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Forty two samples of the Late Eocene Kiliran oil shale, Central Sumatra Basin, Indonesia were collected from a 102 m long drill core. The oil shale core represents the deposition time of about 240.000 years. Palynofacies and geochemical analyses have been carried out to reconstruct the paleoenvironmental conditions and paleoecology during deposition of the oil shale. Amorphous organic matter (AOM) is very abundant (>76%). B. braunii palynomorphs are present (3-16%) as the only autochtonous structured organic matter and generally more abundant in the middle part of the profile. The stable carbon isotopic composition of bulk organic matter (13C) varies from -27.0 to -30.5‰ and is generally more depleted in the middle part of the profile. The ratio of total organic carbon to sulfur (TOC/S), used as salinity indicator, ranges from 2.5 to 15.8 and shows variations along the profile. Slightly less saline environments are observed in the middle part of the profile. Fungal remains are generally present only in this part with a distinct peak of abundance. The presence of fungal remains is regarded as an indication for a relatively warmer climate during deposition of the middle part of the profile. The warmer climate is thought to influence the establishment of a thermocline, limiting the supply of recycled nutrients to epilimnion. Consequently, the primary productivity in the Kiliran lake decreased during deposition of the middle part of the profile as indicated by the relatively depleted 13C values and the blooming of B. braunii. The chemocline was also shoaling during the deposition according to the higher abundance of total isorenieratane and its derivatives originated from green sulfur bacteria dwelling in the photic zone euxinia. The warmer climate is also thought to influence the slightly decrease of water salinity during deposition of the middle part of the profile. The occurrence of B. braunii in Kiliran lake is also recognized from organic geochemical data. The distribution of n-alkanes is characterized by the unusual high amount of C27 n-alkane relative to the other long-chain n-alkanes. The concentrations of C27 n-alkane vary from 30.1 to 393.7 μg/g TOC and are generally in parallel with the abundances of B. braunii palynomorphs along the profile. The 13C values of this compound are about -31‰ and up to 2‰ enriched relative to those of the adjacent long-chain n-alkanes. B. braunii race A can thus be regarded as the significant biological source of the C27 n-alkane. Lower amounts of lycopane are observed in many oil shale samples (0 to 54.7 μg/g TOC). The 13C value of this compound is 17.2‰. This strong enrichment of 13C suggests that the lycopane was derived from B. braunii race L. The concentrations of lycopane develop generally in opposite with those of C27 μalkane. It is likely that both B. braunii races bloomed in alternation in the lake, probably due to changes on specific water chemistry. Norneohop-13(18)-ene and neohop-13(18)-ene derived from methanotrophic bacteria are the dominant hopanoid hydrocarbons. The sum of their concentrations varies from 40.6 to 360.0 μg/g TOC. The 13C of these compounds are extremely depleted (-45.2 to -50.2‰). The occurrence of abundant bacteria including methanotrophic bacteria was responsible for the recycling of carbon below the chemocline of the lake. The effect of the recycling of carbon is observed by the presence of a concomitant depletion (about 7-9‰) in 13C of some specific biomarkers derived from organisms dwelling in the whole phototrophic zone. 4-Methylsterane and 4-methyldiasterene homologues occur in the oil shale as the predominant biomarkers. The sum of the concentrations of all homologues are about 40.3-1,009.2 μg/g TOC with generally higher values in the uppermost and lower parts of the profile. Calcium (Ca) accounts as the predominant element in the oil shale, ranging from 5.0 to 16.7%. This element shows generally parallel variation with the 4-methylsterane and 4-methyldiasterene homologues along the profile. This suggests that these compounds were derived from biological sources favoring more alkaline and more trophic environments. On the other hand, these compounds were less abundant in the middle part of the profile which is consistent with less alkaline and less trophic environments promoting B. braunii to bloom. Alternation between Dinoflagellates and B. braunii in ancient lacustrine environments due to water chemistry changes have been known from previous studies. In the present case, distinct alternation between B. braunii abundances and concentrations of 4-methylsterane and 4-methyldiasterene homologues along the studied oil shale profile suggest a hypothesis that these compounds were derived from freshwater Dinoflagellates although dinosterane is not present in the sediment extracts. Water alkalinity and trophic level changes were most likely responsible for the alternation of Dinoflagellates and B. braunii blooming.
A thick Middle and Late Pleistocene loess/palaeosol sequence is exposed at the gravel quarry Gaul located east of Weilbach in the southern foreland of the Taunus Mountains. The loess/palaeosol sequence correlates to the last three glacial cycles. Seven samples were dated by luminescence methods using an elevated temperature IRSL (post-IR IRSL) protocol for polymineral fine-grains to determine the deposition age of the sediment and to set up a more reliable chronological framework for these deposits. The fading corrected IR50 and the pIRIR225 age estimates show a good agreement for almost all samples. The fading corrected IRSL ages range from 23.7 ± 1.6 ka to >350 ka indicating that the oldest loess was deposited during marine isotope stage (MIS) 10 or earlier and that the humic-rich horizon (Weilbacher Humuszone) was developed during the late phase of MIS 7. Loess taken above the fCc horizon most likely accumulated during MIS 6 indicating that the remains of the palaeosol are not belonging to the last interglacial soil. The two uppermost samples indicate that the youngest loess accumulated during MIS 2 (Upper Würmian). Age estimates for the loess-palaeosol sequence of the gravel quarry Gaul/Weilbach could be obtained up to ~350 ka using the pIRIR225 from feldspar. Keywords: loess, luminescence dating, IRSL, fading, Weilbach, chronostratigraphy
Mémoire géologique sur le Bassin d'Amiens, et en partienlier sur les Cantons Littoraux de la Somme
(1834)
We present simulations with the Chemical Lagrangian Model of the Stratosphere (CLaMS) for the Arctic winter 2002/2003. We integrated a Lagrangian denitrification scheme into the three-dimensional version of CLaMS that calculates the growth and sedimentation of nitric acid trihydrate (NAT) particles along individual particle trajectories. From those, we derive the HNO3 downward flux resulting from different particle nucleation assumptions. The simulation results show a clear vertical redistribution of total inorganic nitrogen ( ), with a maximum vortex average permanent removal of over 5ppb in late December between 500 and 550K and a corresponding increase of of over 2ppb below about 450K. The simulated vertical redistribution of is compared with balloon observations by MkIV and in-situ observations from the high altitude aircraft Geophysica. Assuming a globally uniform NAT particle nucleation rate of 7.8x10-6cm-3h-1 in the model, the observed denitrification is well reproduced.
In the investigated winter 2002/2003, the denitrification has only moderate impact (≤14%) on the simulated vortex average ozone loss of about 1.1ppm near the 460K level. At higher altitudes, above 600K potential temperature, the simulations show significant ozone depletion through -catalytic cycles due to the unusual early exposure of vortex air to sunlight.
Viertaljahresbericht der Kaiserlichen Hauptwetterwarte von Deutsch-Ostafrika. 1913, 2. Vierteljahr
(1913)
Beilage in: Deutsch-Ostafrikanische Zeitung. April 1913
In weiten Teilen zentraleuropäischer Mittelgebirge wird das anstehende Gestein durch periglaziäre Lagen verhüllt. Diese polygenetisch entwickelten Lockergesteinsdecken sind Schichten im geologisch-sedimentologischen Sinne und das Ausgangsmaterial der Bodenbildung. Ihre Substrateigenschaften, die durch pedogenetische Prozesse lediglich modifiziert werden, beeinflussen maßgeblich die ökologischen Standortbedingungen. Bisher waren nur sehr wenige Informationen zum Aufbau des oberflächennahen Untergrundes und der Böden des hessischen Spessarts vorhanden. Deswegen wurden im Rahmen dieser Arbeit in fünf Untersuchungsgebieten die Verbreitung und Eigenschaften der periglaziären Lagen und Böden mit Hilfe von umfangreichen Geländeuntersuchungen, Laboranalysen und mikromorphologischen Analysen erfasst. Die Ergebnisse belegen die Koppelung verschiedener Bodentypen mit bestimmten Schichtungskombinationen periglaziärer Lagen. Mit Hilfe von Dünnschliffanalysen wird die Wirksamkeit unterschiedlicher bodenbildender Prozesse in den Substraten näher beleuchtet. In lösslehmreichen, lithologisch dreigeteilten Lockergesteinsdecken sind Parabraunerden entwickelt. Die Untersuchung der Bodendünnschliffe offenbart jedoch, dass ein Teil der Tongehaltsdifferenz auf Sedimenteigenschaften der Deckschichten zurückzuführen ist: In der Mittellage finden sich Reste einer Paläobodenbildung in Form von Toncutanbruchstücken und tonigen Aggregaten. Teilweise wurde dieses Material auch bei der Formung der Hauptlage aufgearbeitet und als tonige Aggregate in die schluffige Matrix inkorporiert. Rezente Lessivierungsprozesse maskieren lediglich den schichtungsbedingten Tongehaltsunterschied und damit auch den Einfluss der Paläobodenreste auf die heutige Profilgestalt. In den höher gelegenen Gebieten des Gebirges stellen Braunerden aus Hauptlage über Basislage den am weitesten verbreiteten Bodentyp. Der Lösslehmanteil in der Hauptlage ist gegenüber den Profilen am Westrand des Spessarts deutlich geringer, lösslehmreiche Mittellagen kommen kaum vor. Mikromorphologische Analysen bestätigen Geländebefunde, nach denen sich die Verbraunung auf die lösslehmhaltigen Sedimente (Hauptlage, in die Basislage eingemischtes Hauptlagenmaterial) beschränkt. Lessivierungsprozesse dagegen sind nicht an bestimmte Schichten oder Substrate gebunden: Toneinspülungen sind in allen periglaziären Lagen nachweisbar und die Verlagerung findet schichtübergreifend statt. Sehr viele Bodenprofile zeigen Podsolierungstendenzen, trotzdem bleibt der Braunerdecharakter der Profile bestimmend. Stärkere Podsolierung beschränkt sich auf durch den Menschen in der Vergangenheit stark veränderte Substrate. Weitere Fragestellungen für die Dünnschliffuntersuchungen waren die qualitative Bewertung der Überformungsintensität periglaziärer Lagen durch bioturbate Prozesse sowie die Identifikation von Solumsedimenten, die granulometrisch kaum vom liegenden Hauptlagenmaterial zu unterscheiden sind.
Das Ziel dieser Studie ist es, die Möglichkeiten und Grenzen von hochauflösenden Klimaprojektionen in orographisch beeinflussten Gebieten an den Beispielen der europäischen Alpen und des Himalajas zu prüfen. Insbesondere wird die Fragestellung untersucht, ob beobachtete regionale Muster in den höher aufgelösten Daten besser wiedergegeben werden als in den antreibenden großskaligen Daten. Dazu werden regionale Klimasimulationen des COSMO-CLM Modells und Daten von zwei statistischen Regionalisierungsmethoden mit ERA40 Reanalysen sowie Daten des globalen Atmosphäre-Ozean Modells ECHAM5/MPIOM für verschiedene Parameter des Klimasystems verglichen. Ein Vergleich mit den Reanalysen anhand täglicher Niederschlagsstatistiken ergibt, dass die COSMO-CLM Niederschlagsdaten auf der 0.5° Skala vergleichbar sind mit ERA40 Niederschlägen und mit statistisch regionalisierten ERA40 Niederschlägen. Eine zusätzliche Fehlerkorrektur der COSMO-CLM Niederschläge liefert gute Ergebnisse. Dabei sind jedoch etwa 500 Regentage notwendig, um eine robuste Fehlerabschätzung zu gewährleisten. Für das südasiatische Gebiet ist eine realistische Wiedergabe des indischen Sommermonsuns (ISM) in den Modellen von hoher Relevanz. Betrachtet man nur die Mittelwerte und zeitlichen Variabilitäten von verschiedenen Indizes des ISM, so liefert das COSMO-CLM keinen Mehrwert im Vergleich zu den antreibenden Daten. Allerdings werden die räumlichen Strukturen von Niederschlag und vertikaler Windscherung, sowie die zeitliche Korrelation der modellierten Indizes gegenüber dem ECHAM5/MPIOM Modell verbessert. Die durchgeführten COSMO-CLM Projektionen für die Jahre 1960 bis 2100 zeigen negative Trends des ISM für die SRES Szenarien A2, A1B und B1. Die negativsten Trends sind dabei im Szenario A2 zu finden, gefolgt von A1B und B1. Fast keine Trends zeigen sich im commitment Szenario. Trotz großen zeitlichen Variabilitäten sind die Abnahmen in Niederschlagsmengen, ausgehender langwelliger Strahlung und Windscherung statistisch signifikant in großen Regionen des Simulationsgebietes. Für Nordwest-Indien weisen die Projektionen teilweise einen Rückgang der Monsunniederschläge von über 70% in 100 Jahren auf. Der Rückgang der Windscherung ist hauptsächlich auf Veränderungen in der oberen Troposphäre bei 200 hPa zurück zu führen. Während in den COSMO-CLM Projektionen alle Indizes des ISM synchrone Negativtrends aufweisen, sind die Trends für den Monsunregen über Indien im globalen ECHAM5/MPIOM Model positiv. Gemäß den Definitionen der verschiedenen Indizes, sind jedoch synchrone Trends wahrscheinlicher und das COSMO-CLM liefert zu den globalen ISM Projektionen ebenfalls einen Mehrwert. Insgesamt zeigen die Ergebnisse dieser Studie, dass das COSMO-CLM wertvolle regionale Zusatzinformationen zu den globalen Modellen in den beiden untersuchten Regionen liefert. Für die Einzugsgebiete der oberen Donau und des oberen Brahmaputra liefern die COSMO-CLM Projektionen einen signifikanten Anstieg der Temperatur für alle Jahreszeiten der Jahre 1960 bis 2100. Die Werte sind generell höher im Brahmaputragebiet, mit den größten Trends in der Region des tibetanischen Plateaus. Im Niederschlag zeigen die saisonalen Anteile ebenfalls klare Trends, beispielsweise eine Zunahme des Frühjahrsniederschlags im Einzugsgebiet der oberen Donau. Die größten Trends werden wiederum in der Region des tibetanischen Plateaus projiziert mit einem Anstieg von bis zu 50% in der Länge der Trockenperioden zwischen Juni und September und einem gleichzeitigen Anstieg von etwa 10% für die maximale Niederschlagsmenge an fünf aufeinander folgenden Tagen. Für die Region Assam in Indien, zeigen die Projektionen zudem eine Zunahme von 25% in der Anzahl der aufeinander folgenden trockenen Tage während der Monsunzeit
In this thesis, laboratory investigations have been conducted to investigate several processes occurring during the melt segregation (crystal settling and compaction processes), as well as during emplacement of plutons. With the help of three different sets of centrifuge experiments rates of these three magmatic processes have been evaluated. In the first series of the centrifuge experiments, the diapiric ascent of buoyant material from two source layers at different depths was studied. Through five models, the hypothesis of ascending diapirs was tested and it was demonstrated whether a rising diapir ascends straight upward or if its ascent might be deviated by another buoyant, softer – and consequently easier to travel through – layer which is located within the overburden strata. We were interested under which conditions they can be formed. For this purpose we placed perturbations on top of both the buoyant layers; either with a set-off of both the protrusions (for three of these experiments), or with both protrusion sitting directly on top of each other (for one of the experiments). In the first experiment, we omitted the perturbations, to test which pathways diapirs take which grow from natural Rayleigh-Taylor instabilities. Three others experiments differed in the viscosity contrast between the overburden and the buoyant material. Through the experimental runs, the effects of different overburden viscosities and perturbation positions on the number of the diapirs were observed. The modeling results show that two diapirs rising from the offset perturbations do not take the same pathway through the overburden layer. Rather, each diapir takes a different pathway, with the deeper diapir piercing through its overburden while rising, regardless if it was a buoyant layer or denser overburden layers. However, when the two perturbations were situated directly above each other in the different PDMS layers, this resulted in the formation of one big diapir rather than several smaller ones, and the overburden layer was less deformed than with offset perturbations. Diapiric structures as those derived from the models without perturbation and where the perturbation are offset occur within Great Kavir Basin (Iran), where numerous salt diapirs grew from several salt horizons, which show a similar spatial distribution. The resulting structure observed in the model where the two perturbations situated directly above each other, is close to what is observed in composite batholiths such as the Flasergranitoid Zone within the Bergsträßer Odenwald Crystalline Complex (Germany). The second series of models were aimed to study crystal settling within a magma. For this purpose experiments with an artificial magma of 30 vol% olivine in 70 vol% basaltic melt were conducted to elucidate the formation mechanisms and time scales of gravitational cumulates. Through the experiments, two physical processes have been observed: (i) purely mechanical compaction, and (ii) chemical compaction induced by dissolution and re-precipitation of settled crystals. The results reveals that the mechanical settling of the dense olivine suspension occurs at about 1/6 the speed of simple Stokes settling, and a sedimentation exponent n of 4.1 is found. Evidences of chemical compaction induced by dissolution and re-precipitation of settled crystals have been highlighted by a detailed analysis of the fine structure of olivine grain boundaries. This last has revealed (1) the presence of Ca, which is characteristic only for MORB-melt, at the interface of two adjacent Ol-grains even when no melt is present; (2) a not fully crystallized boundary layer between two adjacent olivine grains. The crystal size distribution curves and the grain size growth exponent n ~3.6 indicate that diffusion controlled Ostwald ripening is the dominant crystal growth mechanism in concentrated magmatic suspensions. Finally, the formation times in natural olivine adcumulates have been calculated. The last series of centrifuge experiments deals with the crystal-melt settling-floating mechanism in a system composed of natural two pyroxene gabbro. The results have revealed a vertical evolution of the major and trace elements in the melt phase. Then, a numerical modelling of the sedimentation process of the crystals has been made in order to describe the compaction evolution with time. In comparing the numerical simulation with the centrifuge modelling, the stratification of the compacted layer in the runs is reproduced in numerical models. Moreover, on the base of the numerical and centrifuge modelling, a sedimentation exponent describing a deviation of settling in concentrated suspensions from Stokes sedimentation has been evaluated. Finally, the numerical simulation is applied to the Muskox intrusion to estimate the formation time and the melt fraction evolution in using the hindered sedimentation model calculations.
IFLS-Journal. Nr. 4, 2003
(2003)
IFLS-Journal. Nr. 3, 2003
(2003)
IFLS-Journal. Nr. 2, 2002
(2002)
IFLS-Journal. Nr. 1, 2002
(2002)
In this study, I investigate the crustal and upper mantle velocity structure beneath the Rwenzori Mountains in western Uganda. This mountain range is situated within the western branch of the East African Rift and reaches altitudes of more than 5000 m. I use four different approaches that belong to the travel-time tomography method. The first approach is based on the isotropic tomographic inversion of local data, which contain information about 2053 earthquakes recorded by a network of up to 35 stations covering an area of 140×90 km2. The LOTOS-09 algorithm described here is used to realize this approach. The second approach is based on the anisotropic tomographic inversion of the same local dataset. This method employs the tomographic code ANITA, developed with my participation, which provides 3D anisotropic P and isotropic S velocity distributions based on P and S travel-times from local seismicity. For the P anisotropic model, four parameters for each parameterization cell are determined. This represents an orthorhombic anisotropy with one vertically-oriented predefined direction. Three of the parameters describe slowness variations along three horizontal orientations with azimuths of 0°, 60° and 120°, and one is a perturbation along the vertical axis. The third approach is based on tomographic inversion of the teleseismic data, which contain information about the traveltimes of P-waves coming from 284 teleseismic events recorded by the seismic network stations. The TELELOTOS code, which is my own modification of the LOTOS-09 algorithm, is used in this approach. The TELELOTOS code is designed to iteratively invert the local and/or teleseismic datasets. Finally, I present the results of the new tomographic approach, which is based on the simultaneous inversion of the joint local and teleseismic data. The simultaneous use of these datasets for the tomographic inversion has several advantages. In this case, the velocity structure in the study area can be resolved as deep as in the teleseismic approach. At the same time, in the upper part of the study volume, the resolution of the obtained models is as good as in the local tomography. The TELELOTOS algorithm is used to perform the joint tomographic inversion. Special attention is paid in this work to synthetic testing. A number of different synthetic and real data tests are performed to estimate the resolution ability and robustness of the obtained models. In particular, synthetic tests have shown that the results of the anisotropic tomographic inversion of the local data have to be considered as unsatisfactory. For all approaches used in this study, I present synthetic models that reproduce the same pattern of anomalies as that obtained by inverting the real data. These models are used to interpret the results and estimate the real amplitudes of the obtained anomalies. The obtained models exhibit a relatively strong negative P anomaly (up to -10%) beneath the Rwenzori Mountains. Low velocities are found in the northeastern part of the array at shallower depths and are most likely related to sedimentary deposits, while higher velocities are found beneath the eastern rift shoulder and are thought to be related to old cratonic crust. The presence of low velocities in the northwestern part of the array may be caused by a magmatic intrusion beneath the Buranga hot springs. Relatively low velocities were observed within the lower crust and upper mantle in the western and southern parts of the study area (beneath the rift valley and the entire length of the Rwenzori range). The higher amplitude of the low-velocity anomaly in the south can be related to the thinner lithosphere in the southern part of the Albertine rift. In the center of the study area, a small negative anomaly is observed, with the intensity increasing with depth. This anomaly is presumably related to a fluids rising up from a plume branch in the deeper part of the mantle. According to the interpretation of the local earthquake distribution, the Rwenzori Mountains are located between two rift valleys with flanks marked by normal faults. The Rwenzori block is bounded by thrust faults that are probably due to compression.