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This document describes the dataflow of the CubeSat mission SpaceTeamSat1 (STS1) of the TU Wien Space Team (TUST). We developed the dataflow architecture during a game which relates to the Concurrent Design Facility (CDF) utilized by the European Space Agency (ESA). In our so called Dataflow Game every member played the role of a subsystem of the CubeSat. Then we played through different scenarios like sending a beacon from the CubeSat, or uploading a file from the ground to the CubeSat considering both normal operation and error cases. This allowed us to test our high-level design and deduce the functionality of the subsystems in a top-down manner.

One of the most important challenges in the development of autonomous driving systems is to make them robust against unexpected or unknown objects. Many of these systems perform really good in a controlled environment where they encounter situation for which they have been trained. In order for them to be safely deployed in the real world, they need to be aware if they encounter situations or novel objects for which the have not been sufficiently trained for in order to prevent possibly dangerous behavior. In reality, they often fail when dealing with such kind of anomalies, and do so without any signs of uncertainty in their predictions. This thesis focuses on the problem of detecting anomalous objects in road images in the latent space of a VAE. For that, normal and anomalous data was used to train the VAE to fit the data onto two prior distributions. This essentially trains the VAE to create an anomaly and a normal cluster. This structure of the latent space makes it possible to detect anomalies in it by using clustering algorithms like k-means. Multiple experiments were carried out in order to improve to separation of normal and anomalous data in the latent space. To test this approach, anomaly data from multiple datasets was used in order to evaluate the detection of anomalies. The approach described in this thesis was able to detect almost all images containing anomalous objects but also suffers from a high false positive rate which still is a common problem of many anomaly detection methods.

Volcanic ash layers are important markers for the chronostratigraphy of paleoclimate and paleoenvironmental archives at the southern tip of South America. However, this requires that tephras are well-dated. We report geochemical data from the MA1 stalagmite formed in a non-karst cave near Mt. Burney volcano in southernmost Patagonia (~53°S). High-resolution LA-ICP-MS analyses, SEM imagery, and NanoSIMS enable to identify volcanogenic signals during the last 4.5 kyrs BP from sub-annual trace element variations and tephra particles in distinct laminae. The new 230Th/U-chronology of MA1 provides precise dating of tephra from Mt. Burney (MB) and Aguilera (A) at 4216 +93/−193 yrs BP (MB2), 2291 ± 33 yrs BP (MB3), 853 +41/−60 yrs BP (MB4) and 2978 +91/−104 yrs BP (A1). This unique high-resolution record of MA1 holds potential to date further eruptions from Southern Andean volcanoes for the tephrochronology in this critical region, and potentially also large-volume explosive volcanism off South America.

International audience; The aim of this paper is to determine the composition and age of high-temperature (HT) hydrothermal fluids in Closepet granites (Dharwar craton, India). The magmatic origin of the Neoarchaean Closepet batholith has been recognized and dated many times, whereas a HT fluid system, strong evidence for which has been partly investigated, has never been dated. Titanite was chosen for a geochemical study on its pristine and altered domains to illustrate the fluid composition; the domains were dated to recognize the timing of fluid activity. Titanite presents distinct trace element enrichments in non-altered domains and strong depletions in trace elements in marginal, irregular, patchy zones. The high total rare earth element (REE) concentrations and the marked negative Eu anomalies suggest crystallization from a residual melt. The negative Eu anomalies diminish progressively in the REE patterns of altered parts and become positive. Trace element ratios (Nb/Ta, Y/Ho, and U/Th) indicate fluid-crystal interactions. Strong U/Th fractionation might be linked to the presence of CO2 and Cl-. Zr-in-titanite thermometry yields a crystallization/recrystallization temperature of ~700 °C for both magmatic and altered domains. The titanite factor Ti+4/(Al+3 + Fe+3) reveals an affinity with significant mantle input to the fluid system. Pristine and altered titanite domains have been successfully dated by laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS). Reversely discordant apparent ages suggest interaction with fluids, which modified the Pb composition of the magmatic titanite. The oldest semi-concordant analyses of titanite cores indicate an age of approximately 2500 Ma, which we interpret as the minimum age of magmatic titanite crystallization. Narrow dark rims of titanite with considerably lower Th/U ratios form a more coherent group of analyses defining an upper concordia intercept age of 2345 ± 0.016 Ma, interpreted as the best estimate for the time of complete titanite resetting associated with the metasomatic event. The HT fluid system appears to have remained active into the Palaeoproterozoic. Confirmation by dating that the tested fluids belonged to the Archaean hydrothermal system gives us information about this system at the time, but the information that it worked at least until the Palaeoproterozoic provides additional valuable information about the hydrothermal systems during the Neoarchaean-Palaeoproterozoic transition.

Major and trace element concentrations of thirteen limestone samples from zone XX of the Tlayua Quarry Fossillagerstatte were analysed with the aim of elucidating the source of rare earth elements plus yttrium (REE+Y) as well as some palaeoenvironmental conditions attributable to them. The concentrations of cortex-derived elements/element oxides (SiO2, Al2O3, Zr), as well as of phosphorus, show no significant contamination by means of terrigenous material and/or phosphates, which means that the REE+Y concentrations can be interpretable. REE+Y patterns display partly typical modern seawater signals, particularly positive La and Y anomalies, mostly superchondritic Y/Ho ratios (between 42.34 and 56.38) and moderate depletions of light rare earth elements (LREE) and middle rare earth elements (MREE) in comparison to heavy rare earth elements (HREE) (x PrSN/YbSN = 0.12, x NdSN/YbSN = 0.14 and x DySN/YbSN = 0.42, respectively). Negative cerium anomalies could also be identified [(Ce/Ce*SN) = 0.73], which indicate oxidising conditions. In addition, positive Eu anomalies [(Eu/Eu*SN) = 2.53] were detected. Since no convincing evidence for diagenesis, hydrothermal or aeolian input exists, the origin of these anomalies can, to some extent, be attributable to the influence of the dissolution of plagioclases in the water column, which can be inferred from the bivariate correlation of (Eu/Eu*)SN and Na/Al. Despite depicting modern seawater-like signals, an important difference between the REE+Y patterns from zone XX of the Tlayua Quarry and modern seawater REE+Y patterns can be determined. For instance, modern seawater does not display significant europium anomalies. Nevertheless, REE+Y patterns from zone XX of the Tlayua Formation can altogether be reliable palaeoenvironmental proxies for the Cretaceous. The inferred palaeoenvironment for zone XX from these proxies is represented by an open-marine setting, showing oxidising conditions, evidence of plagioclase dissolution and overall negligible terrigenous influence. The palaeoecological interpretation from these patterns does not exclude, however, the probability of monsoonal or tidally influenced sedimentation in other sediments from zone XX or from other zones in Tlayua, as previous works suggest.