Source of Analytical Data on Main Faults and Faulted Areas with Seismic Potential
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- | ====== Diendorf - Boskovice Fault Zone (DBZ) ====== | ||
- | **Structure ID:** DBZ\\ | ||
- | **Fault Section IDs:** DIE_1-8; BB_1-17; WEI_1-3\\ | ||
- | **Related terms:** Diendorf fault (//ger//: Diendorfer Störung), Boskovice Graben fault (//cze//: okrajový zlom boskovické brázdy), Weitzendorf fault (//ger//: Weitzendorfer Störung;// cze//: weitzendorfský zlom)\\ | ||
- | **Editor:** Petr Špaček\\ | ||
- | **Last update:** 17.7.2019 | ||
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- | ====== Diendorf - Boskovice Fault Zone (DBZ) ====== | ||
- | |||
- | **Structure ID:** DBZ\\ | ||
- | **Fault Section IDs:** DIE_1-8; BB_1-17; WEI_1-3\\ | ||
- | **Related terms:** Diendorf fault (//ger//: Diendorfer Störung), Boskovice Graben fault (//cze//: okrajový zlom boskovické brázdy), Weitzendorf fault (//ger//: Weitzendorfer Störung;// cze//: weitzendorfský zlom)\\ | ||
- | **Editor:** Petr Špaček\\ | ||
- | **Last update:** 17.7.2019\\ | ||
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- | //Patience please! This map may load slowly... //=) | ||
- | {{url> | ||
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- | ===== General description ===== | ||
- | Over 200 km long fault structure running in the general NE-SW direction from the Alpine thrust front in Austria to the transverse faults of the Haná fault zone in the Czech Republic. | ||
- | It is formed by two major faults: the //Diendorf fault// (DF) to the south and the eastern marginal fault of the Boskovice half-graben, | ||
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- | ----- | ||
- | ===== Pre-Quaternary evolution ===== | ||
- | *Both DF and BF have been considered major structures with partly shared evolution since the early geological research (e.g. Suess 1926, Shermann 1966, Jaroš & Mísař 1967, Matura 1976, Figdor and Scheidegger 1977). | ||
- | *DBZ corresponds with the surface trace of Variscan terrane boundary between Brunovistulicum and Moldanubicum. It also correlates with western termination of the Lower Carboniferous flysch (comp. Melichar 1995), i.e. the root zone of Variscan externide nappes. | ||
- | *Significant synsedimentary slip with vertical component (>1600m) took place at BF during Upper Carboniferous-Permian and produced the Boskovice half graben with StephanianC-Autunian sedimentary fill. Fans of coarse Rokytná conglomerates are associated with BF-bounded eastern margin of the graben. This faulting is assumed to be of normal geometry, related to orogen gravitational collaps (e.g. Jaroš 1961a, Malý 1993, Jaroš and Malý 2001). Locally, dikes and sills of basalt-andesite (sub-)volcanics were observed to penetrate the sediments (e.g. Přichystal 1994). Relic of Permian sediments near Zöbing suggests that analogical subsidence may have been associated with northern/ | ||
- | *Locally observed steep reverse geometry at BF (e.g. Suess 1907, Zapletal 1924, Jaroš 1958, Jaroš 1962) and the intra-basin deformation structures (reverse faults and long wavelegth folds, Jaroš a Malý 2001) indicate post-Permian compression or transpression. The age of this phase is unknown and likely pre-Cretaceous as no corresponding structures were observed in Cretaceous strata (Zapletal 1924). | ||
- | *At DF, strike-slip geometry is accentuated with cumulative post-Variscan (post-collision) left-lateral slip estimated in the range 25-70 km (as inferred from offset of crystalline bodies with mutual affinity; Schermann 1966; Matura 1976; Figdor and Scheidegger 1977). | ||
- | *Post-Lower Miocene slip is indicated by sharp, steeply dipping contacts of Lower Miocene (Eggenburgian, | ||
- | *Transverse fault-bounded grabens with Cretaceous fill disrupt the BF in the north (Boskovice and Valchov grabens). These structures rule out locally the significant strike-slip displacement postdating their formation during or before early Middle Miocene (likely Paleogene). | ||
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- | ---- | ||
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- | |||
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- | ===== Fault structure and dip ===== | ||
- | At **//shallow levels//** the dip is always steep to vertical in both BF and DF. At **//general scale//** I model the fault as a plane uniformly dipping 75° to the northwest. The azimuth of the fault trace ranges between <20° and >45°. | ||
- | |||
- | *At BF the dip directions to the west (Zapletal 1924, 1929, Polák 1959) or east (Suess 1907; Zapletal 1924; Jaroš 1958) were observed. In case of the latter, observations of overturned Permian strata were reported from the fault neighbourhood (Jaroš 1958). In the Miroslav horst and further south (BB_1, 2) a steep western dip is indicated by natural outcrop in an erosional gully, observations in trenches and shallow geophysical profiles ([[diendorf-boskovice_fault# | ||
- | *In the commonly adopted models of the Boskovice graben (Jaroš 1961a; Malý 1993; Jaroš & Malý 2001) the BF is shown as a steeply east-dipping fault. However, it must be stressed that clear evidence for deeper geometry is missing and these models should be taken as the authors' | ||
- | *The importance of thrust component repeated in literature seems to me overrated. Local variations observed are assumed to prevail near the surface, they could partly represent flower structures related to the expected prevailing strike-slip kinematics of the post-Stephanian fault displacements. | ||
- | *At DF, rare observations were reported from excavation near Maissau (DIE_4; Posch-Trotzmüller and Peresson 2012) and [[diendorf-boskovice_fault# | ||
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- | The **//fault core//**, where observed, is often built by several meter wide mélange with fragments or bodies of limestones and greywackes (sections BB_2 to BB_14; Špaček et al. 2002) locally containing dark colored clays. Surface observations near Zöbing (vineyards north of Kammern) suggest that the strongly deformed zone may be >10 m broad there. Similar width is expected elsewhere in Permian and crystalline rocks. In trench near Hostěradice ([[diendorf-boskovice_fault# | ||
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- | A <20 to 250 m wide **//process zone//** of the main fault is documented in Early Miocene sediments in a large part of BB_1 section by EM conductivity mapping (Fojt and Špaček, unpublished) and by observations in aerial photographs. | ||
- | |||
- | **// | ||
- | Multiple parallel and oblique faults (observed and assumed) located in a broader zone (within up to 10 km to both sides of the BF and DF) indicates distributed faulting reflecting the complexity of long term evolution in different stress fields. | ||
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- | ---- | ||
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- | ===== Cross structures and Segmentation ===== | ||
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- | I am just finishing this section! FIXME | ||
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- | ---- | ||
- | ===== Scarp morphology ===== | ||
- | Surface morphology at the fault trace varies significantly, | ||
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- | ***//Well developed linear fault scarp//** is observed where Lower Miocene sediments were juxtaposed to crystalline rocks due to the fault slip and were later partly or entirely denudated (fault sections DIE_4, BB_2 and very likely DIE_1.2 to 1.4). The scarp of fault section BB_2 exhibits number of gullies with disequilibrium profiles breaking at the fault line, suggesting fast fall of erosional base (which I interpret as due to fast erosional exhumation of the old fault scarp; see [[diendorf-boskovice_fault# | ||
- | ***//Eroded scarp//** is common in parts with relics of Middle Miocene sediments on bedrock (sections BB_3, 5, 9, 10.1, 16 to 17) and with increased local river erosion (sections DIE_1.5 and BB_7-8). | ||
- | ***// | ||
- | *In parts where Mesozoic and Tertiary sediments are present at both sides of the fault line the scarp is **// | ||
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- | ---- | ||
- | ===== Seismicity ===== | ||
- | To be revisited after completion of earthquake catalogue. FIXME | ||
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- | ---- | ||
- | ===== Fault activity ===== | ||
- | ====Tertiary==== | ||
- | *The post-Eggenburgian/ | ||
- | *More precise time constraint of this phase of activity is problematic as a sound evidence from relics of Karpatian and early Badenian (late Burdigalian to early Langhian) is not available and younger Tertiary sediments are missing regionally. I assume, basing on a regional tectonic model and some local observations, | ||
- | *Significant large scale post-Badenian strike-slip at DBZ is :!: counterevidenced by [[diendorf-boskovice_fault# | ||
- | *Termination of the early Miocene strike-slip phase at BF is further affirmed by development of a system of small-amplitude faults with average NW-SE strike. On the DF such faults are not present in geological maps, however, they are clearly indicated in relief (e.g. near Schönbühel a.d. Donau, [[diendorf-boskovice_fault# | ||
- | *In the Dyje basin crossing the DBZ in segments DIE_6-8, post-Lower Miocene faulting is indicated by apparent strata cutoffs at several ERT profiles crossing some major morpholineaments in the basin (Špaček et al. 2016). Steeply dipping faults of WNW-WSE to NNW-SSE strike were described from near Stošíkovice na Louce ([[diendorf-boskovice_fault# | ||
- | *Magnitude and timing of dip-slip component is difficult to constrain at most fault sections as the data on well dated stratigraphic bases of Tertiary deposits on the fault are insufficient. | ||
- | *At fault sections BB_1 ([[diendorf-boskovice_fault# | ||
- | |||
- | ====Quaternary==== | ||
- | Following evidence is considered in the assessment of Quaternary activity: | ||
- | ***// | ||
- | * The sealing strata observed in detail in trenches in sections BB_1, BB_2 ([[diendorf-boskovice_fault# | ||
- | * Termination of older strata in Kadov trench on a fault plane allow considering slip with min. vertical component of 2 m in 100 - <23ky time window, however, the non-tectonic model of origin of this structure is preferred (see references for site [[diendorf-boskovice_fault# | ||
- | * Sealing strata in a trench at DIE_7 ([[diendorf-boskovice_fault# | ||
- | * Vertically non-displaced base of high terrace and its relics mapped in detail in section BB_4 ([[diendorf-boskovice_fault# | ||
- | * Likewise, vertically non-displaced base of high terrace between villages of Dyje, Lechovice, Božice and Hodonice (" | ||
- | |||
- | ***// | ||
- | * Total absence of systematic horizontal offsets of geomorphological features (or any other piercing lines), including the deeply incised cross-cutting valeys in hard rocks (mainly BB_2, 4, 8, 12), brings :!: evidence against significant active horizontal slip since river incision in Middle Pleistocene. | ||
- | * The fault [[diendorf-boskovice_fault# | ||
- | |||
- | ***// | ||
- | * A cluster of epicentres of weak earthquakes (both historical and modern) between the towns of Langenlois, Gfohl, Ybbs an der Donau and Melk suggest possible connection with southern Diendorf fault (sections DIE_1, 2, 5 and 6). However, the causal links are unclear as the cluster shape (possibly affected by poor accuracy of location) allows for different conclusions. In the area of southern Bohemian Massif the increased seismicity seems to be characteristic. Some observations suggest that unmapped NW-SE striking faults may be responsible for at least part of these earthquakes (see site [[diendorf-boskovice_fault# | ||
- | * 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 [[diendorf-boskovice_fault# | ||
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- | :!: **Basing on this local evidence the fault activity is currently evaluated in a following way:** | ||
- | *In the southern part of DBZ, the sections DIE_1 to BB_2 are ranked **class 3**, i.e. assumed or admitted to be active. Quaternary slip rate at fault sections north of DIE_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 DBZ, the sections BB_3 to BB_ 17 are ranked **class 4**, i.e. assumed or demonstrated to be inactive. | ||
- | On a theoretical basis, the evaluation of similarly oriented fault sections by different ranks may be justified by: | ||
- | -expected northward decrease of rate of stress buildup (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. | ||
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- | ---- | ||
- | |||
- | ===== Related local evidence ===== | ||
- | |||
- | //(See layer //**Local evidence**// | ||
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- | ====Schönbühel a.d. Donau: Cross-structure==== | ||
- | **evi_ID:** SCHO_A\\ | ||
- | **seg_ID:** DIE_1, DIE_9\\ | ||
- | *Pronounced scarp of WNW-ESE direction dividing the hilly terrain with narrow valley of Danube to the NE from comparatively flat area with wide Danube valley to the SW. Interrupted and multiple morpholineament continues in ESE direction towards Hafnerbach, partly reflecting the structure of the crystalline basement. This scarp, very likely a fault (not identified in geological maps), possibly a minor normal fault terminating now eroded Tertiary Molasse sediments, seems to lack any horizontal offset by Diendorf fault (sections DIE_1 and DIE_9), therefore providing evidence against significant strike slip of the latter after the formation of the former. | ||
- | *This structure is likely a part of a system of WNW- to NW- striking faults with small slip amplitude documented by multiple observations and indicated by penetrative presence of morpholineaments in an extensive area hosting the whole DF and southern BF. The age of these faults is largely unknown but some of them were observed to displace Quaternary strata. In Dunkelsteiner Wald and Wachau this fault system may host sources of weak seismicity. | ||
- | *Also note the N-S oriented morpholineaments near Aggasbach Dorf north of here which seem to coincide with deflected valley of Danube river.\\ | ||
- | doplnit do databáze + obrázek FIXME\\ | ||
- | ............. | ||
- | ====Limberg: | ||
- | **evi_ID: LIM_A**\\ | ||
- | **seg_ID: DIE_4**\\ | ||
- | *Eggenburgian synsedimentary faulting near Diendorf fault - parallel secondary faults in Hengel quarry in Limberg (Decker 1999). Faults are steep, on stereodiagrams they seem to be vertical on average with strike-slip kinematics. In the schematic profile the east-dipping faults are emphasized.\\ | ||
- | + obrázek Decker FIXME\\ | ||
- | ............. | ||
- | ====Tasovice: | ||
- | **evi_ID: TAS_A, TAS_B**\\ | ||
- | **seg_ID: DIE_7**\\ | ||
- | *Absence of fault-related displacement of >5 m thick sequence of Quaternary? loess, sand, paleosol, silt, clay and gravel sealing the observed fault in a broad fault zone exposed in deep trench. Dating based on OSL is problematic but the age largely exceeding 100 ka is very likely for the central and lower parts of the sequence. | ||
- | *Thin blind clastic dike cuts through the lower part of the sedimentary sequence above the fault. No systematic offset was observed, only local disturbation of beds adjacent to the dike (Prachař 2017). The clastic dike can be interpreted as an effect of local liquefaction generated by earthquake-induced shaking. This hypothetical earthquake is not necessarily related to Diendorf fault. (Špaček et. al 2018)\\ | ||
- | + obrázek ? FIXME\\ | ||
- | ............. | ||
- | |||
- | ====Lechovice: | ||
- | **evi_IDs: LECH_A, LECH_B**\\ | ||
- | **seg_ID: BB_1**\\ | ||
- | *Roadcut (presently rehabilitated) situated ~1.5 km from the Diendorf fault line. System of NNW-striking normal faults displacing sandy gravels of high river terrace (LECH_A) associated with sand intrusions (LECH_B). All feeder dikes are blind. Strong block rotation on the observed faults, formation of small-scale graben structures and colocation with sand-intrusions suggest formation by lateral spreading, near-synchronous with deposition of Lower to early Middle Pleistocene terrace. The causal link between the hypothetical earthquake and the Diendorf fault or the deep-seated NW-SE to NNW-SSE oriented cross-faults has not been resolved. The observed faults are similarly oriented as those at Stošíkovice (below) but also sub-parallel to local scarp and to general-scale trend of the Jevišovka river valley. Structural control by either of these features is possible. (Špaček et al. 2018)\\ | ||
- | + obrázky FIXME\\ | ||
- | ............. | ||
- | ====Stošíkovice: | ||
- | **evi_ID: STOS_A**\\ | ||
- | **seg_ID: BB_1**\\ | ||
- | *Small sand pit in L. Miocene sands situated ~250 m from the Diendorf fault line. WNW-WSE striking fault with incorporated gravel of high terrace relic (explained either by active faulting or structurally controlled cryoturbation) and a system of older, small-displacement, | ||
- | + obrázek FIXME\\ | ||
- | ............. | ||
- | ====Hostěradice: | ||
- | **evi_ID:** HOS_A\\ | ||
- | **seg_ID:** BB_1\\ | ||
- | *Trench HOS-1 with fault in Lower Miocene sediments sealed by 17 ky old sands and and ?28 ky loess loam. Špaček et al. (2017, 2018)\\ | ||
- | + obrázky ERT+trench FIXME\\ | ||
- | ............. | ||
- | ====Kadov: Observed sealing strata==== | ||
- | **evi_ID:** KAD_A\\ | ||
- | **seg_ID:** BB_2\\ | ||
- | *Trench KAD-1 with fault sealed by the 23 ky old loess and the pre-loess scree. Fault slip in the time range 100 to <23 ky can not be ruled out (see references below for more details). The exposure of fault contact crystalline vs. E. Miocene sediment in an erosional gully some 120 m NE from here provided fault slickensides with striations plunging 50° to NNE. Špaček et al. (2017, 2018)\\ | ||
- | + obrázky ERT+trench FIXME\\ | ||
- | ............. | ||
- | |||
- | ====Lesonice: | ||
- | **evi_ID:** LES_A\\ | ||
- | **seg_ID:** BB_3\\ | ||
- | *Refraction and reflection seismic profile crossing the fault line (Alexa 2007; diploma thesis supervised by J. Valenta) showing a >50 m vertical offset at the base of low-velocity strata (assumed Lower Miocene sediment and/or strongly weathered crystalline) and a >40 m thick, apparently vertically undisplaced, | ||
- | doplnit do databáze + obrázky FIXME\\ | ||
- | ............. | ||
- | |||
- | ====Budkovice: | ||
- | **evi_ID:** BUD_A\\ | ||
- | **seg_ID:** BB_4\\ | ||
- | *Undisplaced high terrace (Lower to early Middle Pleistocene) sealing the fault and terrace relics at the same height on both sides of the fault. Špaček et al. (2018)\\ | ||
- | + doplnit detaily a obrázky FIXME | ||
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- | ---- | ||
- | |||
- | ===== Main data sources for fault map ===== | ||
- | |||
- | **Geological maps and explaining texts: | ||
- | *scale 1:25000: | ||
- | * sheet 34-133 Hatě (Čtyroký et al. 1978, 1987; Batík et al. 1978) | ||
- | * sheet 34-132 Božice (Dornič et al. 1983, 1984) | ||
- | * sheet 34-131 Šatov (Batík et al. 1977, 1982, 1983) | ||
- | * sheet M-33-117-C-a Šatov (Dlabač et al. 1970) | ||
- | * sheet M-33-117-C-b Jaroslavice (Batík et al. 1972) | ||
- | * sheet 34-114 Prosiměřice (Dornič et al. 1985a,b) | ||
- | * sheet 34-113 Znojmo (Čtyroký et al. 1978, 1983a,b) | ||
- | * sheet 34-112 Miroslav (Dornič et al. 1987) | ||
- | * sheet M-33-117-B-a Miroslav (Dornič 1972) | ||
- | * sheet M-33-105-D-c Moravský Krumlov (Dlabač et al. 1975) | ||
- | * sheet M-33-105-D-b Ivančice (Jaroš 1964a,b) | ||
- | * sheet 24-341 Oslavany (Buriánek et al. 2011a,b) | ||
- | * sheet M-33-105-B-d Rosice (Jaroš et al. 1972c) | ||
- | * sheet M-33-105-B-b Veverská Bitýška (Mísař and Jaroš 1972; Jaroš et al. 1972a,b) | ||
- | * sheet 24-321 Tišnov (Hanžl et al. 2001a,b) | ||
- | * sheet 24-322 Blansko (Hanžl et al. 2000a,b) | ||
- | *scale 1:50000: | ||
- | * sheet 37-Mautern (Matura et al. 1983) | ||
- | * sheet 23-Hadres (Rötzel et al. 2007) | ||
- | * sheet 22-Hollabrun (Rötzel et al. 1998) | ||
- | * sheet 21-Horn (Frasl et al. 1991) | ||
- | * sheet 9-Retz (Rötzel et al. 1999) | ||
- | * sheet 34-13 Dyjákovice (Čtyroký et al. 1987; Müller et al. 2003) | ||
- | * sheet 34-11 Znojmo (Matějovská et al. 1988; Müller et al. 2002) | ||
- | * sheet 24-33 Moravský Krumlov (Matějovská et al. 1991) | ||
- | * sheet 34-12 Pohořelice (Havlíček et al. 1988; Müller et al. 1995) | ||
- | * sheet 24-34 Ivančice (Pálenský et al. 1994; Müller et al. 1994; Batík et al. 1994) | ||
- | * sheets 24-32, 24-14, 24-23, 24-21 (ČGS 2014) | ||
- | *scale 1:200 000: sheet Niederösterreich Nord (Schnabel 2002) | ||
- | *special maps: (Čížek 1976; Mátl 1980; Kolektiv 1994; Špaček et al. 2015, 2016) | ||
- | |||
- | **Geophysics: | ||
- | *Regional gravimetry a aeromagnetic survey (compiled maps of Švancara in Špaček et al. 2018; Blaumoser 1992) | ||
- | *Local airborne magnetic and electromagnetic survey (DIE_5, WEI_2; Sieberl et al. 1996, 1997) | ||
- | *Local gravimetry (DIE_1 to DIE_5, Figdor and Scheidegger 1977; BB_7-10, Halíř et al. 1987) | ||
- | *Electrical resistivity tomographic profiles, seismic refraction and reflection profiles (Valenta and Tábořík et al. in Špaček et al. 2016, 2018 and references therein; Alexa 2017) | ||
- | *Local high-resolution electromagnetic conductivity survey between Hostěradice and Lechovice (BB_1; yet unpublished data by Fojt and Špaček) | ||
- | *Vertical electrical sounding in the sediments on sections DIE_6-8, BB_1 and BB_9,10 (Kraus 1989, Synek 1980, Hron 1980, Bláha a Synek 1987, //none of these surveys have good enough resolution and none of them shows changes of physical properties or structure which could be associated with the fault//). | ||
- | |||
- | **Other: | ||
- | *DEM: Lidar based models of the Czech Republic (DMR4g and 5g; ČÚZK 2013, 2016) and Lower Austria | ||
- | *Drill survey: mainly shallow drilling (mostly from CGS/Geofond archive, see references in Špaček et al. 2015b) | ||
- | |||
- | |||
- | ---- | ||
- | ===== Other notes===== | ||
- | |||
- | **Ongoing reserach and possible future work to be done:** | ||
- | *EM conductivity mapping of fault and covering sediments south of Hostěradice (Fojt and Špaček, ongoing), near Ivančice, Lesonice and Bořitov (planned) | ||
- | *studies on cross structures | ||
- | |||
- | |||
- | ---- | ||
- | ===== References ===== | ||
- | *Alexa, M. (2017): Studium Diendorf-Boskovické stuktury pomocí geofyzikálních metod. Diplomová práce MS. PřF UK Praha. | ||
- | *Batík P. et al. (1977) : Vysvětlivky k základní geologické mapě 1:25000 list 34-131 Šatov. ÚÚG Praha. | ||
- | *Batík, P. et al. (1978): Vysvětlivky k základní geologické mapě 1:25 000 34-133 Hatě. ČGS/ | ||
- | *Batík, P. et al. (1982): Vysvětlivky k základní geologické mapě ČSSR 1:25 000; 34-131 Šatov. ÚÚG, Praha. | ||
- | *Batík, P. et al. (1983): Geologická mapa ČR 1:25 000, list 34-131 Šatov. ÚÚG, Praha. | ||
- | *Batík, P., Dlabač, M., Dudek, A., Skořepa, J., Zeman, A. (1972): Vysvětlující text k základní geologické mapě 1:25 000 list M-33-117-C-b Jaroslavice. Ms. ČGS – Geofond, Praha. | ||
- | *Batík, P., Dlabač, M., Gabriel, M., Neubauer, M., Zeman, A. (1970): Vysvětlující text k základní geologické mapě 1:25 000 M-33-117-C-a Šatov. Ms. ČGS – Geofond, Praha. | ||
- | *Bláha, V. and Synek, V. (1987): Neogénní sedimenty jihozápadní části karpatské předhlubně (reinterpretace). Geofyzika Brno, GF P055751. | ||
- | *Blaumoser N.H. (1992): Eine erste gesamte aeromagnetische Karte von Österreich und ihre Transformationen. Mitt. österr. geol. Ges. 84 (1991), 185-203. | ||
- | *Buriánek, D. et al. (2011a): Základní geologická mapa České republiky 1:25 000, list 24-341 Oslavany. Česká geologická služba. Brno. | ||
- | *Buriánek, D. et al. (2011b): Vysvětlivky k základní geologické mapě České republiky 1 : 25 000 list 24-341 Oslavany. Závěrečná zpráva, 257 s. MS Česká geologická služba. | ||
- | *ČGS (2014): Bezešvá geologická mapa 1:50 000. Česká geologická služba, Praha. On-line, http:// | ||
- | *Čížek, P. (1976): Mapování a vývoj miocénních sedimentů v okolí Ivančic a Oslavan. Ms. Přírodovědecká fakulta MU, Brno. | ||
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