| Autor: |
Bo Johanson, Raimo Lahtinen, Jarmo Kohonen, Yann Lahaye, Hannu Huhma, Asko Kontinen |
| Rok vydání: |
2013 |
| Předmět: |
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| Zdroj: |
Lithos. :86-103 |
| ISSN: |
0024-4937 |
| DOI: |
10.1016/j.lithos.2013.05.003 |
| Popis: |
The western margin of the Karelia Province of the Fennoscandian Shield consists of Archean crust covered by remnants of Paleoproterozoic (c. 2.5–1.9 Ga) metasedimentary rocks. The study area in the eastern part of the margin shows 2.3–2.1 Ga cratonic sedimentation followed by 2.1–2.05 Ga rift sedimentation and c. 1.91–1.92 Ga foredeep to foreland sedimentation related to continent–arc/continent collision. Extreme LREE mobility (loss up > 95% of La) is recorded by many samples from these units. Monazite, bastnasite and, in some cases, allanite have been the prealteration LREE host phases in the LREE depleted samples. Monazite was altered to Th-silicates with variable loss of the LREE, the remaining part of which was incorporated in Th-poor monazite. The depositional age of the sedimentary units was studied by dating (LA-MC-ICPMS) detrital zircon grains, and the age of LREE mobility by dating monazite and xenotime and by whole-rock Sm–Nd modeling. The maximum deposition age of the foredeep to foreland basin is 1.91–1.92 Ga based on detrital zircon data and the minimum age of the main foliation in the study area is 1.87–1.86 Ga based on the younger age limit of late-to post-tectonic xenotime and the ages of few probable metamorphic zircons. Coeval bastnasite, with xenotime in a LREE enriched sample, suggests that this was also one important stage of LREE mobility. Monazite crystallizations have occurred 1.76–1.78 Ga ago while the Rb–Sr whole rock data suggest that the closure of this isotope system took place 1732 ± 21 Ma ago. The Sm–Nd modeling gives ages at 0.4–1.0 Ga for LREE depletion. The Sm–Nd age of 412 ± 27 Ma can be considered as the age of the latest major LREE depletion event. We propose that alkali-bearing oxidizing fluids started to form in the cratonic sequences due to diagenetic reactions maybe as early as 2.3–2.1 Ga. Alkalinity of fluids was later increased by interaction with alkaline 2.05 Ga source materials before and during the c. 1.91–1.92 Ga foredeep to foreland basin stage. Basin inversion and metamorphic crystallization occurred at 1.91–1.87 Ga. Episodes of fluid migration at 1.78–1.73 Ga and afterwards were focused along fracture zones and in microfracture networks. The 0.4 Ga stage is the most prominent of the |
| Databáze: |
OpenAIRE |
| Externí odkaz: |
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