In this Master's thesis I engage in the problematics of the species concept of green subaerial alga Trentepohlia (Ulvophyceae, Chlorophyta). This genus has been studied intensively since the 18th century. For more than 200 years, Trentepohlia species have been delimited using various morphological criteria. However, recent molecular studies showed inadequacies in this approach Therefore, my goal was a precise morphological study of the European Trentepohlia species and the re-evaluation of their phylogenetic position using rbcL gene sequencing. During the period 2013-2015, I carried out a detailed study of the oldest references of Trentepohlia species and compiled a delimitation key of the European species. Based on this research I concluded that it would be desirable to synonymize T. odorata with T. jolithus, as well as T. uncinata with T. arborum. I also sampled Trentepohlia species within Europe and carefully studied and described their morphology. Fresh Trentepohlia thalli were molecularly characterized by cloning, which revealed a common mixture of Trentepohlia species in what on a first sight appears to be a homogenous crust. Phylogenetic analyses based on the rbcL confirmed the ongoing inconsistencies among morphologically and molecularly delimited species and also the existence of cryptic...

Florida's Plio-Pleistocene strata record episodes of sea-level highstands. The age of the strata is often ambiguous as there are no consistently reliable dating techniques that can be unequivocally applied to many of the units. The lack of preservation of continuous Plio-Pleistocene sedimentary sequences is a consequence of Pleistocene mean sea-levels not flooding peninsular Florida, the low volume of sedimentary supply, and the lack of new accommodation space. This study investigates a 6 m cyclothem-type set of six shallow-marine shell beds separated by five subaerially exposed packstone beds. These strata are part of the biostratigraphically-defined early Pleistocene (1.1 -- 1.6 Ma) Bermont formation and were likely deposited during a 160 kyr interval between 1.3 and 1.1 Ma. The shell beds are mollusk-rich and contain moderately well-sorted fine sands. The packstones contain sparry calcite cements and show evidence of subaerial weathering, such as an irregular upper solution surface, root molds, and sparry freshwater calcite cements. The upper surfaces of the packstones are unconformities that separate five episodes of highstand deposition. A grain-size analysis shows an upward-coarsening trend between depositional episodes, which most likely indicates a progressively decreasing water depth. The bivalve assemblages suggest a mean paleodepth during the deposition of the shell beds of approximately 7.5 m; alternatively, in situ Anodontia alba, which colonized these units after deposition, point to a depth of 1 m. A subsidence rate of 6 m/Ma is inferred from the thickness of deposits near the locality. Based on a comparison of the height of the strata with ex isting eustatic curves, the early Pleistocene age of the formation, and the 6 m/Ma subsidence rate, the most parsimonious duration for the interval between the cyclothems is 41 kyr, dominantly forced by obliquity orbital variability. Combining the data indicates that the early Pleistocene sea level was between 11.2 and 14.4 m above sea level (asl); previous estimates of early Pleistocene highstands have shown an elevation approximately 15 m asl. If the 1 m depth of Anodontia alba is used, the depth was likely 6.3 m asl.

This project histologically examined weathering on faunal bones. The sample consisted of a mixture of faunal remains, assessed and assigned to weathering stages (WS) 0-2 from Behrensmeyer’s (1978) scoring method. A total of 77 bones sections were observed for histological analysis. A portion were obtained, partially fleshed, commercially and were placed at the Outdoor Research Facility (ORF) in Holliston, MA. After deposition, bones were collected at specific time intervals allowing for 2, 4, 6, 8, 12, and 18-month exposure times. Bones were also collected from several outdoor locations in Ohio, having been exposed for an unknown period, and ranging from WS 0-2. Following histological preparation of the sample, the microstructure of each weathering stage was observed using the image analysis software Fiji from the National Institutes of Health (NIH). Data recorded included the number of cracks present per unit area and the depth of cracking. The number of cracks per unit area for each section of bone was calculated by dividing the number of cracks per section by the total section area resulting in number of cracks per mm2. Depth of cracking was analyzed through maximum crack length and average crack length. This data was compiled and one-way ANOVA tests were applied to determine where weathering stage and exposure time were statistically significant. This was followed by Bonferroni post-hoc analyses which were utilized to analyze the interactions within the WS and exposure time variables; to allow for analysis of statistical significance of WS to one another and exposure time intervals to one another. It was hypothesized that different weathering states would be statistically significant from one another, and microscopically identifiable through a histological examination, and that these would be able to be differentiated from other sources of microtaphonomic alteration including burial and thermal alteration. It was also hypothesized that exposure time would significantly impact the histological characteristics including the number of cracks per mm2 and the maximum and average crack depth. One-way ANOVA analysis indicated that WS has a significant impact on the number of cracks per mm2 and the maximum crack length. No significance was observed for analysis of WS and average crack length. Post-hoc analysis involving the number of cracks per mm2 revealed statistical significance between WS 0 and WS 1, WS 0 and WS 2. Analysis involving maximum crack length indicated significance only between WS 0 and WS 1. Post-hoc analysis involving average crack length did not indicate any statistically significant relationships between the WS. One-way ANOVA analysis of exposure time indicated that exposure time has a significant impact when on all three variables: number of cracks per mm2, average crack length, and maximum crack length. Post-hoc analysis involving the number of cracks per mm2 found that months 0, 2, 4, 6, and 8 were all statistically significant from 18 months. Analysis of average crack length revealed that months 0 and 2 were both statistically from 8 months of exposure. Post-hoc analysis involving maximum crack length reveals statistical significance between months 0 and 8, 0 and 12, and 2 and 8. Histological characteristics of weathered bone were found to include delamination and cracking. Delamination was observed on several bones in WS 2 and one in WS 1, while cracking was observed in bones of all stages. Positive relationships were observed between WS and number of cracks per mm2, and between exposure time and cracks per mm2 indicating that as one increased so did the other. No trend was observed for the relationship between exposure time and either of the crack length variables; the same was observed for the relationship between WS and the two crack length variables. Through comparison of the histological characteristics of weathered bone with other sources of microtaphonomic alterations, it was determined that weathering and its histological characteristics are different from other alteration sources, including burial and thermal alteration, to allow for determination of the microtaphonomic process affecting the bone.

In this study, numerical modeling of landslide generated tsunami waves in closed basins and their mechanisms are presented. Historical landslide generated tsunamis are investigated and also the governing parameters affecting impulse wave parameters are studied. The numerical model is based on the solution of nonlinear form of the long wave equations with respect to related initial and boundary conditions. In order to validate the outputs of the modeling by NAMIDANCE, empirical formulation is applied to the same cases as the numerical model and the results are discussed. The numerical model is then applied to Pervari Dam artificial reservoir as a case study to investigate the effects of potential landslide into the reservoir. The outputs of the numerical model are compared with empirical formulation results for different approaches of modeling the landslide effect in water body. The critical sections are observed for overtopping and maximum wave amplitude values and the results are discussed.

Tsunamis are one of the most catastrophic natural events impacting coastal regions often generated by undersea earthquakes. Nevertheless, in enclosed basins, i.e., fjords, reservoirs and lakes, subaerial or submarine landslides can initiate devastating tsunamis with similar consequences. Although a subaerial or submarine landslide that impinges into a large water body can generate a tsunami, subaerial landslides are much more efficient tsunami generators than its counterpart. In this study we aim to integrate laboratory scale experiments of tsunami generation by subaerial landslide with numerical models. The work focuses on the numerical validation of two three-dimensional Navier-Stokes (3D-NS) models, FLOW-3D and our developed model TSUNAMI3D. The models are validated based on previous large scale laboratory experiments performed by a tsunami research team lead by Dr. Hermann Fritz, Georgia Institute of Technology. Three large scale landslide scenarios were selected from the set of laboratory experiments, namely, fjord like, headland and far field coastline. These scenarios showed that complex wave fields can be generated by subaerial landslides. The correct definition and evolution of the wave field are key to accurate modeling the ensuing tsunami and its effect in coastal regions. In this study, comparisons are performed between numerical results and laboratory experiments. Methodology and key parameters for soil rheology are defined for model validations. Results of the models are expected to be under the allowable errors indicated by the National Tsunami Hazard Mitigation Program (NTHMP), National Oceanic and Atmospheric Administration (NOAA) guidelines for validation of tsunami numerical models. The ultimate goal of this research is to obtain better tsunami calculation tools for real-world application of 3-D models for landslide tsunamis, which are necessary for the construction of inundation maps in the Gulf of Mexico and the Caribbean regions.

Riparian buffers are promoted for water quality improvement, habitat restoration, and stream bank stabilization. While considerable research has been conducted on the effects of riparian buffers on water quality and aquatic habitat, little is known about the influence of riparian vegetation on stream bank erosion. The overall goal of this research was to evaluate the effects of woody and herbaceous riparian buffers on stream bank erosion. This goal was addressed by measuring the erodibility and critical shear stress of rooted bank soils in situ using a submerged jet test device. Additionally, several soil, vegetation, and stream chemistry factors that could potentially impact the fluvial entrainment of soils were measured. A total of 25 field sites in the Blacksburg, Virginia area were tested. Each field site consisted of a 2nd-4th order stream with a relatively homogeneous vegetated riparian buffer over a 30 m reach. Riparian vegetation ranged from short turfgrass to mature riparian forest. Multiple linear regression analysis was conducted to determine those factors that most influence stream bank erodibility and the relative impact of riparian vegetation. Results of this research indicated woody riparian vegetation reduced the susceptibility of stream bank soils to erosion by fluvial entrainment. Riparian forests had a greater density of larger diameter roots, particularly at the bank toe where the hydraulic stresses are the greatest. These larger roots (diameters > 0.5 mm) provided more resistance to erosion than the very fine roots of herbaceous plants. Due to limitations in the root sampling methodology, these results are primarily applicable to steep banks with little herbaceous vegetation on the bank face, such as those found on the outside of meander bends. In addition to reinforcing the stream banks, riparian vegetation also affected soil moisture and altered the local microclimate. While summer soil desiccation was reduced under deciduous riparian forests, as compared to herbaceous vegetation, winter freeze-thaw cycling was greater. As a result, in silty soils that were susceptible to freeze-thaw cycling, the beneficial effects of root reinforcement by woody vegetation were offset by increased freeze-thaw cycling. Using the study results in an example application, it was shown that converting a predominately herbaceous riparian buffer to a forested buffer could reduce soil erodibility by as much as 39% in soils with low silt contents. Conversely, for a stream composed primarily of silt soils that are prone to freeze-thaw cycling, afforestation could lead to localized increases in soil erodibility of as much as 38%. It should be emphasized that the riparian forests in this study were deciduous; similar results would not be expected under coniferous forests that maintain a dense canopy throughout the year. Additionally, because dense herbaceous vegetation would likely not develop in the outside of meander bends where hydraulic shear stresses are greatest, the reductions in soil erodibility afforded by the herbaceous vegetation would be limited to areas of low shear stress, such as on gently sloping banks along the inside of meander bends. As the first testing of this type, this study provided quantitative information on the effects of vegetation on subaerial processes and stream bank erosion. It also represents the first measurements of the soil erosion parameters, soil erodibility and critical shear stress, for vegetated stream banks. These parameters are crucial for modeling the effects of riparian vegetation for stream restoration design and for water quality simulation modeling. / Ph. D.

Mes travaux de recherche ont eu pour but d’analyser la diversité des microorganismes des trois domaines du vivant présents dans des biofilms phototrophes exposés à l’air, se développant sur des substrats minéraux divers, afin d’essayer, d’une part, de répondre à des questions de diversité et de biogéographie et, d’autre part, d’étudier le processus de colonisation par le biais d’expériences d’exposition contrôlées.J’ai ainsi caractérisé, essentiellement par des approches moléculaires basées sur l'analyse des banques des gènes d'ARNr de la petite sous-unité (SSU rDNAs) et sur des analyses d'empreintes communautaires, la diversité microbienne (procaryote et eucaryote) formant des biofilms matures (exposés depuis plusieurs années) dans plusieurs sites géographiques en Irlande du Nord, en France et en Ukraine, dans la région de Chernobyl. Dans ces biofilms soumis à forte pression sélective, nous avons mis en évidence beaucoup de microorganismes hétérotrophes et phototrophes, mais avec une diversité relativement restreinte en comparaison à d’autres milieux comme les sols ou les systèmes aquatiques. Les archées étaient absentes. Les conditions environnementales auxquelles ce type de biofilm est constamment exposé comme l’irradiation, la dessiccation et la limitation des nutriments sélectionnent des microorganismes qui développent des stratégies pour s’adapter comme, entre autres, la production de pigments. Ce sont des microorganismes fréquemment retrouvés dans des milieux désertiques extrêmes et résistants aussi aux radiations ionisantes qui ont ainsi été identifiés, notamment des Deinococcales et des Actinobacteria, ou encore des champignons ascomycètes (Ascomycota). Parmi les organismes phototrophes, nous avons dénombré des Cyanobacteria, des algues vertes (Chlorophyta) et des Streptophyta. Nous avons mis en évidence que les facteurs environnementaux influencent la composition des biofilms. Toutefois, tandis que la composition de la communauté bactérienne est fortement dépendante de la nature du substrat ou elle se développe, la composition des communautés microbiennes eucaryotes dépend de la distance géographique. Nous avons également mené des expériences de colonisation en exposant un même substrat minéral dans trois sites géographiques en Irlande du Nord et en France. L'analyse de la diversité microbienne lors du processus de colonisation a révélé des changements importants dans la composition des communautés, que ce soit pour les procaryotes ou pour les eucaryotes avec, cependant, des comportements différents de ces deux groupes de microorganismes. Dans le cas des bactéries, on observe une transition des Gammaproteobacteria, qui dominent les temps 0-6 mois et qui correspondent vraisemblablement aux cellules inactives en dispersion, vers des Betaproteobacteria, Bacteroidetes, Alphaproteobacteria et Actinobacteria dans des phases successives de formation du biofilm. Par contre, dès leur détection sur le substrat minéral, les eucaryotes sont massivement dominés par des champignons ascomycètes et basidiomycètes, des algues vertes ainsi que d'autres composantes minoritaires comme des ciliés, étant détectées dans des stades plus tardifs. Nos résultats montrent que les organismes hétérotrophes sont pionniers dans la formation de ces biofilms, ce qui permet d'émettre l'hypothèse qu'ils facilitent l'installation des cyanobactéries et surtout des algues vertes. Ils montrent aussi que le processus d'assemblage des communautés bactériennes dépend du temps de colonisation, alors que le site géographique détermine celui des microorganismes eucaryotes. Ces différences majeures de comportement pourraient être expliquées par des modes de vie différents entre les organismes de ces deux grands groupes. / The major objective of my PhD work was the analysis of the diversity of microorganisms from the three domains of life associated with phototrophic biofilms developing on different mineral substrates exposed outdoors. These studies aimed at answering questions about microbial diversity and biogeography and also at studying the colonization process through controlled exposure experiments. I have thus characterized, essentially by molecular methods based on small subunit (SSU) rRNA gene libraries and fingerprinting analyses the diversity of prokaryote and eukaryote microorganisms forming mature biofilms (exposed for several years) in various geographic sites in Northern Ireland, France and Ukraine, in the Chernobyl area. In these biofilms, subjected to strong selective pressure, we found many heterotrophic and phototrophic microorganisms, but their diversity was limited when compared to that of other environments such as soils or aquatic systems. Archaea were absent from all biofilms. The environmental conditions to which these biofilms are constantly exposed, such as irradiation, desiccation and nutrient limitation select for organisms that develop particular adaptive strategies including, among others, pigment production. The microorganisms identified in these biofilms are also frequently found in extreme, desert environments and are known for their resistance also to ionizing radiation, such as Deinococcales and Actinobacteria or ascomycete fungi (Ascomycota). Among phototrophic lineages, we identified Cyanobacteria, Chlorophyta (green algae) and sometimes Streptophyta. We showed that environmental parameters influenced biofilm microbial communities. However, whereas the bacterial community composition depends on the nature of the substrate, the microbial eukaryotic community composition depends on the geographic distance. We also carried out colonization experiences exposing outdoors the same mineral substrate in three different sites in Northern Ireland and France. The analysis of microbial diversity along the colonization process revealed important changes in community composition both for prokaryotes and eukaryotes, although the behavior of the two groups was different. In the case of bacteria, we observed a transition from Gammaproteobacteria, which dominated the initial 0-6 months and which likely corresponded to inactive dispersive cells, towards Betaproteobacteria, Bacteroidetes, Alphaproteobacteria and Actinobacteria in successive steps of biofilm formation. By contrast, since their detection on mineral substrates, eukaryotes were massively dominated by ascomycete and basidiomycete fungi, green algae and other minor components such as ciliates were detected in later stages of biofilm formation. Our results show that heterotrophic organisms are pioneers in the formation of these biofilms, leading to the hypothesis that they facilitate the settlement of Cyanobacteria and, especially, of green algae. They also show that the process of bacteria community assembly depends on colonization time whereas the geographic site determines that of eukaryotic microorganisms. These major differences might be explained by different lifestyles between organisms of the two groups

Die Sedimente des Halleschen Permokarbonkomplexes gaben schon immer Raum für Spekulationen. Aufgrund ihrer Dominanz an rhyolithischen Geröllen wurden sie über einen langen Zeitraum einheitlich als Postporphyrschutt ausgehalten. Vielfältig wechselnde Faziesbedingungen machten es jedoch notwendig, die Sedimente aufzugliedern. Neuere Erkenntnisse in der Erforschung des Halleschen Permokarbonkomplexes erfordern eine Überprüfung v. a. der nach KUNERT (1995) aufgestellten allgemeinen stratigraphischen Gliederung der Unterrotliegendsedimente in Halle,- Hornburg,- Sennewitz- und Brachwitz-Formation anhand einiger ausgewählter Beispiele. Der ursprüngliche Gedanke der Diplomarbeit bestand darin, eine Fazies- und eine Geröllanalyse der unterpermischen Abtragungsprodukte des Halle-Vulkanitkomplexes anzufertigen. Zur Verfügung standen zwei Kernbohrungen und zwei Aufschlüsse, sowie diverse Unterlagen zu angrenzenden Bohrungen in der Saale-Senke. Die beiden Oberflächenaufschlüsse Riveufer und Teichgrund sollten stratigraphisch aufgenommen werden, so dass eine Fazieszuordnung möglich ist. Die Bohrung Brachwitz 2/62 wurde mit dem Ziel aufgenommen, neuere Theorien über den Ablagerungszeitraum der Rotliegend-Sedimente in Bezug auf den permokarbonen Vulkanismus zu widerlegen oder zu bekräftigen. Die zweite Bohrung (Kb Lochau 7/65) wurde am Rande mit in die Diplomarbeit einbezogen, da sie das immense Spektrum der spätvulkanischen Aktivitäten im Halle Permokarbonkomplex erweitert. Ergebnis ist eine Neugliederung des Rotliegend im Halleschen Permokarbonkomplex, in der nur noch die Halle-Formation mit ihrem ausgeprägten Vulkanismus und die Hornburg-Formation, stellvertretend für alle jüngeren Abtragungsprodukte des Halle Vulkanitkomplexes, unterschieden werden. Mit einem großen Hiatus folgt anschließend die Eisleben-Formation.

Die Sedimente des Halleschen Permokarbonkomplexes gaben schon immer Raum für Spekulationen. Aufgrund ihrer Dominanz an rhyolithischen Geröllen wurden sie über einen langen Zeitraum einheitlich als Postporphyrschutt ausgehalten. Vielfältig wechselnde Faziesbedingungen machten es jedoch notwendig, die Sedimente aufzugliedern. Neuere Erkenntnisse in der Erforschung des Halleschen Permokarbonkomplexes erfordern eine Überprüfung v. a. der nach KUNERT (1995) aufgestellten allgemeinen stratigraphischen Gliederung der Unterrotliegendsedimente in Halle,- Hornburg,- Sennewitz- und Brachwitz-Formation anhand einiger ausgewählter Beispiele. Der ursprüngliche Gedanke der Diplomarbeit bestand darin, eine Fazies- und eine Geröllanalyse der unterpermischen Abtragungsprodukte des Halle-Vulkanitkomplexes anzufertigen. Zur Verfügung standen zwei Kernbohrungen und zwei Aufschlüsse, sowie diverse Unterlagen zu angrenzenden Bohrungen in der Saale-Senke. Die beiden Oberflächenaufschlüsse Riveufer und Teichgrund sollten stratigraphisch aufgenommen werden, so dass eine Fazieszuordnung möglich ist. Die Bohrung Brachwitz 2/62 wurde mit dem Ziel aufgenommen, neuere Theorien über den Ablagerungszeitraum der Rotliegend-Sedimente in Bezug auf den permokarbonen Vulkanismus zu widerlegen oder zu bekräftigen. Die zweite Bohrung (Kb Lochau 7/65) wurde am Rande mit in die Diplomarbeit einbezogen, da sie das immense Spektrum der spätvulkanischen Aktivitäten im Halle Permokarbonkomplex erweitert. Ergebnis ist eine Neugliederung des Rotliegend im Halleschen Permokarbonkomplex, in der nur noch die Halle-Formation mit ihrem ausgeprägten Vulkanismus und die Hornburg-Formation, stellvertretend für alle jüngeren Abtragungsprodukte des Halle Vulkanitkomplexes, unterschieden werden. Mit einem großen Hiatus folgt anschließend die Eisleben-Formation.:Inhalt Abbildungsverzeichnis Tabellenverzeichnis Abkürzungsverzeichnis 1. Einleitender Teil 1 1.1 Einleitung 1 1.2 Aufgabenstellung und Problematik 1 1.3 Geographischer Überblick über die Bohrungen und Aufschlüsse 2 2. Regionalgeologischer Teil 4 2.1 Aufbau des Halle Vulkanitkomplexes 4 2.2 Beckenentwicklung des Permokarbons im Bereich des Halle- Vulkanitkomplexes 5 2.3 Historischer Rückblick über die Einstufung der Rotliegend-Formationen im Halle Vulkanitkomplex 10 2.4 Neueste Entwicklungen in der Erforschung des Saale-Beckens 15 2.4.1 Die Ablagerungen der Halle-Formation 15 2.4.2 Die Ablagerungen der Sennewitz-Formation 16 2.4.3 Die Ablagerungen der Hornburg-Formation 17 2.4.4 Die Ablagerungen der Brachwitz-Formation 19 2.4.5 Die Ablagerungen der Eisleben-Formation 20 2.4.6 Aktuelle Stratigraphische Gliederung 22 2.5 Die späte Phase des Halle Vulkanitkomplexes und ihr Bezug zur Diplomarbeit 23 3 Arbeitsmethodik 24 3.1 Aufnahme der Bohrungen Brachwitz 2/62 und Lochau 7/65 24 3.2 Aufnahme des Aufschlusses am Teichgrund bei Döblitz 26 3.3 Aufnahme des Aufschlusses am Riveufer im Stadtgebiet von Halle 26 4. Vulkanische und sedimentäre grobklastische Transport- und Ablagerungssysteme 27 4.1 Vulkanische Massentransporte 27 4.1.1 Pyroklastische Ablagerungen 27 4.1.1.1 Pyroklastische Fallablagerungen 28 (1) Aschefallablagerungen 28 (2) Bimsführende Fallablagerungen 29 (3) Scoriaführende Fallablagerungen 29 4.1.1.2 Pyroklastische Stromablagerungen 29 (1) Bimsführende pyroklastische Stromablagerungen oder Ignimbrite 29 (2) Block- und Aschestromablagerungen 31 (3) Scoriaführende pyroklastische Stromablagerungen 32 4.1.1.3 Pyroklastische Surge-Ablagerungen 32 (1) Surgeablagerungen durch Aschewolken 32 (2) Ablagerungen am Boden der pyroklastischen Surge 33 (3) Ablagerungen an der Basis der pyroklastischen Surge 33 4.1.2 Explosive vulkanische Eruptionen 33 (1) Hawaiianische Eruptionen 34 (2) Plinianische Eruptionen 34 (3) Strombolianische Eruptionen 35 (4) Vulkanianische und Surtseyanische Eruptionen 35 4.1.3 Produkte phreatomagmatischer Eruptionen 36 (1) Maare 37 (2) Tuffkegel und Tuffringe 37 4.1.4 Tephraablagerungen 38 4.2 Sedimentäre Massentransporte 39 4.2.1 Alluviale Fächer 40 4.2.2 Schichtfluten 42 4.2.3 Flußsyteme 42 4.2.4 Überflutungsebenen 43 4.2.5 Deltas und Ästuare 44 5. Lithologien und Faziestypen 45 6. Aufschlüsse und Bohrungen 45 6.1 Aufschlußkomplex am Riveufer im Stadtteil Giebichenstein in Halle 48 6.1.1 Allgemeine Aussagen 48 6.1.2 Das Faziesmodell eines verflochtenen Flußsystems 48 (1) Ausbildung von Rinnen 48 (2) Einfallen der Rinnen 50 (3) Prallhänge 50 (4) Seitenanschnitte an beiden Enden des Aufschlusses 51 6.1.3 Ein tuffgefülltes Spaltensystem als syn- bis postsedimentäres Ereignis 52 6.1.4 Interpretation 53 6.2 Aufschluß am Teichgrund bei Döblitz 55 6.2.1 Allgemeine Aussagen 55 6.2.2 Sedimentäre Lithofaziestypen und -assoziationen 56 6.2.3 Dokumentation der einzelnen Aufschlüsse 56 6.2.3.1 Aufschluß T1 56 (1) Detaildarstellung Aufschluß am Teichgrund T1-1 56 6.2.3.2 Aufschluß T2 59 6.2.3.3 Aufschluß T3 59 6.2.4 Fazielle Diskussion 59 6.3 Kernbohrung Brachwitz BrwSk 2/62 südöstlich der Ortschaft Friedrichsschwerz 61 6.3.1 Allgemeine Informationen 61 6.3.2 Erläuterungen zu den Lithofaziestypen 61 (1) SFT-B1 Konglomerat der Eislebenformation 61 (2) SFT-T1 Sedimentäre Brekzie 61 (3) SFT-T4 Mittel- bis Grobsandstein 62 (4) SFT-B2 Schluffstein 62 (5) VFT-T0 Rhyolith, brekziös/ VFT-T1 Porphyrbrekzie, monomikt 63 (6) VFT-B12 Porphyrbrekzie mit Obsidianmatrix 64 (7) VFT-B2 Porphyrbrekzien, oligomikt und polymikt 64 (8) VFT-B3 Mittelsand, vulkanogen 65 (9) VFT-B5 Schluffstein, brekziiert 66 6.3.3 Auswertung 66 6.4 Kernbohrung Lochau 7/65 südöstlich Halle 68 6.4.1 Allgemeines 68 6.4.2 Erläuterungen zu den Vulkanischen Faziestypen 68 (1) VFT-L1 Aschentuff 68 (2) VFT-L2 Surges 69 (3) VFT-L3 Surge oder Explosionsbrekzie 70 (4) VFT-L4 Explosionsbrekzie mit Tuffzwickelfüllung 71 (5) Tuff mit einzelnen Ballistischen Bomben 72 6.4.4 Beispiel Ha-Lo7/17 73 6.4.5 Diskussion 74 7. Zusammenfassung und Ausblick 76 8. Literatur- und Quellenverzeichnis 78 9. Anhang Anlage 1: Allgemeines Anlage 2: Teichgrund bei Döblitz Anlage 3: Riveufer im Stadtzentrum von Halle (Saale) Anlage 4: Kb Brachwitz 2/62 Anlage 5: Kb Lochau 7/65