Fig. 1. A schematic diagram showing the formation environment of Archean felsic volcanic rocks. Modified from Giles (1980).[1] Felsic eruption forms felsic volcanic rocks near the volcano and a spectrum of volcano-sedimentary sequence in the sea in Archean.[1]

Archean felsic volcanic rocks are felsic volcanic rocks that were formed in the Archean Eon (4 to 2.5 billion years ago).[2] The term "felsic" means that the rocks have silica content of 62–78%.[3] Given that the Earth formed at ~4.5 billion year ago,[4] Archean felsic volcanic rocks provide clues on the Earth's first volcanic activities on the Earth's surface started 500 million years after the Earth's formation.[5]

As the Archean Earth was hotter than the present, formation of felsic volcanic rocks may differ from the modern plate tectonics.[5][6][7]

Archean felsic volcanic rocks are distributed only in the preserved Archean greenstone belts, where deformed sequences of volcanic-sedimentary rocks are common.[5][6][8] Felsic volcanic rocks are rare in the early Earth and only contribute to less 20% of rocks in the Archean greenstone belts worldwide.[6] Nonetheless, mafic volcanic rocks (such as basalt and komatiite, silicate content <52%[3]) occupy about 50% in the greenstone belts.[6] Thus, felsic volcanic rocks are rare members in the Archean terranes.

Archean felsic volcanic activities commonly occur in submarine environments.[7] The composition of Archean felsic volcanic rocks are equivalent to a spectrum between dacite and rhyolite.[5] They can be distinguished by their mineral assemblages, rock chemistry and rock layer relationship in the sequences.[7]

Archean felsic volcanic rocks are utilised to date the timing of geological events and match distant rock units in separated Archean cratons.[9] They are important to reconstruct Archean geological environments.[10][11]

Felsic granitoids are the most prevalent rock type in Archean terranes.[6] These intrusive felsic igneous rocks include TTG suites (Tonalite-trondhjemite-granodiorite) that contributes over half the portion of Archean cratons.[6] They have implications in finding how the felsic volcanic rocks were formed and related to the granitoids.[9][12]

Occurrence

Archean felsic volcanic rocks are only preserved in Archean cratons.[8] A craton is an ancient stable continental block.[13] Also, a craton has survived from plate tectonics that pull apart, collide or tear continents.[13] On average, the felsic volcanic rocks only contribute to ≈15-20% in volcanic rocks of greenstone belts.[6] See Figure 2 and Table 1 for Examples of Archean felsic volcanic rocks occurrence.

All Archean felsic volcanic rocks are distributed in greenstone belts.[6] In Archean cratons, greenstone belts represent supracrustal rocks formed at the Earth's surface and the belts are dominated by volcano-sedimentary sequences.[9][11][14][15][16] Some volcanic sequences can be several kilometers thick, such as the Warrawoona Group of Eastern Pilbara Craton.[17][18] However, ultramafic and mafic units make up the major volume of the volcanic units.[18] The remaining volcanic units are extensive but thin felsic volcanic layers, such as Duffer Formation of the Warrawoona Group.[17] The greenstone belts may be subsequently intruded by dome-shaped magma chambers.[19] The intrusion deformed the felsic volcanic rocks along with the volcano-sedimentary sequences.[5]

Observing modern volcanic processes is relatively easier than observing Archean volcanism, because erosion constantly started removing earlier formed materials.[20] So, studying the Archean supracrustal rocks back in deep time may be subjected to sampling bias.[6]

Table 1. Examples of Archean felsic volcanic rocks occurrence in greenstone belts
Felsic volcanic units/localities Age (Ma) Greenstone belt Craton Country/Region
Duffer Formation[11][10] 3468 ± 2[21] Warrawoona Eastern Pilbara Craton Australia
Marda Tank[22] 2734 ± 3[23] Marda Volcanic Complex Yilgarn Craton Australia
Kallehadlu Felsic Volcanics[15] 2677 ± 2[24] Gadag-Chitradurga Dharwar Craton India
Kovero schist belt[25] 2754 ± 6[25] Ilomantsi Baltic Shield Finland
Sample SM/GR/93/57[26][27] 3710 ± 4[27] Isua North Atlantic Craton Greenland
Musk massive sulphide deposit[28] 2689.3 +2.4/-1.8[28] Yellowknife Slave Province Canada
Blake River Group[29][30] 2694.1±4.5[31] Abitibi Superior Province Canada
Upper Michipicoten volcanic sequences[32] 2696 ± 2[33] Wawa Superior Province Canada
Bulawayan Group[34] 2615 ± 28[34] Harare Zimbabwean Craton Zimbabwe
Onverwacht Group[35] 3445 ± 3[35] Barberton Kaapvaal Craton South Africa
Fig. 2. A map showing examples greenstone belts with documented Archean felsic volcanic rocks localities. See citations in Table 1.

Characteristics

Mineralogy and texture

The meaning of "felsic" refers to high silica (SiO2) content from 62 to 78 wt% in rock.[3] In terms of mineralogy, the felsic volcanic rocks are rich in feldspar and quartz.[36] A typical mineral assemblage is quartz + feldspar (albite/oligoclase) + amphibole (chlorite) + micas (biotite and/or muscovite).[36] The mineralogy seems similar with modern rhyolites and dacites.[36] The volcanics are aphanitic, whereas some exhibits porphyritic texture that certain larger minerals (phenocrysts) are visible by eyes.[37]

Fig. 3. Archean felsic volcanic rocks have particular characteristic structure. Some are tuffs, formed by volcanic materials from eruption. A significant structure is fiamme, which are recrystallised quartz with flame-like ending points. The illustration is fiamme in Archean Woman Lake rhyolitic tuff, Superior Province, Canada. Adopted and modified from photograph of Thurston (1980).[37]

Felsic volcanic rocks also include felsic tuff that was formed when tephra was consolidated.[17] Tuff is composed of volcanic ash, glass shards and lithic fragments.[11][37] Reported eutaxitic tuff from Superior Province, Canada (Figure 3),[37] contains lenticular fiamme. When hot pumice deposits on a cool surface, it is rapidly cooled, recrystallised and welded into quartz with flame-like ending tips.[37] The eutaxitic texture represents a hot vapour-phase emplacement of the fragmented volcanic materials on the Earth's surface.[37]

Flow bands are present in massive, uniform felsic lava flow units.[36] When the viscous lava flow encounters a surface, friction drags the mobile lava and forms internal banding.[36]

Structureless hyaloclastite is commonly found in Archean felsic volcanic rocks.[7][17][36][37] In submarine environments, water quenches and cools lava rapidly during volcanic eruption.[7] The flow is fragmented and form glassy volcanic breccia.[7]

Geochemistry

The composition of Archean felsic volcanic rocks falls in the calc-alkaline series.[32] Such magmatic series indicate that fractional crystallisation of magma occurred during cooling. Magnesium and iron content in the rock are low, and it forms dacite or rhyolite. Magma is a mixture of various minerals. When minerals crystallise from the molten magma, they are progressively removed and dissociated from the melt. The last proportion of the melt is strongly fractionated, causing richness in quartz and feldspars that make the volcanic rocks felsic.

Dacite and rhyolite are characterised by high silica (SiO2) content from 62 to 78 wt%.[3] The average composition of felsic volcanic rocks in Archean greenstone belts is between dacite and rhyolite (Table 2).[3][6] In comparison, the modern felsic volcanic rock average composition (after Archean, <2.5 Ga) is similar to rhyolite, indicating a more felsic shift with greater alkali content in felsic volcanism.[6] However, the composition may be biased because of weathering right after deposition or metamorphism during later stages of deformation.[9]

Table 2. Average composition of felsic volcanic rocks[6]
Time SiO2 (wt%) Na2O+K2O (wt%) Rock Classification[3]
Archean 72.2–73.0 6.4–6.8 Dacite–Rhyolite
Post-Archean 73.0–73.6 7.0–8.0 Rhyolite

Archean felsic volcanic rocks also have high zircon abundance. Incompatible elements, like zirconium, are reluctant to substitute into early-forming crystals.[17] As a result, they tend to remain in the melt. In strongly fractionated felsic magma, zircon is easily saturated. As a result, zircon is common in felsic rocks.[38] The timing of felsic volcanism and tectonic constraints can be identified by radiometric dating and isotopic analysis.[17]

Eruption style

In the Archean aeon, underwater eruptions of felsic lava were common.[7][36][39] Submarine eruption is evident by coarse volcanic breccia formed in situ, hyaloclastite or underwater pyroclastic deposits (clastic rock, composed of tephra only). Since felsic magma is viscous, volcanic eruptions that form dacite or rhyolite are explosive and violent. The Archean felsic eruption may be assigned to Vesuvius eruption type in the present day.[36]

Submarine rhyolitic flows were widespread in the Archean but are uncommon in the modern volcanic environment.[39] Viscous felsic eruption often causes pyroclastic flow (hot, dense gas with volcanic fragments) instead of fluid lava flow. However, if the rhyolitic lava is still molten during eruption, it can behave and flow like fluid lava.[7][40]

Subaqueous deposits

Fig. 4. Schematic illustration of documented subaqueous felsic lava deposits. (a) Submarine lava flow, based on Héré Creek rhyolite (modified from De Rosen-Spence et al., 1980[7]). (b) Submarine lava dome, based on the Gold Lake dome and flow complex (modified from Lambert et al., 1990).[41] Illustration adopted from Sylvester et al. (1997) in de Wit & Ashwal (1997).[14]

Felsic lava flow and lava dome are the two common types of underwater deposits formed by Archean felsic volcanic rocks (Fig. 4).[7] Documented Archean lava structures are distinctive from post-Archean felsic lava because underwater eruptions are so rare in the post-Archean.[39] The dacitic or rhyolitic lava flows are quenched right after the eruption.[7][17] When seawater contacts the flow, the lava quickly cools down.[40] Finally, The lava solidifies and breaks up as clasts, and the clasts accumulate on the flow fronts to form breccia.[36]

Lava flow

Effusive felsic lava flows elongate several kilometres. During an eruption, lava continuously wells out from the vent, then starts to flow outward on the sea floor. Due to quenching, lava is rapidly fragmented to form breccia.[40] A new lobe of lava is injected inside the breccia but it is cooled less quickly, and pushes the flow further outwards.[7]

Lava dome

Short, stocky dome with subsequent pyroclastic deposits extend less than few kilometres long. When explosive eruption occurs, volcanic fragments would be deposited by violent pyroclastic flows. Coarse breccia would be formed as a result.[41] Submarine sediments would subsequently be deposited along the steep flank of the volcano.[41] Submarine landslides would occur to form turbidites.[41]

Stratigraphic significance

Archean felsic volcanic rocks are important in determining absolute age of the rock units in greenstone belts.[14] Felsic eruptions are episodic, making the felsic volcanic layers distinctive stratigraphic units.[11] Also, felsic volcanic rocks are distributed across long distances because of their extensive deposition.[7][17][18][41] However, the rock sequences of greenstone belts are commonly obscured by later deformation, such as regional folding or intrusion of granitoids.[17] By identifying these felsic sequences and dating their time of formation, stratigraphic units of different locations can be correlated despite the obstacles or discontinuity between felsic volcanic units.[17][41]

Timing of volcanism

The geochronology of Archean events strongly relies on U-Pb dating[11][26] and Lu-Hf dating.[42] Since mafic rocks (contain low silica content, such as basalt) are lack of zircon, only the age of felsic rocks can be dated among the volcanic rocks in greenstone belts.[14] As felsic volcanic rocks are episodically deposited in between mafic layers, the age range of a particular mafic layer can be constrained by the upper and lower felsic volcanic layers.[11] Thus the time of occurrence and the duration of volcanic episodes can be revealed.[17]

Relationships between Archean felsic volcanic rocks and granitoids

From TTG to GMS granitoids

Two plutonic, igneous rock suites form 50% of Archean cratons.[6] They are (1) Tonalite-trondhjemite-granodiorite (TTG) suites and (2) Granite-Monzonite-Syenite (GMS) suites in chronological order.[6] They are magma chambers that later formed the volcanics on the Earth's surface by volcanic eruption.[30] Later they intruded the supracrustal rocks of similar age and composition in the Archean.[19] The uprising magma bodies deformed the surface greenstone belt on a cratonic scale.[5]

Table 3. Comparison between 2 common Archean Granitoids[9][43]
Relative age Granitoid Important mineral present Magma origin
Older (1st granitoid) Tonalite-trondhjemite-granodiorite (TTG) Na-rich plagioclase + garnet + amphibole hydrated mafic crust
Younger (2nd granitoid) Granite-Monzonite-Syenite (GMS) K-feldspar felsic crust

The two kinds of granitoids have different magma origins: (a) melting of water-rich mafic materials formed older sodium-rich TTG and (b) melting of felsic materials (e.g. TTG and/or sediments[44]) formed younger potassium-rich GMS (see Table 3).[9][43] They imply gradual chemical changes in the magma and the Earth's crust.[9]

Conflicting compositions

Records of Archean felsic volcanic rocks shows a peculiar trend. The eruption of felsic volcanic rocks and plutonic activities in Archean are largely synchronised as show in overlapping zircon ages.[9] On contrary, the chemical compositions of some felsic volcanic rocks are similar to that of GMS but they are much older than GMS.[9] For example, a GMS-like rhyolite unit in the Abitibi Greenstone Belt (abnormally more enriched in potassium and heavy rare-earth elements than other Archean felsic volcanic rocks) has no plutonic equivalent in the same period.[12][30] The composition of felsic volcanic rocks are being altered concurrently with shifting granitoid composition.[9]

Fig 5. Possible relationship 1 of Archean felsic volcanic rocks and granitoids. GMS may have intruded the crust at a very shallow depth, and later TTG intruded.[9]

Possible relationships

The older GMS-like felsic volcanic rocks formed with similar age of TTG has two implications:[9]

  1. GMS may have intruded the crust and GMS-like volcanics at a very shallow depth. Later, intense erosion rips up all GMS suites and deposited at a proximal distance. If this is true, then GMS and TTG intruded the crust together at the same time. No solid evidence is present yet but the irregular geochemical fingerprints may link both to TTG or GMS.[9]
  2. GMS is concentrated at the upper crust and TTG at deeper intermediate crust. Later, GMS as well as GMS-like volcanics are eroded and deposit as sediments. The detrital zircons may show a range of mixed GMS and TTG geochemical signature.[9]

Limitation

Fig 6. Possible relationship 2 of Archean felsic volcanic rocks and granitoids. GMS and TTG may have intruded the crust at the same time. Yet, GMS was concentrated at the upper crust and TTG at deeper intermediate crust.[9]

Revealing the relationship between Archean felsic volcanic rocks and the granitoids may be difficult. It is because weathering alters the geochemical signatures of the felsic rocks above the Earth's surface.[45] The earliest weathering record can be traced back to 3.8 Ga during Eoarchean.[45] Potassium is enriched but sodium is depleted in these weathered felsic rocks.[45] Altered feldspars in the rocks may result in such anomalous signatures.[45]

See also

References

  1. 1 2 Giles, Christopher William (1980). A comparative study of Archaean and Proterozoic felsic volcanic associations in Southern Australia / by Chris W. Giles (Thesis).
  2. ↑ Cohen, K.M., Finney, S.M., Gibbard, P.L., Fan, J.-X. (2013). The ICS International Chronostratigraphic Chart. Episodes 36, 199-204.
  3. 1 2 3 4 5 6 Le Bas, M. J.; Le Maitre, R. W.; Streckeisen, A.; Zanettin, B. (1986). "A Chemical Classification of Volcanic Rocks Based on the Total Alkali-Silica Diagram". Journal of Petrology. 27 (3): 745–750. Bibcode:1986JPet...27..745B. doi:10.1093/petrology/27.3.745. ISSN 0022-3530.
  4. ↑ Braterman, Paul S. "How Science Figured Out the Age of Earth". Scientific American. Retrieved 2018-12-02.
  5. 1 2 3 4 5 6 Halla, J; Whitehouse, M. J.; Ahmad, T.; Bagai, Z. (2017). "Archaean granitoids: an overview and significance from a tectonic perspective". Geological Society, London, Special Publications. 449 (1): 1–18. Bibcode:2017GSLSP.449....1H. doi:10.1144/SP449.10. ISSN 0305-8719.
  6. 1 2 3 4 5 6 7 8 9 10 11 12 13 14 Condie, Kent C. (1993). "Chemical composition and evolution of the upper continental crust: Contrasting results from surface samples and shales". Chemical Geology. 104 (1–4): 1–37. Bibcode:1993ChGeo.104....1C. doi:10.1016/0009-2541(93)90140-e. hdl:10068/310317. ISSN 0009-2541.
  7. 1 2 3 4 5 6 7 8 9 10 11 12 13 de Rosen-Spence, Andrée F.; Provost, Gilles; Dimroth, Erich; Gochnauer, Karen; Owen, Victor (1980). "Archean subaqueous felsic flows, Rouyn-Noranda, Quebec, Canada, and their Quarternary [sic] equivalents". Precambrian Research. 12 (1–4): 43–77. Bibcode:1980PreR...12...43D. doi:10.1016/0301-9268(80)90023-6. ISSN 0301-9268.
  8. 1 2 Szilas, Kristoffer (2018). "A Geochemical Overview of Mid-Archaean Metavolcanic Rocks from Southwest Greenland". Geosciences. 8 (7): 266. Bibcode:2018Geosc...8..266S. doi:10.3390/geosciences8070266. ISSN 2076-3263.
  9. 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 Agangi, Andrea; Hofmann, Axel; Elburg, Marlina A. (2018). "A review of Palaeoarchaean felsic volcanism in the eastern Kaapvaal craton: Linking plutonic and volcanic records". Geoscience Frontiers. 9 (3): 667–688. doi:10.1016/j.gsf.2017.08.003. ISSN 1674-9871.
  10. 1 2 Van Kranendonk, Martin J.; Hugh Smithies, R.; Hickman, Arthur H.; Wingate, Michael T.D.; Bodorkos, Simon (2010). "Evidence for Mesoarchean (≈3.2Ga) rifting of the Pilbara Craton: The missing link in an early Precambrian Wilson cycle". Precambrian Research. 177 (1–2): 145–161. Bibcode:2010PreR..177..145V. doi:10.1016/j.precamres.2009.11.007. ISSN 0301-9268.
  11. 1 2 3 4 5 6 7 Thorpe, R.I.; Hickman, A.H.; Davis, D.W.; Mortensen, J.K.; Trendall, A.F. (1992). "U-Pb zircon geochronology of Archaean felsic units in the Marble Bar region, Pilbara Craton, Western Australia". Precambrian Research. 56 (3–4): 169–189. Bibcode:1992PreR...56..169T. doi:10.1016/0301-9268(92)90100-3. ISSN 0301-9268.
  12. 1 2 Paradis, Suzanne; Ludden, John; Gélinas, Léopold (1988). "Evidence for contrasting compositional spectra in comagmatic intrusive and extrusive rocks of the late Archean Blake River Group, Abitibi, Quebec". Canadian Journal of Earth Sciences. 25 (1): 134–144. Bibcode:1988CaJES..25..134P. doi:10.1139/e88-013. ISSN 0008-4077.
  13. 1 2 W., Bleeker; W., Davis, B. (2004). "What is a craton? How many are there? How do they relate? And how did they form?". AGU Spring Meeting Abstracts. 2004: T41C–01. Bibcode:2004AGUSM.T41C..01B.{{cite journal}}: CS1 maint: multiple names: authors list (link)
  14. 1 2 3 4 Sylvester, P. J.; Harper, G. D.; Byerly, G. R.; Thurston, P. C. (1997). "Volcanic Aspects". In De Wit, Maarten J.; Ashwal, Lewis D. (eds.). Greenstone belts. Oxford: Clarendon Press. pp. 55–90. ISBN 978-0198540564. OCLC 33104147.
  15. 1 2 Manikyamba, C.; Ganguly, Sohini; Santosh, M.; Subramanyam, K.S.V. (2017). "Volcano-sedimentary and metallogenic records of the Dharwar greenstone terranes, India: Window to Archean plate tectonics, continent growth, and mineral endowment". Gondwana Research. 50: 38–66. Bibcode:2017GondR..50...38M. doi:10.1016/j.gr.2017.06.005. ISSN 1342-937X.
  16. ↑ Johnson, Tim E.; Brown, Michael; Goodenough, Kathryn M.; Clark, Chris; Kinny, Peter D.; White, Richard W. (2016). "Subduction or sagduction? Ambiguity in constraining the origin of ultramafic–mafic bodies in the Archean crust of NW Scotland" (PDF). Precambrian Research. 283: 89–105. Bibcode:2016PreR..283...89J. doi:10.1016/j.precamres.2016.07.013. hdl:20.500.11937/9924. ISSN 0301-9268.
  17. 1 2 3 4 5 6 7 8 9 10 11 DiMarco, Michael J.; Lowe, Donald R. (1989). "Stratigraphy and sedimentology of an early Archean felsic volcanic sequence, eastern Pilbara Block, Western Australia, with special reference to the Duffer Formation and implications for crustal evolution". Precambrian Research. 44 (2): 147–169. Bibcode:1989PreR...44..147D. doi:10.1016/0301-9268(89)90080-6. ISSN 0301-9268.
  18. 1 2 3 Barley, M.E. (1993). "Volcanic, sedimentary and tectonostratigraphic environments of the ≈3.46 Ga Warrawoona Megasequence: a review". Precambrian Research. 60 (1–4): 47–67. Bibcode:1993PreR...60...47B. doi:10.1016/0301-9268(93)90044-3. ISSN 0301-9268.
  19. 1 2 Kerrich, Robert; Polat, Ali (2006). "Archean greenstone-tonalite duality: Thermochemical mantle convection models or plate tectonics in the early Earth global dynamics?". Tectonophysics. 415 (1–4): 141–165. Bibcode:2006Tectp.415..141K. doi:10.1016/j.tecto.2005.12.004. ISSN 0040-1951.
  20. ↑ V., Cas, R. A.F Wright, J. (1996). Volcanic successions modern and ancient: a geological approach to processes, products and successions. Chapman and Hall. ISBN 978-0412446405. OCLC 961300385.{{cite book}}: CS1 maint: multiple names: authors list (link)
  21. ↑ Nelson, David R. (2001). "An assessment of the determination of depositional ages for precambrian clastic sedimentary rocks by U–Pb dating of detrital zircons". Sedimentary Geology. 141–142: 37–60. Bibcode:2001SedG..141...37N. doi:10.1016/s0037-0738(01)00067-7. ISSN 0037-0738.
  22. ↑ Hallberg, J.A.; Johnston, C.; Bye, S.M. (1976). "The Archaean Marda igneous complex, Western Australia". Precambrian Research. 3 (2): 111–136. Bibcode:1976PreR....3..111H. doi:10.1016/0301-9268(76)90029-2. ISSN 0301-9268.
  23. ↑ Nelson, D. R. (2001). 168961: welded tuffaceous rhyolite, Marda Tank. Geochronology Record, 195. Geological Survey of Western Australia.
  24. ↑ Jayananda, M.; Peucat, J.-J.; Chardon, D.; Rao, B. Krishna; Fanning, C.M.; Corfu, F. (2013). "Neoarchean greenstone volcanism and continental growth, Dharwar craton, southern India: Constraints from SIMS U–Pb zircon geochronology and Nd isotopes". Precambrian Research. 227: 55–76. Bibcode:2013PreR..227...55J. doi:10.1016/j.precamres.2012.05.002. ISSN 0301-9268.
  25. 1 2 Vaasjoki, M., Sorjonen-Ward, P. and Lavikainen, S. (1993). U-Pb age delerminations and sulfide Pb-Pb Characteristics from the late Archean Hattu Schist Belt, Ilomantsi, eastern Finland. Geological Survev of Finland, Special Paper 17, 103-131
  26. 1 2 KAMBER, B; WHITEHOUSE, M; BOLHAR, R; MOORBATH, S (2005). "Volcanic resurfacing and the early terrestrial crust: Zircon U–Pb and REE constraints from the Isua Greenstone Belt, southern West Greenland". Earth and Planetary Science Letters. 240 (2): 276–290. Bibcode:2005E&PSL.240..276K. doi:10.1016/j.epsl.2005.09.037. ISSN 0012-821X.
  27. 1 2 Nutman, Allen P.; Bennett, Vickie C.; Friend, Clark R.L.; Rosing, Minik T. (1997). "~ 3710 and ⪖ 3790 Ma volcanic sequences in the Isua (Greenland) supracrustal belt; structural and Nd isotope implications". Chemical Geology. 141 (3–4): 271–287. Bibcode:1997ChGeo.141..271N. doi:10.1016/s0009-2541(97)00084-3. ISSN 0009-2541.
  28. 1 2 Mortensen, J. K.; Thorpe, R. I.; Padgham, W. A.; Keng, J. E.; Davis, W. J. (1988). "U-Pb zircon ages for felsic volcanism in Slave Porvince, N.W.T." Radiogenic Age and Isotopic Studies: Report 2. Paper No. 88-2: 85–95. doi:10.4095/126606.
  29. ↑ Goodwin, A.M.; Smith, I.E.M. (1980). "Chemical discontinuities in Archean metavolcanic terrains and the development of Archean crust". Precambrian Research. 10 (3–4): 301–311. Bibcode:1980PreR...10..301G. doi:10.1016/0301-9268(80)90016-9. ISSN 0301-9268.
  30. 1 2 3 Lesher, C. M.; Goodwin, A. M.; Campbell, I. H.; Gorton, M. P. (1986). "Trace-element geochemistry of ore-associated and barren, felsic metavolcanic rocks in the Superior Province, Canada". Canadian Journal of Earth Sciences. 23 (2): 222–237. Bibcode:1986CaJES..23..222L. doi:10.1139/e86-025. ISSN 0008-4077.
  31. ↑ Ayer, J.; Amelin, Y.; Corfu, F.; Kamo, S.; Ketchum, J.; Kwok, K.; Trowell, N. (2002). "Evolution of the southern Abitibi greenstone belt based on U–Pb geochronology: autochthonous volcanic construction followed by plutonism, regional deformation and sedimentation". Precambrian Research. 115 (1–4): 63–95. Bibcode:2002PreR..115...63A. doi:10.1016/s0301-9268(02)00006-2. ISSN 0301-9268.
  32. 1 2 Sylvester, Paul J.; Attoh, Kodjo; Schulz, Klaus J. (1987). "Tectonic setting of late Archean bimodal volcanism in the Michipicoten (Wawa) greenstone belt, Ontario". Canadian Journal of Earth Sciences. 24 (6): 1120–1134. Bibcode:1987CaJES..24.1120S. doi:10.1139/e87-109. ISSN 0008-4077.
  33. ↑ Turek, A.; Smith, Patrick E.; Schmus, W. R. Van (1982). "Rb–Sr and U–Pb ages of volcanism and granite emplacement in the Michipicoten belt—Wawa, Ontario". Canadian Journal of Earth Sciences. 19 (8): 1608–1626. Bibcode:1982CaJES..19.1608T. doi:10.1139/e82-138. ISSN 0008-4077.
  34. 1 2 Baldock, J.W.; Evans, J.A. (1988). "Constraints on the age of the Bulawayan group metavolcanic sequence, Harare Greenstone Belt, Zimbabwe". Journal of African Earth Sciences (and the Middle East). 7 (5–6): 795–804. Bibcode:1988JAfES...7..795B. doi:10.1016/0899-5362(88)90022-x. ISSN 0899-5362.
  35. 1 2 Krüner, Alfred; Byerly, Gary R.; Lowe, Donald R. (1991). "Chronology of early Archaean granite-greenstone evolution in the Barberton Mountain Land, South Africa, based on precise dating by single zircon evaporation". Earth and Planetary Science Letters. 103 (1–4): 41–54. Bibcode:1991E&PSL.103...41K. doi:10.1016/0012-821x(91)90148-b. ISSN 0012-821X. PMID 11538384.
  36. 1 2 3 4 5 6 7 8 9 Morris, P. A.; Barnes, S. J.; Hill, R. E. T. (1993). Eruptive environment and geochemistry of Archaean ultramafic, mafic and felsic volcanic rocks of the eastern Yilgarn Craton : IAVCEI, Canberra 1993 : excursion guide. Australia: Australian Geological Survey Organisation. p. 6. ISBN 978-0642196637. OCLC 221544061.
  37. 1 2 3 4 5 6 7 Thurston, P. C. (1980). "Subaerial volcanism in the Archean Uchi-Confederation volcanic belt". Precambrian Research. 12 (1–4): 79–98. Bibcode:1980PreR...12...79T. doi:10.1016/0301-9268(80)90024-8. ISSN 0301-9268.
  38. ↑ Watson, E. Bruce (1979). "Zircon saturation in felsic liquids: Experimental results and applications to trace element geochemistry". Contributions to Mineralogy and Petrology. 70 (4): 407–419. Bibcode:1979CoMP...70..407W. doi:10.1007/bf00371047. ISSN 0010-7999. S2CID 128813711.
  39. 1 2 3 Mueller, Wulf; White, James D.L. (1992). "Felsic fire-fountaining beneath Archean seas: pyroclastic deposits of the 2730 Ma Hunter Mine Group, Quebec, Canada". Journal of Volcanology and Geothermal Research. 54 (1–2): 117–134. Bibcode:1992JVGR...54..117M. doi:10.1016/0377-0273(92)90118-w. ISSN 0377-0273.
  40. 1 2 3 Yamagishi, Hiromitsu; Dimroth, Erich (1985). "A comparison of Miocene and Archean rhyolite hyaloclastites: Evidence for a hot and fluid rhyolite lava". Journal of Volcanology and Geothermal Research. 23 (3–4): 337–355. Bibcode:1985JVGR...23..337Y. doi:10.1016/0377-0273(85)90040-x. ISSN 0377-0273.
  41. 1 2 3 4 5 6 Lambert, M B; Burbidge, G; Jefferson, C W; Beaumont-smith, C; Lustwerk, R (1990). "Stratigraphy, Facies and Structure in Volcanic and Sedimentary Rocks of the Archean Back River Volcanic Complex, N.w.t." Current Research, Part C, Geological Survey of Canada, Paper 90-IC: 151–165. doi:10.4095/131253.
  42. ↑ Liu, Xiao-Chi; Wu, Yuan-Bao; Fisher, Christopher M.; Hanchar, John M.; Beranek, Luke; Gao, Shan; Wang, Hao (2016). "Tracing crustal evolution by U-Th-Pb, Sm-Nd, and Lu-Hf isotopes in detrital monazite and zircon from modern rivers". Geology. 45 (2): 103–106. Bibcode:2017Geo....45..103L. doi:10.1130/g38720.1. ISSN 0091-7613.
  43. 1 2 Lowe, Donald R.; Byerly, Gary R. (2007), "Chapter 5.3 An Overview of the Geology of the Barberton Greenstone Belt and Vicinity: Implications for Early Crustal Development", Earth's Oldest Rocks, Elsevier, pp. 481–526, doi:10.1016/s0166-2635(07)15053-2, ISBN 9780444528100
  44. ↑ Watkins, J. M.; Clemens, J. D.; Treloar, P. J. (2007-03-06). "Archaean TTGs as sources of younger granitic magmas: melting of sodic metatonalites at 0.6–1.2 GPa". Contributions to Mineralogy and Petrology. 154 (1): 91–110. Bibcode:2007CoMP..154...91W. doi:10.1007/s00410-007-0181-0. ISSN 0010-7999. S2CID 131343174.
  45. 1 2 3 4 Nutman, Allen P.; Bennett, Vickie C.; Chivas, Allan R.; Friend, Clark R.L.; Liu, Xiao-Ming; Dux, Florian W. (2015). "3806Ma Isua rhyolites and dacites affected by low temperature Eoarchaean surficial alteration: Earth's earliest weathering". Precambrian Research. 268: 323–338. Bibcode:2015PreR..268..323N. doi:10.1016/j.precamres.2015.07.014. ISSN 0301-9268.
This article is issued from Wikipedia. The text is licensed under Creative Commons - Attribution - Sharealike. Additional terms may apply for the media files.