Source of Analytical Data on Main Faults and Faulted Areas with Seismic Potential
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dbz:diendorf-boskovice_fault [2020/05/29 16:02] petrs |
dbz:diendorf-boskovice_fault [2024/05/29 16:39] (current) petrs [Diendorf - Boskovice fault system] |
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- | * A cluster of epicentres of weak earthquakes between the towns of Langenlois, Gfohl, Ybbs an der Donau and Melk (see **[[dbz: | + | * A cluster of epicentres of weak earthquakes between the towns of Langenlois, Gfohl, Ybbs an der Donau and Melk (see **[[dbz: |
* To the north of Langenlois the low number and magnitude of historical and instrumental earthquakes and their low spatial correlation with fault line do not allow affiliation of seismicity to any known structures. | * To the north of Langenlois the low number and magnitude of historical and instrumental earthquakes and their low spatial correlation with fault line do not allow affiliation of seismicity to any known structures. | ||
* Rare local observations of soft sediment deformation structures are interpreted as due to paleoearthquakes with minimum intensity of 6-7° (sites **[[dbz: | * Rare local observations of soft sediment deformation structures are interpreted as due to paleoearthquakes with minimum intensity of 6-7° (sites **[[dbz: | ||
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* Results of some long-term geodetic measurements in the region were interpreted as tectonic deformation in several studies (Pospíšil et al. 2009, 2010, 2012; Roštínský et al. 2013). However, editor of this text is skeptical to interpretation of these observations as due to tectonic strain because: | * Results of some long-term geodetic measurements in the region were interpreted as tectonic deformation in several studies (Pospíšil et al. 2009, 2010, 2012; Roštínský et al. 2013). However, editor of this text is skeptical to interpretation of these observations as due to tectonic strain because: | ||
- | - the reported strain rates are too large (10< | + | - the reported strain |
- the locally observed geological records rule out that such deformation at BF could have been operative on a long-term scale during Quaternary; | - the locally observed geological records rule out that such deformation at BF could have been operative on a long-term scale during Quaternary; | ||
- | - the non-tectonic deformation (climatic/ | + | - the non-tectonic deformation (climatic/ |
:!: **Basing on this local evidence the fault activity is currently evaluated in a following way:** | :!: **Basing on this local evidence the fault activity is currently evaluated in a following way:** | ||
*In the southern part of DBF, the sections DF_1 to BF_2 are ranked **class 3**, i.e. assumed or admitted to be active but without direct evidence. Quaternary slip rate at fault sections north of DF_3 is assumed very low (<0.01 mm/y). Southern sections may later be ranked class 1 (demonstrably active) when new earthquake data (better location, focal mechanism) bring clear evidence. | *In the southern part of DBF, the sections DF_1 to BF_2 are ranked **class 3**, i.e. assumed or admitted to be active but without direct evidence. Quaternary slip rate at fault sections north of DF_3 is assumed very low (<0.01 mm/y). Southern sections may later be ranked class 1 (demonstrably active) when new earthquake data (better location, focal mechanism) bring clear evidence. | ||
*In the northern part of DBF, the sections BF_3 to BF_ 17 are ranked **class 4**, i.e. assumed or demonstrated to be inactive. | *In the northern part of DBF, the sections BF_3 to BF_ 17 are ranked **class 4**, i.e. assumed or demonstrated to be inactive. | ||
- | On a theoretical basis, the evaluation of similarly oriented | + | On a theoretical basis, the evaluation of similarly oriented sections |
-expected northward decrease of rate of stress build-up (and hence crustal strain rate), and | -expected northward decrease of rate of stress build-up (and hence crustal strain rate), and | ||
-expected northward decrease of slip potential due to rotation of stress orientation near junction of the Alpine and the West-European stress domains. | -expected northward decrease of slip potential due to rotation of stress orientation near junction of the Alpine and the West-European stress domains. | ||
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===== Related local evidence ===== | ===== Related local evidence ===== | ||
- | //(See layer //**Local evidence**// | + | //(See layer //**Local evidence**// |
====Schönbühel a.d. Donau: Cross-structure==== | ====Schönbühel a.d. Donau: Cross-structure==== |