Arthur H. Hickman
Springer International Publishing
e druk, 2023
9783031180057
Archean Evolution of the Pilbara Craton and Fortescue Basin
Specificaties
Gebonden, blz.
|
Engels
Springer International Publishing |
2023
ISBN13: 9783031180057
Rubricering
Onderdeel van serie
Modern Approaches in Solid Earth Sciences
Levertijd ongeveer 9 werkdagen
Gratis verzonden
Samenvatting
One of today’s major geoscientific controversies centres on the origin of the Archean granite‒greenstone terranes. Is the geology of these scattered remnants of our planet’s early crust consistent with the theory that modern-style plate-tectonic processes operated from the early Archean, or does it indicate that tectonic and magmatic processes were different in the Archean? Earth has clearly evolved since its initial formation, so at what stage did its processes of crustal growth first resemble those of today? The logical place to seek answers to these intriguing and important questions is within the best-preserved early Archean crust.
The Pilbara region of northwest Australia is internationally famous for its abundant and exceptionally well-preserved fossil evidence of early life. However, until recently the area has received much less recognition for the key evidence it provides on early Archean crustal evolution. This book presents and interprets this evidence through a new stage-by-stage account of the development of the Pilbara’s geological record between 3.53 and 2.63 Ga.
The Archean Pilbara crust represents one fragment of Earth’s oldest known supercontinent Vaalbara, which also included the Kaapvaal Craton of southern Africa. Recognition of Vaalbara expands the background database for both these areas, allowing us to more fully understand each of them.
Specificaties
ISBN13:9783031180057
Taal:Engels
Bindwijze:gebonden
Uitgever:Springer International Publishing
Inhoudsopgave
<p>Chapter 1</p>
<p>Overview of the Pilbara Craton</p>
<p>1.1 Introduction</p>
<p>1.1.2 Investigations of the Pilbara Craton</p>
<p>1.1.3 Stratigraphy of the northern Pilbara Craton</p>
<p>1.1.4 Tectonic units</p>
<p>1.1.5 Fragment of an Archean continent</p>
<p>1.1.6 Vaalbara continent?</p>
<p>1.1.7 Concept of an ‘ancient nucleus’</p>
<p>1.1.8 Concealed Pilbara Craton</p>
<p> </p>
<p>Chapter 2</p>
<p>Eoarchean and early Paleoarchean crust of the Pilbara Craton</p>
<p>2.1 Introduction</p>
<p>2.2 Eoarchean to early Paleoarchean crust (3800–3530 Ma)</p>
<p>2.2.1 U–Pb zircon geochronology</p>
<p>2.2.2 Sm–Nd isotope data</p>
<p>2.2.3 Lu–Hf isotopes in zircon</p>
<p>2.3 Conclusions</p>
<p> </p>
<p>Chapter 3</p>
<p>Warrawoona Large Igneous Province, 3530–3427 Ma</p>
<p>3.1 Introduction</p>
<p>3.1.1 Preservation of the Warrawoona Group</p>
<p>3.2 Stratigraphy</p>
<p>3.2.1 Coonterunah Subgroup</p>
<p>3.2.2 Talga Talga Subgroup</p>
<p>3.2.3 Coongan Subgroup</p>
<p>3.2.4 Salgash Subgroup</p>
<p>3.3 Origin of the Warrawoona Group</p>
<p>3.4 Evolution of the Warrawoona Group</p>
<p>3.5 Large Igneous Province</p>
<p>3.6 Granitic supersuites of the Warrawoona LIP</p>
<p>3.6.1 Mulgundoona Supersuite (3530–3490 Ma)</p>
<p>3.6.2 Callina Supersuite (3484–3462 Ma)</p>
<p>3.6.3 Tambina Supersuite (3451–3416 Ma)</p>
<p>3.6.4 Emu Pool Supersuite (3324–3290 Ma)</p>
<p>3.6.5 Cleland Supersuite (3270–3223 Ma)</p>
<p>3.7 Tectonic setting of the Warrawoona LIP</p>
<p>3.7.1 Plate tectonic models</p>
<p>3.7.2 Oceanic plateau?</p>
<p> </p>
<p>Chapter 4</p>
Strelley Pool Formation: continental sedimentation between Paleoarchean LIPs<p></p>
<p>4.1 Introduction</p>
<p>4.2 Stratigraphy</p>
<p>4.2.1 Stratigraphic rank: formation or group?</p>
<p>4.2.2 Relations to the Panorama Formation</p>
<p>4.2.3 Unconformities</p>
<p>4.3 Geochronology</p>
<p>4.4 World’s oldest paleosols</p>
<p>4.5 Suggestion of hydrothermal deposition</p>
<p>4.6 Correlation with the Buck Reef Chert</p>
<p>4.7 Fossil record</p>
<p>4.7.1 Stromatolites</p>
<p>4.7.2 Microfossils</p>
<p>4.7.3 Microbial mats</p>
<p>4.8 Significance to crustal evolution</p>
<p>4.9 Conclusions</p>
<p> </p>
<p>Chapter 5</p>
<p>Kelly Large Igneous Province, 3350–3315 Ma</p>
<p>5.1 Introduction</p>
<p>5.1.1 Tectonic setting</p>
<p>5.1.2 Kelly Large Igneous Province</p>
<p>5.2 Stratigraphy</p>
<p>5.2.1 Euro Basalt</p>
<p>5.2.2 Wyman Formation</p>
<p>5.2.3 Charteris Basalt</p>
<p>5.2.4 Unconformities within the Kelly Group</p>
<p>5.3 Komatiite and komatiitic basalt in the Kelly Group</p>
<p>5.4 Tholeiitic basalt in the Kelly Group</p>
<p>5.5 Sm–Nd isotope data</p>
<p>5.6 Relevance to continental deposition of the Warrawoona Group</p>
<p>5.7.1 Emu Pool Supersuite (3324–3290 Ma)</p>
5.8 Emu Pool Event (3325–3290 Ma)<p></p>
<p> </p>
<p>Chapter 6</p>
<p>Paleoarchean continental breakup of the Pilbara Craton</p>
<p>6.1 Introduction</p>
<p>6.2 East Pilbara Terrane Rifting Event</p>
<p>6.3 Stratigraphy</p>
<p>6.3.1 Sulphur Springs Group</p>
<p>6.3.2 Roebourne Group</p>
<p>6.3.3 Cleland Supersuite</p>
<p>6.4 Continental breakup</p>
<p>6.4.1 Evidence</p>
<p>6.4.2 Other fragments of the Paleoarchean plateau?</p>
<p> </p>
<p>Chapter 7</p>
<p>Mesoarchean rift and marginal basins of the Pilbara Craton</p>
<p>7.1 Introduction</p>
<p>7.2 Basaltic rift basins</p>
<p>7.2.1 Regal Basin</p>
<p>7.3 Early Mesoarchean passive margins</p>
<p>7.3.1 Soanesville Basin</p>
<p>7.3.2 Nickol River Basin</p>
<p>7.3.3 Early Mosquito Creek Basin</p>
<p> </p>
<p>Chapter 8</p>
<p>Mesoarchean subduction in the Pilbara Craton</p>
<p>8.1 Introduction</p>
<p>8.2 Sholl Terrane</p>
<p>8.2.1 Whundo Group</p>
<p>8.2.2 Railway Supersuite</p>
<p>8.3 Ophiolite (3220–3165 Ma Regal Formation)</p>
<p>8.4 Prinsep Orogeny and Elizabeth Hill Supersuite</p>
<p>8.4.1 Elizabeth Hill Supersuite</p>
<p>8.5 Magmatic arcs of the De Grey Superbasin</p>
<p>8.5.1 Orpheus Supersuite</p>
<p>8.5.2 Maitland River Supersuite</p>
<p>8.5.3 Sisters Supersuite</p>
<p> </p>
<p>Chapter 9</p>
<p>Mesoarchean basin evolution inland of magmatic arcs</p>
<p>9.1 Introduction</p>
<p>9.2 De Grey Supergroup</p>
<p>9.2.1 Gorge Creek Group</p>
<p>9.2.2 Regional stratigraphic continuity</p>
<p>9.2.3 Conclusions regarding the Gorge Creek Basin</p>
<p>9.2.4 Geochronology</p>
<p>9.2.5 Coonieena Basalt</p>
<p>9.2.6 Croydon Group</p>
<p>9.2.7 Whim Creek Group</p>
<p>9.2.8 Bookingarra Group</p>
<p>9.3 Tectonic evolution of the De Grey Superbasin</p>
<p> </p>
<p>Chapter 10</p>
<p>Orogenies, cratonization and post-orogenic granites</p>
<p>10.1 Introduction</p>
<p>10.1.1 North Pilbara Orogeny</p>
<p>10.1.2 Mosquito Creek Orogeny</p>
<p>10.2 Cutinduna Supersuite</p>
<p>10.3 Split Rock Supersuite</p>
<p> </p>
<p>Chapter 11</p>
<p>Mineralization in the northern Pilbara</p>
<p>11.1 Paleoarchean mineralization</p>
<p>11.1.1 Sediment-hosted, hydrothermal massive sulfates</p>
<p>11.1.2 Volcanogenic massive sulfides</p>
<p>11.1.3 Black shale-hosted Cu–Zn</p>
<p>11.1.4 Vein and hydrothermal base metals</p>
<p>11.1.5 Copper and molybdenum mineralization</p>
<p>11.1.6 Precious metals</p>
<p>11.2 Mineralization during the EPTRE</p>
<p>11.2.1 Sulphur Springs Group</p>
<p>11.2.2 Roebourne Group</p>
<p>11.2.3 VMS Cu–Zn mineralization, Tabba Tabba Shear Zone</p>
<p>11.2.4 Soanesville Group</p>
<p>11.3 Mesoarchean mineralization</p>
<p>11.3.1 Mineralization during closure of the Regal Basin</p>
<p>11.3.2 Gold and copper north of the Sholl Shear Zone</p>
<p>11.3.3 Mineralization in the De Grey Superbasin</p>
<p>11.3.4 Gold in the Mosquito Creek Basin</p>
<p>11.3.5 Post-orogenic mineralization (2895–2830 Ma)</p>
<p>11.4 Neoarchean mineralization</p>
<p> </p>
<p>Chapter 12</p>
<p>Fortescue Group: the Neoarchean breakup of the Pilbara Craton</p>
<p>12.1 Introduction</p>
<p>12.1.1 Re-definition of the Fortescue Group</p>
<p>12.2 Stratigraphy</p>
<p>12.2.1 Tectono-stratigraphic sequences</p>
<p> </p>
<p>Overview of the Pilbara Craton</p>
<p>1.1 Introduction</p>
<p>1.1.2 Investigations of the Pilbara Craton</p>
<p>1.1.3 Stratigraphy of the northern Pilbara Craton</p>
<p>1.1.4 Tectonic units</p>
<p>1.1.5 Fragment of an Archean continent</p>
<p>1.1.6 Vaalbara continent?</p>
<p>1.1.7 Concept of an ‘ancient nucleus’</p>
<p>1.1.8 Concealed Pilbara Craton</p>
<p> </p>
<p>Chapter 2</p>
<p>Eoarchean and early Paleoarchean crust of the Pilbara Craton</p>
<p>2.1 Introduction</p>
<p>2.2 Eoarchean to early Paleoarchean crust (3800–3530 Ma)</p>
<p>2.2.1 U–Pb zircon geochronology</p>
<p>2.2.2 Sm–Nd isotope data</p>
<p>2.2.3 Lu–Hf isotopes in zircon</p>
<p>2.3 Conclusions</p>
<p> </p>
<p>Chapter 3</p>
<p>Warrawoona Large Igneous Province, 3530–3427 Ma</p>
<p>3.1 Introduction</p>
<p>3.1.1 Preservation of the Warrawoona Group</p>
<p>3.2 Stratigraphy</p>
<p>3.2.1 Coonterunah Subgroup</p>
<p>3.2.2 Talga Talga Subgroup</p>
<p>3.2.3 Coongan Subgroup</p>
<p>3.2.4 Salgash Subgroup</p>
<p>3.3 Origin of the Warrawoona Group</p>
<p>3.4 Evolution of the Warrawoona Group</p>
<p>3.5 Large Igneous Province</p>
<p>3.6 Granitic supersuites of the Warrawoona LIP</p>
<p>3.6.1 Mulgundoona Supersuite (3530–3490 Ma)</p>
<p>3.6.2 Callina Supersuite (3484–3462 Ma)</p>
<p>3.6.3 Tambina Supersuite (3451–3416 Ma)</p>
<p>3.6.4 Emu Pool Supersuite (3324–3290 Ma)</p>
<p>3.6.5 Cleland Supersuite (3270–3223 Ma)</p>
<p>3.7 Tectonic setting of the Warrawoona LIP</p>
<p>3.7.1 Plate tectonic models</p>
<p>3.7.2 Oceanic plateau?</p>
<p> </p>
<p>Chapter 4</p>
Strelley Pool Formation: continental sedimentation between Paleoarchean LIPs<p></p>
<p>4.1 Introduction</p>
<p>4.2 Stratigraphy</p>
<p>4.2.1 Stratigraphic rank: formation or group?</p>
<p>4.2.2 Relations to the Panorama Formation</p>
<p>4.2.3 Unconformities</p>
<p>4.3 Geochronology</p>
<p>4.4 World’s oldest paleosols</p>
<p>4.5 Suggestion of hydrothermal deposition</p>
<p>4.6 Correlation with the Buck Reef Chert</p>
<p>4.7 Fossil record</p>
<p>4.7.1 Stromatolites</p>
<p>4.7.2 Microfossils</p>
<p>4.7.3 Microbial mats</p>
<p>4.8 Significance to crustal evolution</p>
<p>4.9 Conclusions</p>
<p> </p>
<p>Chapter 5</p>
<p>Kelly Large Igneous Province, 3350–3315 Ma</p>
<p>5.1 Introduction</p>
<p>5.1.1 Tectonic setting</p>
<p>5.1.2 Kelly Large Igneous Province</p>
<p>5.2 Stratigraphy</p>
<p>5.2.1 Euro Basalt</p>
<p>5.2.2 Wyman Formation</p>
<p>5.2.3 Charteris Basalt</p>
<p>5.2.4 Unconformities within the Kelly Group</p>
<p>5.3 Komatiite and komatiitic basalt in the Kelly Group</p>
<p>5.4 Tholeiitic basalt in the Kelly Group</p>
<p>5.5 Sm–Nd isotope data</p>
<p>5.6 Relevance to continental deposition of the Warrawoona Group</p>
<p>5.7.1 Emu Pool Supersuite (3324–3290 Ma)</p>
5.8 Emu Pool Event (3325–3290 Ma)<p></p>
<p> </p>
<p>Chapter 6</p>
<p>Paleoarchean continental breakup of the Pilbara Craton</p>
<p>6.1 Introduction</p>
<p>6.2 East Pilbara Terrane Rifting Event</p>
<p>6.3 Stratigraphy</p>
<p>6.3.1 Sulphur Springs Group</p>
<p>6.3.2 Roebourne Group</p>
<p>6.3.3 Cleland Supersuite</p>
<p>6.4 Continental breakup</p>
<p>6.4.1 Evidence</p>
<p>6.4.2 Other fragments of the Paleoarchean plateau?</p>
<p> </p>
<p>Chapter 7</p>
<p>Mesoarchean rift and marginal basins of the Pilbara Craton</p>
<p>7.1 Introduction</p>
<p>7.2 Basaltic rift basins</p>
<p>7.2.1 Regal Basin</p>
<p>7.3 Early Mesoarchean passive margins</p>
<p>7.3.1 Soanesville Basin</p>
<p>7.3.2 Nickol River Basin</p>
<p>7.3.3 Early Mosquito Creek Basin</p>
<p> </p>
<p>Chapter 8</p>
<p>Mesoarchean subduction in the Pilbara Craton</p>
<p>8.1 Introduction</p>
<p>8.2 Sholl Terrane</p>
<p>8.2.1 Whundo Group</p>
<p>8.2.2 Railway Supersuite</p>
<p>8.3 Ophiolite (3220–3165 Ma Regal Formation)</p>
<p>8.4 Prinsep Orogeny and Elizabeth Hill Supersuite</p>
<p>8.4.1 Elizabeth Hill Supersuite</p>
<p>8.5 Magmatic arcs of the De Grey Superbasin</p>
<p>8.5.1 Orpheus Supersuite</p>
<p>8.5.2 Maitland River Supersuite</p>
<p>8.5.3 Sisters Supersuite</p>
<p> </p>
<p>Chapter 9</p>
<p>Mesoarchean basin evolution inland of magmatic arcs</p>
<p>9.1 Introduction</p>
<p>9.2 De Grey Supergroup</p>
<p>9.2.1 Gorge Creek Group</p>
<p>9.2.2 Regional stratigraphic continuity</p>
<p>9.2.3 Conclusions regarding the Gorge Creek Basin</p>
<p>9.2.4 Geochronology</p>
<p>9.2.5 Coonieena Basalt</p>
<p>9.2.6 Croydon Group</p>
<p>9.2.7 Whim Creek Group</p>
<p>9.2.8 Bookingarra Group</p>
<p>9.3 Tectonic evolution of the De Grey Superbasin</p>
<p> </p>
<p>Chapter 10</p>
<p>Orogenies, cratonization and post-orogenic granites</p>
<p>10.1 Introduction</p>
<p>10.1.1 North Pilbara Orogeny</p>
<p>10.1.2 Mosquito Creek Orogeny</p>
<p>10.2 Cutinduna Supersuite</p>
<p>10.3 Split Rock Supersuite</p>
<p> </p>
<p>Chapter 11</p>
<p>Mineralization in the northern Pilbara</p>
<p>11.1 Paleoarchean mineralization</p>
<p>11.1.1 Sediment-hosted, hydrothermal massive sulfates</p>
<p>11.1.2 Volcanogenic massive sulfides</p>
<p>11.1.3 Black shale-hosted Cu–Zn</p>
<p>11.1.4 Vein and hydrothermal base metals</p>
<p>11.1.5 Copper and molybdenum mineralization</p>
<p>11.1.6 Precious metals</p>
<p>11.2 Mineralization during the EPTRE</p>
<p>11.2.1 Sulphur Springs Group</p>
<p>11.2.2 Roebourne Group</p>
<p>11.2.3 VMS Cu–Zn mineralization, Tabba Tabba Shear Zone</p>
<p>11.2.4 Soanesville Group</p>
<p>11.3 Mesoarchean mineralization</p>
<p>11.3.1 Mineralization during closure of the Regal Basin</p>
<p>11.3.2 Gold and copper north of the Sholl Shear Zone</p>
<p>11.3.3 Mineralization in the De Grey Superbasin</p>
<p>11.3.4 Gold in the Mosquito Creek Basin</p>
<p>11.3.5 Post-orogenic mineralization (2895–2830 Ma)</p>
<p>11.4 Neoarchean mineralization</p>
<p> </p>
<p>Chapter 12</p>
<p>Fortescue Group: the Neoarchean breakup of the Pilbara Craton</p>
<p>12.1 Introduction</p>
<p>12.1.1 Re-definition of the Fortescue Group</p>
<p>12.2 Stratigraphy</p>
<p>12.2.1 Tectono-stratigraphic sequences</p>
<p> </p>