposits are remnants of explosive volcanism. The oldest exposed rocks within the belt are fine to medium-grained basalts and andesites. Lava flow units range in thickness from 90 m (300 ft) to 1,500 m (4,900 ft). Mafic agglomerate and breccia are relatively abundant, being either massive and undeformed, or sheared. Dacitic lava flows or tuffs overlie these metamorphosed volcanic rocks along with intermediate volcanic breccias, and are overlain by rhyolite lava flows and tuffs. Acidic lava flow units range in thickness from 90 m (300 ft) to 900 m (3,000 ft) and are common in the Vermilion Lake and Link Lake areas. The felsic tuffs are normally altered and sheared. The most recent intrusive activity in the TGB was the formation of a rhyolite porphyry dike 2687 ± 2 million years ago. This age correlates well with the 2675–2700 million year old intrusions throughout the Abitibi Subprovince, but the 2736 million year old magmatic events in the TGB are older than the closest exposed portion of the Abitibi Subprovince, about 120 km (75 mi) north of Kirkland Lake.
Along with nearby granitic intrusions, the TGB is bounded by layers of rock comprising the Huronian Supergroup. Strathy Township is dominated by metamorphosed volcanic rocks of the northeastern portion of the belt. It is approximately 24 km (15 mi) north of the Grenville Front Tectonic Zone. The volcanic rocks possibly total as much as 6,000 m (20,000 ft) thick. However, portions of the sequence might have been repeatedly sheared by one or several local fault zones. Every large volcanic event is capped by metamorphosed sedimentary rocks and/or iron formations. The metamorphosed sedimentary units range in thickness from 60 m (200 ft) to 300 m (980 ft) and consist of laminated slate and greywacke with or without volcanogenic tuffs. The iron formations are composed of alternate layers of magnetite, white quartzite, jasper, grey cherty quartz, and/or tremolite-chlorite tuff. They are intruded by sills composed of medium-grained, white-weathering, quartz diorite that range in thickness from 100 m (330 ft) to 210 m (690 ft). These rocks are similar to the coarse thicker parts of lava flows, but are interpreted to be partly intrusive, likely conduits that produced mafic volcanism.
A layered intrusion composed of diorite, pyroxenite, gabbro and anorthositic gabbro has been found in northwestern Strathy Township. Pyrrhotite is common in associated pyroclastic rock. Several northeast-trending shear zones less than 5 m (16 ft) wide intersect the edifice, extending along the Net Lake-Vermilion Lake Deformation Zone. This layered intrusion might be similar in age to the Kanichee layered intrusive complex, and may represent a magma chamber that was the source of tholeiitic volcanic activity.
The Kanichee layered intrusive complex, also known as the Kanichee Intrusion and Ajax Intrusion, is the most voluminous mafic-ultramafic body in metamorphosed felsic and mafic volcanic rocks of the northern TGB. It is an oval-shaped layered intrusion that was formed during five phases of magmatic activity. A series of south-southeast dipping cyclic magmatic layers make up the intrusion, similar to those of the surrounding metamorphosed volcanic rocks, indicating that the rocks of the intrusion were formed horizontally and likely close to the surface. Numerous magmatic events may have breached the surface to produce volcanic eruptions. The overall structure of the intrusion indicates it is cylindrical in shape and has a long axis plunging to the southeast at a somewhat steep angle. Its fairly steep angled axis was formed by at least one period of deformation that similarly folded and deformed the surrounding volcanic rocks.
An intrusion of light-coloured diorite lies at the northern end of the Tetapaga Syncline, along the Milne-Sherman Road. Its colouration is from weathering of plagioclase, which comprises more than 50% of the intrusive rock. Several east-trending high-strain zones related to the Link Lake Deformation Zone, less than 1 m (3.3 ft) wide, are found in the intrusion, indicating that it formed at least before the last increment of strain along the Link Lake Deformation Zone. The dioritic intrusion might be the remains of a magma chamber that was the product of calc-alkaline feldspar-phyric felsic volcanism, the erupted products of which are mostly located in the Sherman Mine area.
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Temagami Greenstone Belt
The Temagami Greenstone Belt (TGB) is a small 2.7 billion year old greenstone belt in the Temagami region of Northeastern Ontario, Canada. It represents a feature of the Superior craton, an ancient and stable part of the Earth's lithosphere that forms the core of the North American continent and Canadian Shield. The belt is composed of metamorphosed volcanic rocks that range in composition from basalt to rhyolite. These form the east-northeast trend of the belt and are overlain by metamorphosed sedimentary rocks. They were created during several volcanic episodes involving a variety of eruptive styles ranging from passive lava eruptions to viscous explosive eruptions.
Part of the Canadian Shield, the TGB contains some of the oldest known rocks on Earth. The belt is made up of a number of geologic features such as batholiths, stocks, dikes, volcanic complexes, layered intrusions and deformation zones. These are situated in several geographical townships in the municipality of Temagami, including Chambers, Strathy, Strathcona, Briggs and possibly Best.
Geologists assume that greenstone belts were formed by many geological processes, such as tectonism, magmatism, metamorphism and sedimentation. They are important economically for large metal deposits, and for the insight they provide into crustal evolution and the tectonics of the early Earth. The TGB is 25 km (16 mi) wide and 32 km (20 mi) long. It contains the southernmost remnants of Archean intrusive and supracrustal rocks in Eastern Ontario, as well as some of the most ancient felsic magmatic events in this section of the Superior craton. Uranium-lead dating has established that the Iceland Lake Pluton, as well as an adjacent rhyolitic lava flow, is about 2,736 million years old. Therefore, at least some intrusions were likely formed during the first volcanic phases in the belt and may have been conduits for volcanic eruptions.
The variety of volcanic deposits and intrusions in the TGB indicates that magmatic activity played a significant part in its formation. Pillow lava is found throughout the belt, indicating lava erupted underwater. Its pyroclastic deposits are remnants of explosive volcanism. The oldest exposed rocks within the belt are fine to medium-grained basalts and andesites. Lava flow units range in thickness from 90 m (300 ft) to 1,500 m (4,900 ft). Mafic agglomerate and breccia are relatively abundant, being either massive and undeformed, or sheared. Dacitic lava flows or tuffs overlie these metamorphosed volcanic rocks along with intermediate volcanic breccias, and are overlain by rhyolite lava flows and tuffs. Acidic lava flow units range in thickness from 90 m (300 ft) to 900 m (3,000 ft) and are common in the Vermilion Lake and Link Lake areas. The felsic tuffs are normally altered and sheared. The most recent intrusive activity in the TGB was the formation of a rhyolite porphyry dike 2687 ± 2 million years ago. This age correlates well with the 2675–2700 million year old intrusions throughout the Abitibi Subprovince, but the 2736 million year old magmatic events in the TGB are older than the closest exposed portion of the Abitibi Subprovince, about 120 km (75 mi) north of Kirkland Lake.
Along with nearby granitic intrusions, the TGB is bounded by layers of rock comprising the Huronian Supergroup. Strathy Township is dominated by metamorphosed volcanic rocks of the northeastern portion of the belt. It is approximately 24 km (15 mi) north of the Grenville Front Tectonic Zone. The volcanic rocks possibly total as much as 6,000 m (20,000 ft) thick. However, portions of the sequence might have been repeatedly sheared by one or several local fault zones. Every large volcanic event is capped by metamorphosed sedimentary rocks and/or iron formations. The metamorphosed sedimentary units range in thickness from 60 m (200 ft) to 300 m (980 ft) and consist of laminated slate and greywacke with or without volcanogenic tuffs. The iron formations are composed of alternate layers of magnetite, white quartzite, jasper, grey cherty quartz, and/or tremolite-chlorite tuff. They are intruded by sills composed of medium-grained, white-weathering, quartz diorite that range in thickness from 100 m (330 ft) to 210 m (690 ft). These rocks are similar to the coarse thicker parts of lava flows, but are interpreted to be partly intrusive, likely conduits that produced mafic volcanism.
A layered intrusion composed of diorite, pyroxenite, gabbro and anorthositic gabbro has been found in northwestern Strathy Township. Pyrrhotite is common in associated pyroclastic rock. Several northeast-trending shear zones less than 5 m (16 ft) wide intersect the edifice, extending along the Net Lake-Vermilion Lake Deformation Zone. This layered intrusion might be similar in age to the Kanichee layered intrusive complex, and may represent a magma chamber that was the source of tholeiitic volcanic activity.
The Kanichee layered intrusive complex, also known as the Kanichee Intrusion and Ajax Intrusion, is the most voluminous mafic-ultramafic body in metamorphosed felsic and mafic volcanic rocks of the northern TGB. It is an oval-shaped layered intrusion that was formed during five phases of magmatic activity. A series of south-southeast dipping cyclic magmatic layers make up the intrusion, similar to those of the surrounding metamorphosed volcanic rocks, indicating that the rocks of the intrusion were formed horizontally and likely close to the surface. Numerous magmatic events may have breached the surface to produce volcanic eruptions. The overall structure of the intrusion indicates it is cylindrical in shape and has a long axis plunging to the southeast at a somewhat steep angle. Its fairly steep angled axis was formed by at least one period of deformation that similarly folded and deformed the surrounding volcanic rocks.
An intrusion of light-coloured diorite lies at the northern end of the Tetapaga Syncline, along the Milne-Sherman Road. Its colouration is from weathering of plagioclase, which comprises more than 50% of the intrusive rock. Several east-trending high-strain zones related to the Link Lake Deformation Zone, less than 1 m (3.3 ft) wide, are found in the intrusion, indicating that it formed at least before the last increment of strain along the Link Lake Deformation Zone. The dioritic intrusion might be the remains of a magma chamber that was the product of calc-alkaline feldspar-phyric felsic volcanism, the erupted products of which are mostly located in the Sherman Mine area.
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