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{{short description|Geological complex of ancient rocks in Western Australia}}
⚫ {{Infobox Rockunit
{{Use Australian English|date=May 2024}}
{{no footnotes|date=August 2018}}
⚫ {{Infobox rockunit
| name = Narryer Gneiss Terrane | name = Narryer Gneiss Terrane
| image = Jack hills etm 1999208.jpg | image = Jack Hills, Western Australia (Landsat 5 TM, 2009-07-14, detail).jpg
| caption = Satellite image of ] in the Narryer Gneiss Terrane | caption = Satellite image of ] in the Narryer Gneiss Terrane
| type = Geological complex | type = Geological complex
| prilithology = ] | prilithology = ]
| otherlithology = | otherlithology =
| namedfor = | namedfor =
| namedby = | namedby =
| region = ] | region = ]
| country = ] | country = ], ]
| coordinates = | coordinates =
| unitof = | unitof =
| subunits = Dugel Gneiss, Meeberrie Gneiss, Manfred Complex & metasedimentary rocks | subunits = Dugel Gneiss, Meeberrie Gneiss, Manfred Complex and metasedimentary rocks
| thickness = | thickness =
| extent = | extent =
| area = | area =
| age = > 3.3 Ga}} | age = ]<br> >3.3 Ga
| period = Archean
}}


The '''Narryer Gneiss Terrane''' is a geological complex in ] that is composed of a tectonically interleaved and polydeformed mixture of ], mafic intrusions and metasedimentary rocks in excess of 3.3 Ga, with the majority of the Narryer Gneiss Terrane in excess of 3.6 Ga. The rocks have experienced multiple metamorphic events at amphibolite or granulite conditions, resulting in often complete destruction of original igneous or sedimentary (protolith) textures. Importantly, it contains the oldest known samples of the earths ]: Samples of ] from the ] portion of the Narryer Gneiss have been ] dated at 4.4 Ga, although the majority of zircon crystals are about 3.6-3.8 Ga. The '''Narryer Gneiss terrane''' is a geological complex in ] that is composed of a tectonically interleaved and polydeformed mixture of ], ] ]s and ]ary ]s in excess of 3.3 billion years old, with the majority of the Narryer Gneiss terrane in excess of 3.6 billion years old. The rocks have experienced multiple metamorphic events at ] or ] conditions, resulting in often complete destruction of original ] or ] (]) ]. Importantly, it contains the oldest known samples of the ]'s ]: samples of ] from the ] portion of the Narryer Gneiss have been ] dated at 4.4 billion years old, although the majority of zircon ]s are about 3.6-3.8 billion years old.


The Narryer Gneiss Terrane is adjacent to the northernmost margin of the Yilgarn Craton and is abutted on the north by the ] metasedimentary and metagranite orogen. The Narryer Gneiss Terrane also includes parts of the Yarlarweelor Gneiss which abuts to Nabberu Basin metamorphic sequences of the Bryah-Padbury Basins, where it is present as discontinuous slivers of metamorphic rocks, pelites, metaconglomerates and gneisses caught up within regional strike-slip oblique ]s. The Narryer Gneiss terrane is adjacent to the northernmost margin of the ] and is abutted on the north by the ] metasedimentary and ] ]. The Narryer Gneiss terrane also includes parts of the ] which abuts to ] metamorphic sequences of the ], where it is present as discontinuous slivers of ]s, ]s, ]s and ]es caught up within regional ] oblique ]s.


The Narryer Gneiss in this far-eastern region may form the basement to the 2.0-1.8 Ga Proterozoic rocks, and the ] surface may be preserved within the thrust sheets. The Narryer Gneiss in this far-eastern region may form the basement to the 2.0-1.8 billion year old ] rocks, and the ] surface may be preserved within the thrust sheets.


The Narryer Gneiss Terrane is divided into four major rock sequences (Myers 1990); the Dugel Gneiss, Meeberrie Gneiss, Manfred Complex, and unassigned polydeformed leucocratic gneisses and metasediments. The Narryer Gneiss terrane is divided into four major rock sequences (Myers 1990); the Dugel Gneiss, Meeberrie Gneiss, Manfred Complex, and unassigned polydeformed leucocratic gneisses and metasediments.


===Dugel Gneiss=== ==Dugel Gneiss==
The Dugel Gneiss is syenogranitic or monzogranitic in composition and this is interpreted as the ]. The gneiss is leucocratic, with only minor amounts of biotite and muscovite. The rock exhibits variable intensity of metamorphic banding which may include grain size variations, and has a high degree of deformation around the margins, and preserves an ] facies metamorphic assemblage. The gneiss is pervasively shot through with pegmatite veins. The Dugel Gneiss is syenogranitic or monzogranitic in composition and this is interpreted as the protolith. The gneiss is leucocratic, with only minor amounts of ] and ]. The rock exhibits variable intensity of ] which may include grain size variations, and has a high degree of deformation around the margins, and preserves an amphibolite facies metamorphic assemblage. The gneiss is pervasively shot through with ] veins.


Within the low-strain zones, the Dugel Gneiss exists as a medium grained leucocratic metagranite with phenocrysts of K-feldspar which has recrystallized into granulite facies. The rock is greasy-looking with annealed quartz and feldspar, and syn-granulite facies ] cutting across metamorphic banding, and subsequently deformed by later metamorphism. Within the low-strain zones, the Dugel Gneiss exists as a medium-grained leucocratic metagranite with ]s of ] which has recrystallized into granulite facies. The rock is greasy-looking with ]ed ] and ], and syn-granulite facies ] cutting across metamorphic banding, and subsequently deformed by later ].


The Dugel Gneiss is considered to be intruded into the older Meeberrie Gneiss, possibly as sheets or sills, but most contacts are overprinted by ductile metamorphic banding or ] zones. The Dugel Gneiss is considered to be intruded into the older Meeberrie Gneiss, possibly as sheets or ]s, but most contacts are overprinted by ductile metamorphic banding or ] zones.


===Meeberrie Gneiss=== ==Meeberrie Gneiss==
The Meeberrie Gneiss is a generally ductilely deformed banded gneiss of monzogranitic composition, and its protolith is interpreted as a set of monzogranite sills or lopolithic intrusions. The Meeberrie Gneiss is a generally ductilely deformed banded gneiss of monzogranitic composition, and its protolith is interpreted as a set of monzogranite sills or lopolithic intrusions.


The gneiss is heavily banded by layers of amphibolite-K-feldspar-quartz of varying grainsize, plus networks of pegmatite veins. Most is strongly deformed, but least-deformed areas show a relict ] to equigranular texture. The gneiss is heavily banded by layers of amphibolite-K-feldspar-quartz of varying grainsize, plus networks of pegmatite veins. Most is strongly deformed, but least-deformed areas show a relict ] to equigranular texture.


===Manfred Complex=== ==Manfred Complex==
The Manfred Complex is a heavily attenuated and discontinuous series of ultramafic to mafic ] contained within a matrix or wall-rocks of mixed Dugel and Meeberrie Gneisses. The rock types are primarily pyroxene gabbro to amphibolite, with rare ] peridotite and dunite, occasionally containing relict igneous or metamorphic olivine. The Manfred Complex is a heavily attenuated and discontinuous series of ultramafic to mafic ] contained within a matrix or wall-rocks of mixed Dugel and Meeberrie Gneisses. The rock types are primarily ] ] to amphibolite, with rare ] ] and ], occasionally containing relict igneous or metamorphic ].


These ] of material range from centimetre-scale to ~100m thick and one kilometre long and, based on their position within anticlines and synclines in the Mount Narryer area, are interpreted to have intruded subparallel to bedding and are now strung out by shearing. These ] of material range from centimetre-scale to ~100m thick and one kilometre long and, based on their position within ]s and ]s in the ] area, are interpreted to have intruded subparallel to bedding and are now strung out by ].


The Manfred Complex is interpreted to represent an early Archaean mafic to ultramafic layered intrusion which has been disaggregated. This disaggregation is partly tectonic, but in some areas evidence suggests that this was mostly achieved by the intrusion of the Dugel and Meeberrie gneisses as sills or sheets. The Manfred Complex is interpreted to represent an early ] mafic to ultramafic layered intrusion which has been disaggregated. This disaggregation is partly tectonic, but in some areas evidence suggests that this was mostly achieved by the intrusion of the Dugel and Meeberrie gneisses as sills or sheets.


Geochronology on the Manfred Complex places its age at around 3730 Ma via Pb-Pb on zircon. This makes it the oldest recognised intrusive rock on the Earth, containing the oldest known igneous textures and mineral assemblages. ] on the Manfred Complex places its age at around 3.73 billion via ]-Pb on zircon. This makes it the oldest recognised intrusive rock on the Earth, containing the oldest known igneous textures and mineral assemblages.


=== Metasedimentary rocks === ==Metasedimentary rocks==
Metasedimentary rocks from within the Narryer Gneiss terrane account for about 10% of the outcrop and are variably deformed but uniformly of at least amphibolite grade metamorpism. Metasedimentary rocks from within the Narryer Gneiss terrane account for about 10% of the outcrop and are variably deformed but uniformly of at least amphibolite grade metamorphism.


The most abundant rock types are ] and banded iron formation, with subordinate metamorphic gneisses, metaconglomerates and pelitic to semi-pelitic quartz-muscovite schists. The most abundant rock types are ] and ], with subordinate metamorphic gneisses, metaconglomerates and pelitic to semi-pelitic quartz-muscovite ]s.


The conglomerates are primarily orthoquartzite monomict vein-pebble conglomerates, or polymict pebble conglomerates. In low-strain zones they preserve graded bedding, cross-bedding and heavy-mineral rich horizons. The conglomerates are primarily orthoquartzite monomict vein-] conglomerates, or ] pebble conglomerates. In low-strain zones they preserve graded bedding, ] and heavy mineral-rich horizons.


These rocks provide the bulk of age determinations from the Narryer Gneiss Terrane from detrital zircons, with the bulk of readings bracketing 3.5 to 3.75 Ga, 3.35 to 3.45 Ga, and a population of 4.1 to 4.2 Ga, with outliers of up to 4.45 Ga. These rocks provide the bulk of age determinations from the Narryer Gneiss terrane from detrital zircons, with the bulk of readings bracketing 3.5 to 3.75 billion years old, 3.35 to 3.45 billion years old, and a population of 4.1 to 4.2 billion years, with outliers of up to 4.4 billion years old.


==Structure== ==Structure==
The Narryer Gneiss Terrane has undergone many high-grade polyphase deformation events, with the most notable being at 2600 to 2700 Ma associated with granite-greenstone magmatism in the Yilgarn Craton, following an event at ~3350 Ma of amphibolite facies, resulting in widespread re-equilibration of ], preceded by a deformation loosely constrained to ~3680 Ma and another predating the Meeberrie Gneiss and postdating the Manfred Complex, between 3680 and 3730 Ma. The Narryer Gneiss terrane has undergone many high-grade polyphase deformation events, with the most notable being at 2600 to 2700 ] associated with granite-] ] in the ], following an event at ~3350 Ma of amphibolite facies, resulting in widespread re-equilibration of geochronometers, preceded by a deformation loosely constrained to ~3680 Ma and another predating the Meeberrie Gneiss and postdating the Manfred Complex, between 3680 and 3730 Ma.


Older structural grain is preserved in areas of low stress in subsequent deformations; the 2700 to 2600 Ma Yilgarn Craton associated deformation has overprinted most other deformations, resulting in rotation of previous structures into parallelism with NE-trending upright folds and metamorphic banding. Older structural grain is preserved in areas of low stress in subsequent deformations; the 2700 to 2600 Ma Yilgarn Craton associated deformation has overprinted most other deformations, resulting in rotation of previous structures into parallelism with NE-trending upright folds and metamorphic banding.


Proximal to the Proterozoic orogens and thrust belts, the gneiss belt has become variably overprinted by later deformations. In the Bryah-Padbury Basin fold-thrust belt, Yarlarweelor Gneiss rafts exist as undeformed thrust plates of pelitic schist bounded by discrete mylonite zones, as well as deformed heavily overprinted gneiss blocks caught up within shear zones, some of which appear to preserve the unconformity surface. Proximal to the Proterozoic orogens and thrust belts, the gneiss belt has become variably overprinted by later deformations. In the Bryah-Padbury Basin fold-thrust belt, Yarlarweelor Gneiss rafts exist as undeformed thrust plates of pelitic schist bounded by discrete mylonite zones, as well as deformed heavily overprinted gneiss blocks caught up within shear zones, some of which appear to preserve the unconformity surface.


== Sequence of events == == Sequence of events ==
A simplified sequence of events known from the Narryer Gneiss Terrane of the Western Gneiss Belt of the ] is reproduced after A. F. Trendall (1991); A simplified sequence of events known from the Narryer Gneiss terrane of the Western Gneiss Belt of the Yilgarn craton is reproduced after A. F. Trendall (1991);


* 2000-1600 Ma; <br>Basic dykes, related to the ] and ] * 2000-1600 ]; <br>Basic ], related to the ] and ]
* 2700-2600 Ma; <br> Granite sheets and juxtaposition with the Yilgarn craton. * 2700-2600 Ma; <br> Granite sheets and juxtaposition with the Yilgarn craton.
* 3350-3300 Ma; Amphibolite to granulite facies metamorphism * 3350-3300 Ma; Amphibolite to granulite facies metamorphism
* ~3350-3400 Ma; deposition of metasedimentary rocks * ~3350-3400 Ma; deposition of metasedimentary rocks
* 3400 Ma; Intrusion of syenogranites to form Dugel Gneiss, basic and ultramafic dykes * 3400 Ma; Intrusion of ]s to form Dugel Gneiss, basic and ultramafic dykes
* >3400-3680 Ma; Deformation * >3400-3680 Ma; Deformation
* ~3680 Ma; Meeberrie Gneiss * ~3680 Ma; Meeberrie Gneiss
* >3680-3730 Ma; Deformation * >3680-3730 Ma; Deformation
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* >4100 Ma; Metasedimentary precursor gneiss to host the Manfred Complex * >4100 Ma; Metasedimentary precursor gneiss to host the Manfred Complex


==References== == References ==
{{portal|Geology|Western Australia}}
⚫
{{reflist}}
Fletcher, I.R., D.K. Paul, and A.F. Trendall. (1990) ''Sm‐Nd and geochemical characteristics of metasedimentary rocks at Mt Narryer, Western Australia''. Australian Journal of Earth Sciences 39:67-78.

== Further reading ==
⚫ *
* Myers, J.S., 1990. Western Gneiss Terrane. '''In'' Geology and Mineral Resources of Western Australia: Western Australia Geological Survey, Memoir 3, p 13-31. * Myers, J.S., 1990. Western Gneiss Terrane. '''In'' Geology and Mineral Resources of Western Australia: Western Australia Geological Survey, Memoir 3, p 13-31.
* Valley JW, Cavosie AJ, Ushikubo T, Reinhard DA, Lawrence DF, Larson DJ, Clifton PH, Kelly TF, Wilde SA, Moser DE, Spicuzza MJ (2014) Hadean age for a post-magma-ocean zircon confirmed by atom-probe tomography. Nature Geosci 7: 219-223.

{{coord missing|Western Australia}}


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Latest revision as of 07:55, 29 December 2024

Geological complex of ancient rocks in Western Australia

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Narryer Gneiss Terrane
Stratigraphic range: Archean
>3.3 Ga
Satellite image of Jack Hills in the Narryer Gneiss Terrane
TypeGeological complex
Sub-unitsDugel Gneiss, Meeberrie Gneiss, Manfred Complex and metasedimentary rocks
Lithology
PrimaryGranite
Location
RegionYilgarn Craton
CountryWestern Australia, Australia

The Narryer Gneiss terrane is a geological complex in Western Australia that is composed of a tectonically interleaved and polydeformed mixture of granite, mafic intrusions and metasedimentary rocks in excess of 3.3 billion years old, with the majority of the Narryer Gneiss terrane in excess of 3.6 billion years old. The rocks have experienced multiple metamorphic events at amphibolite or granulite conditions, resulting in often complete destruction of original igneous or sedimentary (protolith) textures. Importantly, it contains the oldest known samples of the Earth's crust: samples of zircon from the Jack Hills portion of the Narryer Gneiss have been radiometrically dated at 4.4 billion years old, although the majority of zircon crystals are about 3.6-3.8 billion years old.

The Narryer Gneiss terrane is adjacent to the northernmost margin of the Yilgarn Craton and is abutted on the north by the Gascoyne Complex metasedimentary and metagranite orogen. The Narryer Gneiss terrane also includes parts of the Yarlarweelor Gneiss which abuts to Nabberu Basin metamorphic sequences of the Bryah-Padbury Basins, where it is present as discontinuous slivers of metamorphic rocks, pelites, metaconglomerates and gneisses caught up within regional strike-slip oblique thrust faults.

The Narryer Gneiss in this far-eastern region may form the basement to the 2.0-1.8 billion year old Proterozoic rocks, and the unconformity surface may be preserved within the thrust sheets.

The Narryer Gneiss terrane is divided into four major rock sequences (Myers 1990); the Dugel Gneiss, Meeberrie Gneiss, Manfred Complex, and unassigned polydeformed leucocratic gneisses and metasediments.

Dugel Gneiss

The Dugel Gneiss is syenogranitic or monzogranitic in composition and this is interpreted as the protolith. The gneiss is leucocratic, with only minor amounts of biotite and muscovite. The rock exhibits variable intensity of metamorphic banding which may include grain size variations, and has a high degree of deformation around the margins, and preserves an amphibolite facies metamorphic assemblage. The gneiss is pervasively shot through with pegmatite veins.

Within the low-strain zones, the Dugel Gneiss exists as a medium-grained leucocratic metagranite with phenocrysts of K-feldspar which has recrystallized into granulite facies. The rock is greasy-looking with annealed quartz and feldspar, and syn-granulite facies leucosomes cutting across metamorphic banding, and subsequently deformed by later metamorphism.

The Dugel Gneiss is considered to be intruded into the older Meeberrie Gneiss, possibly as sheets or sills, but most contacts are overprinted by ductile metamorphic banding or mylonite zones.

Meeberrie Gneiss

The Meeberrie Gneiss is a generally ductilely deformed banded gneiss of monzogranitic composition, and its protolith is interpreted as a set of monzogranite sills or lopolithic intrusions.

The gneiss is heavily banded by layers of amphibolite-K-feldspar-quartz of varying grainsize, plus networks of pegmatite veins. Most is strongly deformed, but least-deformed areas show a relict porphyritic to equigranular texture.

Manfred Complex

The Manfred Complex is a heavily attenuated and discontinuous series of ultramafic to mafic cumulates contained within a matrix or wall-rocks of mixed Dugel and Meeberrie Gneisses. The rock types are primarily pyroxene gabbro to amphibolite, with rare serpentinised peridotite and dunite, occasionally containing relict igneous or metamorphic olivine.

These boudins of material range from centimetre-scale to ~100m thick and one kilometre long and, based on their position within anticlines and synclines in the Mount Narryer area, are interpreted to have intruded subparallel to bedding and are now strung out by shearing.

The Manfred Complex is interpreted to represent an early Archaean mafic to ultramafic layered intrusion which has been disaggregated. This disaggregation is partly tectonic, but in some areas evidence suggests that this was mostly achieved by the intrusion of the Dugel and Meeberrie gneisses as sills or sheets.

Geochronology on the Manfred Complex places its age at around 3.73 billion via Pb-Pb on zircon. This makes it the oldest recognised intrusive rock on the Earth, containing the oldest known igneous textures and mineral assemblages.

Metasedimentary rocks

Metasedimentary rocks from within the Narryer Gneiss terrane account for about 10% of the outcrop and are variably deformed but uniformly of at least amphibolite grade metamorphism.

The most abundant rock types are quartzite and banded iron formation, with subordinate metamorphic gneisses, metaconglomerates and pelitic to semi-pelitic quartz-muscovite schists.

The conglomerates are primarily orthoquartzite monomict vein-pebble conglomerates, or polymict pebble conglomerates. In low-strain zones they preserve graded bedding, cross-bedding and heavy mineral-rich horizons.

These rocks provide the bulk of age determinations from the Narryer Gneiss terrane from detrital zircons, with the bulk of readings bracketing 3.5 to 3.75 billion years old, 3.35 to 3.45 billion years old, and a population of 4.1 to 4.2 billion years, with outliers of up to 4.4 billion years old.

Structure

The Narryer Gneiss terrane has undergone many high-grade polyphase deformation events, with the most notable being at 2600 to 2700 Ma associated with granite-greenstone magmatism in the Yilgarn Craton, following an event at ~3350 Ma of amphibolite facies, resulting in widespread re-equilibration of geochronometers, preceded by a deformation loosely constrained to ~3680 Ma and another predating the Meeberrie Gneiss and postdating the Manfred Complex, between 3680 and 3730 Ma.

Older structural grain is preserved in areas of low stress in subsequent deformations; the 2700 to 2600 Ma Yilgarn Craton associated deformation has overprinted most other deformations, resulting in rotation of previous structures into parallelism with NE-trending upright folds and metamorphic banding.

Proximal to the Proterozoic orogens and thrust belts, the gneiss belt has become variably overprinted by later deformations. In the Bryah-Padbury Basin fold-thrust belt, Yarlarweelor Gneiss rafts exist as undeformed thrust plates of pelitic schist bounded by discrete mylonite zones, as well as deformed heavily overprinted gneiss blocks caught up within shear zones, some of which appear to preserve the unconformity surface.

Sequence of events

A simplified sequence of events known from the Narryer Gneiss terrane of the Western Gneiss Belt of the Yilgarn craton is reproduced after A. F. Trendall (1991);

  • 2000-1600 Ma;
    Basic dykes, related to the Gascoyne Complex and Capricorn Orogeny
  • 2700-2600 Ma;
    Granite sheets and juxtaposition with the Yilgarn craton.
  • 3350-3300 Ma; Amphibolite to granulite facies metamorphism
  • ~3350-3400 Ma; deposition of metasedimentary rocks
  • 3400 Ma; Intrusion of syenogranites to form Dugel Gneiss, basic and ultramafic dykes
  • >3400-3680 Ma; Deformation
  • ~3680 Ma; Meeberrie Gneiss
  • >3680-3730 Ma; Deformation
  • ~3780 Ma; Manfred Complex ultramafic-mafic layered intrusion
  • >4100 Ma; Metasedimentary precursor gneiss to host the Manfred Complex

References

Fletcher, I.R., D.K. Paul, and A.F. Trendall. (1990) Sm‐Nd and geochemical characteristics of metasedimentary rocks at Mt Narryer, Western Australia. Australian Journal of Earth Sciences 39:67-78.

Further reading

  • Geochronological analysis of Narryer Gneiss zircons
  • Myers, J.S., 1990. Western Gneiss Terrane. 'In Geology and Mineral Resources of Western Australia: Western Australia Geological Survey, Memoir 3, p 13-31.
  • Valley JW, Cavosie AJ, Ushikubo T, Reinhard DA, Lawrence DF, Larson DJ, Clifton PH, Kelly TF, Wilde SA, Moser DE, Spicuzza MJ (2014) Hadean age for a post-magma-ocean zircon confirmed by atom-probe tomography. Nature Geosci 7: 219-223.

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