Biogas production in regional integrated biodegradable waste treatment – Possibilities for improving energy performance and reducing GHG emissions

The greatest threat that the biodegradable waste causes on the environment is the methane produced in landfills by the decomposition of this waste. The Landfill Directive (1999/31/EC) aims to reduce the landfilling of biodegradable waste. In Finland, 31% of biodegradable municipal waste ended up into landfills in 2012. The pressure of reducing disposing into landfills is greatly increased by the forthcoming landfill ban on biodegradable waste in Finland. There is a need to discuss the need for increasing the utilization of biodegradable waste in regional renewable energy production to utilize the waste in a way that allows the best possibilities to reduce GHG emissions. The objectives of the thesis are: (1) to find important factors affecting renewable energy recovery possibilities from biodegradable waste, (2) to determine the main factors affecting the GHG balance of biogas production system and how to improve it and (3) to find ways to define energy performance of biogas production systems and what affects it. According to the thesis, the most important factors affecting the regional renewable energy possibilities from biodegradable waste are: the amount of available feedstock, properties of feedstock, selected utilization technologies, demand of energy and material products and the economic situation of utilizing the feedstocks. The biogas production by anaerobic digestion was seen as the main technology for utilizing biodegradable waste in agriculturally dense areas. The main reason for this is that manure was seen as the main feedstock, and it can be best utilized with anaerobic digestion, which can produce renewable energy while maintaining the spreading of nutrients on arable land. Biogas plants should be located close to the heat demand that would be enough to receive the produced heat also in the summer months and located close to the agricultural area where the digestate could be utilized. Another option for biogas use is to upgrade it to biomethane, which would require a location close to the natural gas grid. The most attractive masses for biogas production are municipal and industrial biodegradable waste because of gate fees the plant receives from them can provide over 80% of the income. On the other hand, directing gate fee masses for small-scale biogas plants could make dispersed biogas production more economical. In addition, the combustion of dry agricultural waste such as straw would provide a greater energy amount than utilizing them by anaerobic digestion. The complete energy performance assessment of biogas production system requires the use of more than one system boundary. These can then be used in calculating output–input ratios of biogas production, biogas plant, biogas utilization and biogas production system, which can be used to analyze different parts of the biogas production chain. At the moment, it is difficult to compare different biogas plants since there is a wide variation of definitions for energy performance of biogas production. A more consistent way of analyzing energy performance would allow comparing biogas plants with each other and other recovery systems and finding possible locations for further improvement. Both from the GHG emission balance and energy performance point of view, the energy consumption at the biogas plant was the most significant factor. Renewable energy use to fulfil the parasitic energy demand at the plant would be the most efficient way to reduce the GHG emissions at the plant. The GHG emission reductions could be increased by upgrading biogas to biomethane and displacing natural gas or petrol use in cars when compared to biogas CHP production. The emission reductions from displacing mineral fertilizers with digestate were seen less significant, and the greater N2O emissions from spreading digestate might surpass the emission reductions from displacing mineral fertilizers.

Excavation-drier method of energy-peat extraction reduces long-term climatic impact

Climatic impacts of energy-peat extraction are of increasing concern due to EU emissions trading requirements. A new excavation-drier peat extraction method has been developed to reduce the climatic impact and increase the efficiency of peat extraction. To quantify and compare the soil GHG fluxes of the excavation drier and the traditional milling methods, as well as the areas from which the energy peat is planned to be extracted in the future (extraction reserve area types), soil CO2, CH4 and N2O fluxes were measured during 2006–2007 at three sites in Finland. Within each site, fluxes were measured from drained extraction reserve areas, extraction fields and stockpiles of both methods and additionally from the biomass driers of the excavation-drier method. The Life Cycle Assessment (LCA), described at a principal level in ISO Standards 14040:2006 and 14044:2006, was used to assess the long-term (100 years) climatic impact from peatland utilisation with respect to land use and energy production chains where utilisation of coal was replaced with peat. Coal was used as a reference since in many cases peat and coal can replace each other in same power plants. According to this study, the peat extraction method used was of lesser significance than the extraction reserve area type in regards to the climatic impact. However, the excavation-drier method seems to cause a slightly reduced climatic impact as compared with the prevailing milling method.

Synthesis, properties and characterization of N-Alkyl substituted b-Diketiminato copper(I) Complexes

Le ligand nacnacxylH (xyl = C6Me2H3) et les ligands dikétimines N-alkyle substitués (nacnacCH(Me)PhH, nacnacBnH and nacnaciPrH) ont été préparés avec de bons rendements à l’exception du nacnaciPrH (23%) en utilisant un protocole en une étape et à l’aide d’un montage Dean-Stark. La réaction du S,S-nacnacCH(Me)PhH et du nacnacBnH avec le nBuLi dans le THF conduit au S,S-nacnacCH(Me)PhLi(THF) et au nacnacBnLi(THF). Les tentatives de bromation de ces composés par le N-bromosuccinimide conduisent plutôt aux ligands S,S-succnacnacCH(Me)PhH et succnacnacBnH (succ = succinimido) substitués par un groupement succinimido sur le carbone  La chloration par le N-chlorosuccinimide conduit au produit désiré, mais avec des impuretés. La réaction de ces ligands avec le CuOtBu (ou bien MesCu, où Mes = C6Me3H2, et une quantité catalytique de CuOtBu) en présence de bases de Lewis donne les (nacnacxylCu)2(-toluène), nacnacxylCuCNC6H3(Me)2, nacnacCH(Me)PhCuL (L = PPh3, PMe3, CNC6H3(Me)2, DMAP, lutidine, Py, MeCN), nacnacBnCuL (L = PPh3, CNC6H3(Me)2, styrène, trans-stilbene, phenylvinylether, acrylonitrile, diphenylacetylène), nacnaciPrCuL (L = PPh3, CNC6H3(Me)2, MeCN) et le succnacnacCH(Me)PhCuL (PPh3, CNC6H3(Me)2, pyridine). Tous ces complexes sont jaunes et sensibles à l’air et à l’humidité. En l’absence de fortes bases de Lewis, on n’observe pas de réaction entre les précurseurs de cuivre et les ligands N-alkyle substitués. Les études RMN des complexes dans le C6D6 ne présentent pas de complexe de toluène mais un mélange à l’équilibre du (nacnacxylCu)2(-C6D6) et nacnacxylCu(C6D6) dans une proportion de 2 pour 1. Alors que l’addition de plus de cinquante équivalents soit de THF, soit de toluène n’induit aucun changement des spectres RMN, l’addition de 2 équivalents de MeCN conduit instantanément au complexe nacnacxylCu(MeCN). De plus, le (nacnacxylylCu)2(-C6D6) ne se coordone ni ne réagit avec le N2O, même après avoir été chauffé à 60°C pendant treize jours. En présence de DPA (diphenylacétylène), la réaction du nacnacBnH avec le CuOtBu conduit au dimère ponté (nacnacBnCu)2(µ-DPA). L’addition d’un excès de DPA (10-12 équivalents) transforme le dimère ponté en complexe lié en position terminale nacnacBnCuDPA. Les nacnacRH (R = CH(Me)Ph et i-Pr) ne forment pas de complexe ni avec les oléfines ni avec le DPA. Une réactivité similaire a été observée avec les complexes de nacnacCH(Me)PhCu(NCMe) et nacnaci-PrCu(NCMe). Tandis que le complexe lié en position terminale par MeCN a été isolé et caractérisé, l’équilibre en solution nous laisse suspecter la formation d’un complexe d’acétonitrile ponté. Des études de réactivité comparatives ont été menées sur quelques complexes de cuivre. La Morpholine ne réagit pas avec le nacnacBnCu(acrylonitrile) contrairement à l’acrylonitrile libre. L’expérience de l’échange d’oléfine montre que l’acrylonitrile (une oléfine électro-attractrice) se lie plus fortement que les autres oléfines, mettant ainsi en évidence l’importance de la rétrodonation  face à la donation La rétrodonation est cependant faible comparée aux autres complexes de styrène structurellement caractérisés. Les complexes nacnacCH(Me)PhCuL (L = PPh3 et MeCN) ont été employés dans la cyclopropanation catalytique du styrène et dans l’addition conjuguée du ZnEt2 sur la 2-cyclohexénone, mais les résultats indiquent que le ligand dikétimine est éliminé avant son entrée dans le cycle catalytique. Par conséquent, il n’y a pas d’induction chirale. Les complexes tétra coordinées de cuivre avec les nacnacRCu(phen) (R = Bn, CH(Me)Ph et Phen = 1,10-phenanthroline, 2-Mes-1,10-phenanthroline, 2,9-dimethyl-1,10-phenanthroline (dmp) et 2,9-diphenyl-1,10-phenanthroline (dpp)) ont été synthétisés. Ces complexes sont d’une intense couleur bleue et des interactions d’empilement entre l’un des cycles phényle des ligands nacnac et la phénanthroline ont été observées dans les structures à l’état solide. Les mesures en absorption UV-visible ont été effectuées dans le toluène et les bandes MLCT sont déplacées vers le rouge par rapport à celles des complexes de cuivre et bisphénanthroline. Tous ces composés émettent à l’état solide mais les complexes 1,10-phenanthroline et 2-Mes-1,10-phenanthroline n’émettent pas en solution. Pour renforcer les interactions d’empilement , les nouveaux ligands nacnacRH (R = CH2C6H2(OMe)3, CH2C6F5) et leurs complexes de cuivre respectifs ont été préparés avec du dmp et dpp. Afin de permettre la comparaison, le nacnaciBuCu(dmp) a été synthétisé. Alors que les complexes dmp montrent une augmentation des interactions intramoléculaires - avec les substituants phényle du ligand dikétimine et de la phénanthroline, les complexes dpp ne révèlent pas de telles interactions. Les complexes perfluorés montrent, en absorption et en émission, un déplacement significatif vers le bleu, alors que les complexes substitués par un groupements isobutyle présentent des transitions déplacées vers le rouge. Alors que les intensités de luminescence et les durées de vie sont faibles, les déplacements réduits de Stokes et les pics étroits de luminescence comparables indiquent une réduction des distorsions de l’état excité.

Les transformations microbiennes de l’azote dans les grandes rivières

Les rivières reçoivent de l'azote de leurs bassins versants et elles constituent les derniers sites de transformations des nutriments avant leur livraison aux zones côtières. Les transformations de l’azote inorganique dissous en azote gazeux sont très variables et peuvent avoir un impact à la fois sur l’eutrophisation des côtes et les émissions de gaz à effet de serre à l’échelle globale. Avec l’augmentation de la charge en azote d’origine anthropique vers les écosystèmes aquatiques, les modèles d’émissions de gaz à effet de serre prédisent une augmentation des émissions d’oxyde nitreux (N2O) dans les rivières. Les mesures directes de N2O dans le Lac Saint-Pierre (LSP), un élargissement du Fleuve Saint-Laurent (SLR) indiquent que bien qu’étant une source nette de N2O vers l'atmosphère, les flux de N2O dans LSP sont faibles comparés à ceux des autres grandes rivières et fleuves du monde. Les émissions varient saisonnièrement et inter-annuellement à cause des changements hydrologiques. Les ratios d’émissions N2O: N2 sont également influencés par l’hydrologie et de faibles ratios sont observés dans des conditions de débit d'eau plus élevée et de charge en N élevé. Dans une analyse effectuée sur plusieurs grandes rivières, la charge hydraulique des systèmes semble moduler la relation entre les flux de N2O annuels et les concentrations de nitrate dans les rivières. Dans SLR, des tapis de cyanobactéries colonisant les zones à faible concentration de nitrate sont une source nette d’azote grâce à leur capacité de fixer l’azote atmosphérique (N2). Étant donné que la fixation a lieu pendant le jour alors que les concentrations d'oxygène dans la colonne d'eau sont sursaturées, nous supposons que la fixation de l’azote est effectuée dans des micro-zones d’anoxie et/ou possiblement par des diazotrophes hétérotrophes. La fixation de N dans les tapis explique le remplacement de près de 33 % de la perte de N par dénitrification dans tout l'écosystème au cours de la période d'étude. Dans la portion du fleuve Hudson soumis à la marée, la dénitrification et la production de N2 est très variable selon le type de végétation. La dénitrification est associée à la dynamique en oxygène dissous particulière à chaque espèce durant la marée descendante. La production de N2 est extrêmement élevée dans les zones occupées par les plantes envahissantes à feuilles flottantes (Trapa natans) mais elle est négligeable dans la végétation indigène submergée. Une estimation de la production de N2 dans les lits de Trapa durant l’été, suggère que ces lits représentent une zone très active d’élimination de l’azote. En effet, les grands lits de Trapa ne représentent que 2,7% de la superficie totale de la portion de fleuve étudiée, mais ils éliminent entre 70 et 100% de l'azote total retenu dans cette section pendant les mois d'été et contribuent à près de 25% de l’élimination annuelle d’azote.

Significance of soil microorganisms with special reference to climate change

There are a large number of agronomic-ecological interactions that occur in a world with increasing levels of CO2, higher temperatures and a more variable climate. Climate change and the associated severe problems will alter soil microbial populations and diversity. Soils supply many atmospheric green house gases by performing as sources or sinks. The most important of these gases include CH4, CO2 and N2O. Most of the green house gases production and consumption processes in soil are probably due to microorganisms. There is strong inquisitiveness to store carbon (C) in soils to balance global climate change. Microorganisms are vital to C sequestration by mediating putrefaction and controlling the paneling of plant residue-C between CO2 respiration losses or storage in semi-permanent soil-C pools. Microbial population groups and utility can be manipulated or distorted in the course of disturbance and C inputs to either support or edge the retention of C. Fungi play a significant role in decomposition and appear to produce organic matter that is more recalcitrant and favor long-term C storage and thus are key functional group to focus on in developing C sequestration systems. Plant residue chemistry can influence microbial communities and C loss or flow into soil C pools. Therefore, as research takings to maximize C sequestration for agricultural and forest ecosystems - moreover plant biomass production, similar studies should be conducted on microbial communities that considers the environmental situations

Fütterungsbedingte mikrobielle Zusammensetzung von Rinderkot und deren Einfluss auf Gasemissionen und N-Mineralisierung im Boden

Um die Nährstoffeffizienz im Boden zu erhöhen und klimarelevante Gasemissionen zu minimieren, sind quantitative Informationen zu den C- und N-Fraktionen im Kot sowie deren Mineralisierungspotential nötig. Da über die Hälfte des fäkalen N mikrobiell gebunden ist, sind Methoden zur Bestimmung der mikrobiellen Kotqualität hilfreich. Ziele der ersten Publikation waren die Anwendung der CFE-Methode zur Bestimmung der mikrobiellen Biomasse in Rinderkot, Ergosterolbestimmung als Marker für die pilzliche Biomasse und Aminozuckernachweis zur Analyse der mikrobiellen Gemeinschaftsstruktur (pilzliches Glucosamin und bakterielle Muramin-säure). Mit Hilfe der CFE-Methode sollten lebende Mikroorganismen im Kot, inklusive Bakterien, Pilze und Archaeen, erfasst werden. Verschiedene Extraktionsmittel wurden für diese Methode getestet, um stabile Extrakte und reproduzierbare mikrobielle Biomasse-C- und -N-Gehalte zu erhalten. Der Einsatz von 0.05 M CuSO4 als Extraktionsmittel löste vorherige Probleme mit der Extraktion CHCl3-labiler N-Komponenten und sorgte für stabile Kotextrakte. Die Methoden wurden in einem Kotinkubationsexperiment bei 25 °C verglichen. Mikrobielle Parameter zeigten dynamische Charakteristika und mögliche Verschiebungen innerhalb der mikrobiellen Gemeinschaft. Im Kot von Färsen betrug das mittlere C/N-Verhältnis 5,6 und der mittlere Cmik/Corg-Quotient 2,2%, das Verhältnis von Ergosterol zum mikrobiellen Biomasse-C war 1,1‰. Ergosterol und Aminozuckeranalyse ergaben einen signifikanten Pilzanteil von über 40% des mikrobiellen Gesamt-C. Für die Analyse mikrobieller Parameter in Rinderkot erwiesen sich alle getesteten Methoden als geeignet. Diese wurden für die folgenden Fütterungsversuche weiter unabhängig voneinander angewendet und verglichen. Die zweite Publikation verglich eine N-defizitäre (ND) und eine ausgeglichene N-Bilanz (NB) bei der Fütterung von Milchkühen unter Berücksichtigung der Kot-inhaltsstoffe, der mikrobiellen Parameter und der Verdaulichkeit. Unterschiede zwischen Individuen und Probennahmetagen wurden ebenfalls miteinbezogen. Mittlerer mikrobieller Biomasse-C- und -N-Gehalt war 37 bzw. 4,9 mg g-1 TM. Der Pilzanteil lag diesmal bei 25% des mikrobiellen Gesamt-C. Die Fütterung zeigte signifikante Effekte auf die Kotzusammensetzung. Das fäkale C/N-Verhältnis der NB-Fütterung war signifikant niedriger als bei ND. Gleiches gilt für das C/N-Verhältnis der mikrobiellen Biomasse mit jeweils 9.1 und 7.0 für ND und NB. Auch die Verdaulichkeit wurde durch die Fütterung beeinflusst. Unverdauter Futterstickstoff, Faserstoffe (NDF) und Hemi-cellulose waren in der ND-Behandlung signifikant erhöht. Einige Parameter zeigten nur einen Einfluss der Probennahmetage, mit den angewendeten Methoden gelang jedoch der eindeutige Nachweis der Fütterungseffekte auf mikrobielle Parameter im Rinderkot, wobei sich die Fütterung in nur einer Variable unterschied. Weitere Fütterungseinflüsse auf die Kotqualität wurden schließlich auch für Rinder unterschiedlicher Leistungsstufen erforscht. Hier waren die Unterschiede in der Fütterung wesentlich größer als in den vorhergehenden Experimenten. Der Kot von Färsen, Niederleistungs- und Hochleistungskühen sowie dessen Einfluss auf N2O-Emissionen, N-Mineralisierung und pflanzliche N-Aufnahme wurden untersucht. Die Färsenfütterung mit geringem N- und hohem ADF-Anteil führte zu pilzdominiertem Kot. Besonders im Vergleich zum Kot der Hochleistungskühe war der Gehalt an mikrobiellem Biomasse-C niedrig, in Verbindung mit einem breiten mikrobiellen C/N-Verhältnis und hohem Ergosterolgehalt. Eingemischt in Boden zeigte Färsenkot die niedrigste CO2-Produktion und höchste N-Immobilisierung sowie niedrigste N2O-Emissionen während einer 14-tägigen Inkubation bei 22 °C. In einem 62-Tage-Gefäßversuch mit Welschem Weidelgras waren der Trocken-masseertrag und die pflanzliche Stickstoffaufnahme in den Färsenbehandlungen am niedrigsten. Die Stickstoffaufnahme durch die Pflanzen korrelierte positiv mit der Stickstoffkonzentration im Kot und negativ mit dem Rohfasergehalt, aber auch negativ mit dem C/N-Verhältnis der mikrobiellen Biomasse und dem Verhältnis von pilzlichem zu bakteriellem C. Mikrobielle Parameter im Kot zeigten einen größeren Zusammen-hang mit der pflanzlichen Stickstoffaufnahme als die mikrobiellen Bodenparameter.

Application of biogas slurries from energy crops to arable soils and their impact on carbon and nitrogen dynamics

The use of renewable primary products as co-substrate or single substrate for biogas production has increased consistently over the last few years. Maize silage is the preferential energy crop used for fermentation due to its high methane (CH4) yield per hectare. Equally, the by-product, namely biogas slurry (BS), is used with increasing frequency as organic fertilizer to return nutrients to the soil and to maintain or increase the organic matter stocks and soil fertility. Studies concerning the application of energy crop-derived BS on the carbon (C) and nitrogen (N) mineralization dynamics are scarce. Thus, this thesis focused on the following objectives: I) The determination of the effects caused by rainfall patterns on the C and N dynamics from two contrasting organic fertilizers, namely BS from maize silage and composted cattle manure (CM), by monitoring emissions of nitrous oxide (N2O), carbon dioxide (CO2) and CH4 as well as leaching losses of C and N. II) The investigation of the impact of differences in soil moisture content after the application of BS and temperature on gaseous emissions (CO2, N2O and CH4) and leaching of C and N compounds. III) A comparison of BS properties obtained from biogas plants with different substrate inputs and operating parameters and their effect on C and N dynamics after application to differently textured soils with varying application rates and water contents. For the objectives I) and II) two experiments (experiment I and II) using undisturbed soil cores of a Haplic Luvisol were carried out. Objective III) was studied on a third experiment (experiment III) with disturbed soil samples. During experiment I three rainfall patterns were implemented including constant irrigation, continuous irrigation with periodic heavy rainfall events, and partial drying with rewetting periods. Biogas slurry and CM were applied at a rate of 100 kg N ha-1. During experiment II constant irrigation and an irrigation pattern with partial drying with rewetting periods were carried out at 13.5°C and 23.5°C. The application of BS took place either directly before a rewetting period or one week after the rewetting period stopped. Experiment III included two soils of different texture which were mixed with ten BS’s originating from ten different biogas plants. Treatments included low, medium and high BS-N application rates and water contents ranging from 50% to 100% of water holding capacity (WHC). Experiment I and II showed that after the application of BS cumulative N2O emissions were 4 times (162 mg N2O-N m-2) higher compared to the application of CM caused by a higher content of mineral N (Nmin) in the form of ammonium (NH4+) in the BS. The cumulative emissions of CO2, however, were on the same level for both fertilizers indicating similar amounts of readily available C after composting and fermentation of organic material. Leaching losses occurred predominantly in the mineral form of nitrate (NO3-) and were higher in BS amended soils (9 mg NO3--N m-2) compared to CM amended soils (5 mg NO3--N m-2). The rainfall pattern in experiment I and II merely affected the temporal production of C and N emissions resulting in reduced CO2 and enhanced N2O emissions during stronger irrigation events, but showed no effect on the cumulative emissions. Overall, a significant increase of CH4 consumption under inconstant irrigation was found. The time of fertilization had no effect on the overall C and N dynamics. Increasing temperature from 13.5°C to 23.5°C enhanced the CO2 and N2O emissions by a factor of 1.7 and 3.7, respectively. Due to the increased microbial activity with increasing temperature soil respiration was enhanced. This led to decreasing oxygen (O2) contents which in turn promoted denitrification in soil due to the extension of anaerobic microsites. Leaching losses of NO3- were also significantly affected by increasing temperature whereas the consumption of CH4 was not affected. The third experiment showed that the input materials of biogas plants affected the properties of the resulting BS. In particular the contents of DM and NH4+ were determined by the amount of added plant biomass and excrement-based biomass, respectively. Correlations between BS properties and CO2 or N2O emissions were not detected. Solely the ammonia (NH3) emissions showed a positive correlation with NH4+ content in BS as well as a negative correlation with the total C (Ct) content. The BS-N application rates affected the relative CO2 emissions (% of C supplied with BS) when applied to silty soil as well as the relative N2O emissions (% of N supplied with BS) when applied to sandy soil. The impacts on the C and N dynamics induced by BS application were exceeded by the differences induced by soil texture. Presumably, due to the higher clay content in silty soils, organic matter was stabilized by organo-mineral interactions and NH4+ was adsorbed at the cation exchange sites. Different water contents induced highest CO2 emissions and therefore optimal conditions for microbial activity at 75% of WHC in both soils. Cumulative nitrification was also highest at 75% and 50% of WHC whereas the relative N2O emissions increased with water content and showed higher N2O losses in sandy soils. In summary it can be stated that the findings of the present thesis confirmed the high fertilizer value of BS’s, caused by high concentrations of NH4+ and labile organic compounds such as readily available carbon. These attributes of BS’s are to a great extent independent of the input materials of biogas plants. However, considerably gaseous and leaching losses of N may occur especially at high moisture contents. The emissions of N2O after field application corresponded with those of animal slurries.

Effects of tillage intensity on soil C, N, and P pools with different stability

Es ist bekannt, dass die Umsatzdynamik der organischen Substanz von der Bodenbearbeitungsintensität abhängt. Bis jetzt sind nur wenige Daten zum Einfluss der Bearbeitungsintensität und des Zwischenfruchtanbaus auf C-, N-, und P-Dynamik im Ober- (0-5 cm Tiefe) und Unterboden (5-25 cm Tiefe) von Lössböden verfügbar. Hauptziele dieser Arbeit waren die (i) Quantifizierung des Einflusses von verschiedenen langzeitig durchgeführten Bearbeitungssystemen auf labile, intermediäre, und passive C- und N-Pools; (ii) Quantifizierung des Einflusses dieser Systeme auf P-Fraktionen mit unterschiedlicher Verfügbarkeit für die Pflanzenaufnahme; (iii) Quantifizierung des Einflusses des Zwischenfruchtanbaus in Verbindung mit einer unterschiedlichen Einarbeitungstiefe der der Zwischenfrüchte auf mineralisierbares C und N. Die Ergebnisse des 1. und 2. Teilexperiments basieren auf Untersuchungen von 4 Langzeitfeldexperimenten (LFE) in Ost- und Süddeutschland, die zwischen 1990 und 1997 durch das Institut für Zuckerrübenforschung angelegt wurden. Jedes LFE umfasst 3 Bearbeitungssysteme: konventionelle Bearbeitung (CT), reduzierte Bearbeitung (RT) und Direktsaat (NT). Die Ergebnisse des 3. Teilexperiments basieren auf einem Inkubationsexperiment. Entsprechend den Hauptfragestellungen wurden folgende Untersuchungsergebnisse beschrieben: (i) Im Oberboden von NT wurden höhere labile C-Vorräte gefunden (C: 1.76 t ha-1, N: 166 kg ha-1), verglichen mit CT (C: 0.44 t ha-1, N: 52 kg ha-1). Im Gegensatz dazu waren die labile- C-Vorräte höher im Unterboden von CT mit 2.68 t ha-1 verglichen zu NT mit 2 t ha-1 und RT mit 1.87 t ha-1. Die intermediären C-Vorräte betrugen 73-85% der gesamten organischen C-Vorräte, intermediäre N-Vorräte betrugen 70-95% des Gesamt-N im Ober- und Unterboden und waren vielfach größer als die labilen und passiven C- und N-Vorräte. Nur im Oberboden konnte ein Effekt der Bearbeitungsintensität auf die intermediären N-Pools mit höheren Vorräten unter NT als CT festgestellt werden. Die passiven C- und N-Pools waren eng mit den mineralischen Bodeneigenschaften verbunden und unabhängig vom Bearbeitungssystem. Insgesamt hat sich gezeigt, dass 14 bis 22 Jahre durchgängige Direktsaatverfahren nur im Oberboden zu höheren labilen C- und N-Vorräten führen, verglichen zu konventionellen Systemen. Dies lässt eine tiefenabhängige Stärke der Dynamik der organischen Bodensubstanz vermuten. (ii) Die Konzentration des Gesamt-P (Pt) im Oberboden war höher in NT (792 mg kg-1) und ~15% höher als die Pt-Konzentration in CT (691 mg kg 1). Die Abnahme der Pt-Konzentration mit zunehmender Bodentiefe war höher in NT als in CT. Dies gilt auch für die einzelnen P-Fraktionen, ausgenommen der stabilsten P-Fraktion (residual-P). Generell hatte das Bearbeitungssystem nur einen kleinen Einfluss auf die P-Konzentration mit höheren Pt-Konzentrationen in Böden unter NT als CT. Dies resultiert vermutlich aus der flacheren Einarbeitung der Pflanzenreste als in CT. (iii) Im Zwischenfruchtexperiment war der Biomassezuwachs von Senf am höchsten und nimmt in der Reihenfolge ab (oberirdischer Ertrag in t / ha): Senf (7.0 t ha-1) > Phacelia (5.7 t ha-1) > Ölrettich (4.4 t ha-1). Damit war potentiell mineralisierbares C und N am höchsten in Böden mit Senfbewuchs. Kumulative CO2- und N2O-Emissionen während der Inkubation unterschieden sich nicht signifikant zwischen den Zwischenfruchtvarianten und waren unabhängig von der Verteilung der Pflanzenreste im Boden. Die kumulativen ausgewaschenen mineralisierten N (Nmin)-Vorräte waren in den brachliegenden Böden am höchsten. Die Nmin-Vorräte waren 51-72% niedriger in den Varianten mit Zwischenfrucht und Einarbeitung verglichen zur Brache. In den Varianten ohne Einarbeitung waren die Nmin-Vorräte 36-55% niedriger verglichen zur Brache. Dies weißt auf einen deutlichen Beitrag von Zwischenfrüchten zur Reduzierung von Nitrat-Auswaschung zwischen Winter und Frühjahr hin. Insgesamt führte reduzierte Bearbeitung zu einer Sequestrierung von C und N im Boden und der Zwischenfruchtanbau führte zu reduzierten N-Verlusten. Die P-Verfügbarkeit war höher unter Direktsaat verglichen zur konventionellen Bearbeitung. Diese Ergebnisse resultieren aus den höheren Konzentrationen der OS in den reduzierten, als in den konventionellen Systemen. Die Ergebnisse zeigen deutlich das Potential von reduzierter Bearbeitung zur Sequestrierung von intermediärem C und N zur Reduzierung von klimarelevanten Treibhausgasen. Gleichzeitig steigen die Konzentrationen an pflanzenverfügaren P-Gehalten. Zwischenfrüchte führen auch zu einem Anstieg der C- und N-Vorräte im Boden, offensichtlich unabhängig von der Zwischenfruchtart.

Effects of transformation processes in 'jubraka' agroforestry systems of the Nuba Mountains, Sudan, on nutrient fluxes

Intensification processes in homegardens of the Nuba Mountains, Sudan, raise concerns about strongly positive carbon (C) and nutrient balances which are expected to lead to substantial element losses from these agroecosystems, in particular via soil gaseous emissions. Therefore, this thesis aimed at the quantification of C, nitrogen (N), phosphorus (P) and potassium (K) input and output fluxes with a special focus on soil gaseous losses, and the calculation of respective element balances. A further focus in this thesis was rainfall, a valuable resource for rain-fed agriculture in the Nuba Mountains. To minimize negative consequences of the high variability of rainfall, risk reducing mechanisms were developed by rain-fed farmers that may lose their efficacy in the course of climate change effects predicted for East Africa. Therefore, the second objective of this study was to examine possible changes in rainfall amounts during the last 60 years and to provide reliable risk and probability statements of rainfall-induced events of agricultural importance to rain-fed farmers in the Nuba Mountains. Soil gaseous emissions of C (in form of CO2) and N (in form of NH3 and N2O) of two traditional and two intensified homegardens were determined with a portable dynamic closed chamber system. For C gaseous emission rates reached their peak at the onset of the rainy season (2,325 g CO2-C ha-1 h-1 in an intensified garden type) and for N during the rainy season (16 g NH3-N ha-1 h-1 and 11.3 g N2O-N ha-1 h-1, in a traditional garden type). Data indicated cumulative annual emissions of 5,893 kg CO2-C ha-1, 37 kg NH3-N ha-1, and 16 kg N2O-N ha-1. For the assessment of the long-term productivity of the two types of homegardens and the identification of pathways of substantial element losses, a C and nutrient budget approach was used. In three traditional and three intensified homegardens observation plots were selected. The following variables were quantified on each plot between June and December in 2010: soil amendments, irrigation, biomass removal, symbiotic N2 fixation, C fixation by photosynthesis, atmospheric wet and dry deposition, leaching and soil gaseous emissions. Annual balances for C and nutrients amounted to -21 kg C ha-1, -70 kg N ha-1, 9 kg P ha-1 and -117 kg K ha-1 in intensified homegardens and to -1,722 kg C ha-1, -167 kg N ha-1, -9 kg P ha-1 and -74 kg K ha-1 in traditional homegardens. For the analysis of rainfall data, the INSTAT+ software allowed to aggregate long-term daily rainfall records from the Kadugli and Rashad weather stations into daily, monthly and annual intervals and to calculate rainfall-induced events of agricultural importance. Subsequently, these calculated values and events were checked for possible monotonic trends by Mann-Kendall tests. Over the period from 1970 to 2009, annual rainfall did not change significantly for either station. However, during this period an increase of low rainfall events coinciding with a decline in the number of medium daily rainfall events was observed in Rashad. Furthermore, the availability of daily rainfall data enabled frequency and conditional probability calculations that showed either no statistically significant changes or trends resulting only in minor changes of probabilities.

Nitrosospira spp. can produce nitrous oxide via a nitrifier denitrification pathway

Nitrous oxide (N2O) emission from soils is a major contributor to the atmospheric loading of this potent greenhouse gas. It is thought that autotrophic ammonia oxidizing bacteria (AOB) are a significant source of soil-derived N2O and a denitrification pathway (i.e. reduction of NO2- to NO and N2O), so-called nitrifier denitrification, has been demonstrated as a N2O production mechanism in Nitrosomonas europaea. It is thought that Nitrosospira spp. are the dominant AOB in soil, but little information is available on their ability to produce N2O or on the existence of a nitrifier denitrification pathway in this lineage. This study aims to characterize N2O production and nitrifier denitrification in seven strains of AOB representative of clusters 0, 2 and 3 in the cultured Nitrosospira lineage. Nitrosomonas europaea ATCC 19718 and ATCC 25978 were analysed for comparison. The aerobically incubated test strains produced significant (P < 0.001) amounts of N2O and total N2O production rates ranged from 2.0 amol cell(-1) h(-1), in Nitrosospira tenuis strain NV12, to 58.0 amol cell(-1) h(-1), in N. europaea ATCC 19718. Nitrosomonas europaea ATCC 19718 was atypical in that it produced four times more N2O than the next highest producing strain. All AOB tested were able to carry out nitrifier denitrification under aerobic conditions, as determined by production of N-15-N2O from applied N-15-NO2-. Up to 13.5% of the N2O produced was derived from the exogenously applied N-15-NO2-. The results suggest that nitrifier denitrification could be a universal trait in the betaproteobacterial AOB and its potential ecological significance is discussed.

Tracer correlations in the northern high latitude lowermost stratosphere: Influence of cross‐tropopause mass exchange

We present an analysis of trace gas correlations in the lowermost stratosphere. In‐situ aircraft measurements of CO, N2O, NOy and O3, obtained during the STREAM 1997 winter campaign, have been used to investigate the role of cross‐tropopause mass exchange on tracer‐tracer relations. At altitudes several kilometers above the local tropopause, undisturbed stratospheric air was found with NOy/NOy * ratios close to unity, NOy/O3 about 0.003–0.006 and CO mixing ratios as low as 20 ppbv (NOy * is a proxy for total reactive nitrogen derived from NOy–N2O relations measured in the stratosphere). Mixing of tropospheric air into the lowermost stratosphere has been identified by enhanced ratios of NOy/NOy * and NOy/O3, and from scatter plots of CO versus O3. The enhanced NOy/O3 ratio in the lowermost stratospheric mixing zone points to a reduced efficiency of O3 formation from aircraft NOx emissions.

Methylene spacer-regulated structural variation in cobalt(II/III) complexes with bridging acetate and Salen- or Salpn-type Schiff-base ligands

Two linear, trinuclear mixed-valence complexes, [Co-II{(mu-L-1)(mu-OAc)Co-III (OAc)}(2)] (1) and [Co-II(mu-L-2) (mu-OAc)Co-III(OAc)}(2)] (2) and two mononuclear Con' complexes [Co-III{L-3)(OAc)] (3), and [Co-III {L-4}(OAc)] (4) were prepared and the molecular structures of 1, 2 and 4 elucidated on the basis of X-ray crystallography [OAc = Acetate ion, H2L1 = H(2)Salen 1,6-bis(2-hydroxyphenyl)-2,5-diazahexa-1,5-diene, H2L2 H2Me2-Salen = 2,7-bis(2-hydroxyphenyl)-2,6-diazaocta-2,6-diene, H2L3 = H(2)Salpn = 1,7-bis(2-hydroxyphenyl)-2,6-diazahepta1,6-diene, H2L4 = H(2)Me(2)Salpn = 2,8-bis(2-hydroxyphenyl)3,7-diazanona-2,7-dienel. In complexes I and 2, the acetate groups show both monodentate and bridging bidentate coordination modes, whereas chelating bidentate acetate is present in 4. The terminal (CoN2O4)-N-III centres in 1 and 2 exhibit uniform facial arrangements of both non-bridged N2O and bridging O-3 donor sets and the Co-II centre is coordinated to six (four phenoxo and two acetato) oxygen atoms of the bridging ligands. The effective magnetic moment at room temperature corresponds to the presence of high-spin Coll in both 1 and 2. The complexes 1 and 2 are thus Co-III(S = 0)Co-II(S = 3/2)-Co-II(S = 0) trimers. Complexes 3 and 4 are monomeric and diamagnetic containing low-spin Co-III(S = 0) with chelating tetradentate Schiff base and bidentate acetate. Calculations based on DFT rationalise the formation of trinuclear or monomiclear complexes. (C) Wiley-VCH Verlag GmbH & Co. KGaA, 69451 Weinheim, Germany, 2008).

IR spectrum and radiative forcing of CF4 revisited

Carbon tetrafluoride (CF4) is included as a greenhouse gas within the Kyoto Protocol. There are significant discrepancies in the reported integrated infrared (IR) absorption cross section of CF4 leading to uncertainty in its contribution to climate change. To reduce this uncertainty, the IR spectrum of CF4 was measured in two different laboratories, in 0 933 hPa of air diluent at 296 +/- 2K over the wavelength range 600-3700 cm(-1) using spectral resolutions of 0.03 or 0.50 cm(-1). There was no discernable effect of diluent gas pressure or spectral resolution on the integrated IR absorption, and a value of the integrated absorption cross section of (1.90 +/- 0.17) x 10(-16) cm(2) molecule(-1) cm(-1) was derived. The radiative efficiency (radiative forcing per ppbv) and GWP (relative to CO2) of CF4 were calculated to be 0.102 W m(-2) ppbv(-1) and 7200 (100 year time horizon). The GWP for CF4 calculated herein is approximately 30% greater than that given by the Intergovernmental Panel on Climate Change (IPCC) [ 2002] partly due to what we believe to be an erroneously low value for the IR absorption strength of CF4 assumed in the calculations adopted by the IPCC. The radiative efficiency of CF4 is predicted to decrease by up to 40% as the CF4 forcing starts to saturate and overlapping absorption by CH4, H2O, and N2O in the atmosphere increases over the period 1750-2100. The radiative forcing attributable to increased CF4 levels in the atmosphere from 1750 to 2000 is estimated to be 0.004 W m(-2) and is predicted to be up to 0.033 W m(-2) from 2000 to 2100, dependent on the scenario.

Model car-exhaust catalyst studied by TPD and TP-RAIRS: Surface reactions of NO on clean and O-covered Ir{100}

The adsorption of NO on Ir{100} has been studied as a function of NO coverage and temperature using temperature programmed reflection absorption infrared spectroscopy (TP-RAIRS), low energy electron diffraction (LEED) and temperature programmed desorption (TPD). After saturating the clean (1 x 5)-reconstructed surface with NO at 95 K. two N-2, desorption peaks are observed upon heating. The first N-2 peak at 346 K results from the decomposition of bridge-bonded NO, and the second at 475 K from the decomposition of atop-bonded NO molecules. NO decomposition is proposed to be the rate limiting step for both N-2 desorption states. For high NO coverages on the (1 x 5) surface, the narrow width of the first N-2 desorption peak is indicative of an autocatalytic process for which the parallel formation of N2O appears to be the crucial step. When NO is adsorbed on the metastable unreconstructed (1 x 1) phase of clean Ir{100} N-2 desorption starts at lower temperatures, indicating that this surface modification is more reactive. When a high coverage of oxygen, near 0.5 ML, is pre-adsorbed on the surface, the decomposition of NO is inhibited and mainly desorption of intact NO is observed.

Report of the 2010 assessment of the scientific assessment panel: future ozone and its impact on surface UV

SCIENTIFIC SUMMARY Globally averaged total column ozone has declined over recent decades due to the release of ozone-depleting substances (ODSs) into the atmosphere. Now, as a result of the Montreal Protocol, ozone is expected to recover from the effects of ODSs as ODS abundances decline in the coming decades. However, a number of factors in addition to ODSs have led to and will continue to lead to changes in ozone. Discriminating between the causes of past and projected ozone changes is necessary, not only to identify the progress in ozone recovery from ODSs, but also to evaluate the effectiveness of climate and ozone protection policy options. Factors Affecting Future Ozone and Surface Ultraviolet Radiation • At least for the next few decades, the decline of ODSs is expected to be the major factor affecting the anticipated increase in global total column ozone. However, several factors other than ODS will affect the future evolution of ozone in the stratosphere. These include changes in (i) stratospheric circulation and temperature due to changes in long-lived greenhouse gas (GHG) abundances, (ii) stratospheric aerosol loading, and (iii) source gases of highly reactive stratospheric hydrogen and nitrogen compounds. Factors that amplify the effects of ODSs on ozone (e.g., stratospheric aerosols) will likely decline in importance as ODSs are gradually eliminated from the atmosphere. • Increases in GHG emissions can both positively and negatively affect ozone. Carbon dioxide (CO2)-induced stratospheric cooling elevates middle and upper stratospheric ozone and decreases the time taken for ozone to return to 1980 levels, while projected GHG-induced increases in tropical upwelling decrease ozone in the tropical lower stratosphere and increase ozone in the extratropics. Increases in nitrous oxide (N2O) and methane (CH4) concentrations also directly impact ozone chemistry but the effects are different in different regions. • The Brewer-Dobson circulation (BDC) is projected to strengthen over the 21st century and thereby affect ozone amounts. Climate models consistently predict an acceleration of the BDC or, more specifically, of the upwelling mass flux in the tropical lower stratosphere of around 2% per decade as a consequence of GHG abundance increases. A stronger BDC would decrease the abundance of tropical lower stratospheric ozone, increase poleward transport of ozone, and could reduce the atmospheric lifetimes of long-lived ODSs and other trace gases. While simulations showing faster ascent in the tropical lower stratosphere to date are a robust feature of chemistry-climate models (CCMs), this has not been confirmed by observations and the responsible mechanisms remain unclear. • Substantial ozone losses could occur if stratospheric aerosol loading were to increase in the next few decades, while halogen levels are high. Stratospheric aerosol increases may be caused by sulfur contained in volcanic plumes entering the stratosphere or from human activities. The latter might include attempts to geoengineer the climate system by enhancing the stratospheric aerosol layer. The ozone losses mostly result from enhanced heterogeneous chemistry on stratospheric aerosols. Enhanced aerosol heating within the stratosphere also leads to changes in temperature and circulation that affect ozone. • Surface ultraviolet (UV) levels will not be affected solely by ozone changes but also by the effects of climate change and by air quality change in the troposphere. These tropospheric effects include changes in clouds, tropospheric aerosols, surface reflectivity, and tropospheric sulfur dioxide (SO2) and nitrogen dioxide (NO2). The uncertainties in projections of these factors are large. Projected increases in tropospheric ozone are more certain and may lead to reductions in surface erythemal (“sunburning”) irradiance of up to 10% by 2100. Changes in clouds may lead to decreases or increases in surface erythemal irradiance of up to 15% depending on latitude. Expected Future Changes in Ozone Full ozone recovery from the effects of ODSs and return of ozone to historical levels are not synonymous. In this chapter a key target date is chosen to be 1980, in part to retain the connection to previous Ozone Assessments. Noting, however, that decreases in ozone may have occurred in some regions of the atmosphere prior to 1980, 1960 return dates are also reported. The projections reported on in this chapter are taken from a recent compilation of CCM simulations. The ozone projections, which also form the basis for the UV projections, are limited in their representativeness of possible futures since they mostly come from CCM simulations based on a single GHG emissions scenario (scenario A1B of Emissions Scenarios. A Special Report of Working Group III of the Intergovernmental Panel on Climate Change, Cambridge University Press, 2000) and a single ODS emissions scenario (adjusted A1 of the previous (2006) Ozone Assessment). Throughout this century, the vertical, latitudinal, and seasonal structure of the ozone distribution will be different from what it was in 1980. For this reason, ozone changes in different regions of the atmosphere are considered separately. • The projections of changes in ozone and surface clear-sky UV are broadly consistent with those reported on in the 2006 Assessment. • The capability of making projections and attribution of future ozone changes has been improved since the 2006 Assessment. Use of CCM simulations from an increased number of models extending through the entire period of ozone depletion and recovery from ODSs (1960–2100) as well as sensitivity simulations have allowed more robust projections of long-term changes in the stratosphere and of the relative contributions of ODSs and GHGs to those changes. • Global annually averaged total column ozone is projected to return to 1980 levels before the middle of the century and earlier than when stratospheric halogen loading returns to 1980 levels. CCM projections suggest that this early return is primarily a result of GHG-induced cooling of the upper stratosphere because the effects of circulation changes on tropical and extratropical ozone largely cancel. Global (90°S–90°N) annually averaged total column ozone will likely return to 1980 levels between 2025 and 2040, well before the return of stratospheric halogens to 1980 levels between 2045 and 2060. • Simulated changes in tropical total column ozone from 1960 to 2100 are generally small. The evolution of tropical total column ozone in models depends on the balance between upper stratospheric increases and lower stratospheric decreases. The upper stratospheric increases result from declining ODSs and a slowing of ozone destruction resulting from GHG-induced cooling. Ozone decreases in the lower stratosphere mainly result from an increase in tropical upwelling. From 1960 until around 2000, a general decline is simulated, followed by a gradual increase to values typical of 1980 by midcentury. Thereafter, although total column ozone amounts decline slightly again toward the end of the century, by 2080 they are no longer expected to be affected by ODSs. Confidence in tropical ozone projections is compromised by the fact that simulated decreases in column ozone to date are not supported by observations, suggesting that significant uncertainties remain. • Midlatitude total column ozone is simulated to evolve differently in the two hemispheres. Over northern midlatitudes, annually averaged total column ozone is projected to return to 1980 values between 2015 and 2030, while for southern midlatitudes the return to 1980 values is projected to occur between 2030 and 2040. The more rapid return to 1980 values in northern midlatitudes is linked to a more pronounced strengthening of the poleward transport of ozone due to the effects of increased GHG levels, and effects of Antarctic ozone depletion on southern midlatitudes. By 2100, midlatitude total column ozone is projected to be above 1980 values in both hemispheres. • October-mean Antarctic total column ozone is projected to return to 1980 levels after midcentury, later than in any other region, and yet earlier than when stratospheric halogen loading is projected to return to 1980 levels. The slightly earlier return of ozone to 1980 levels (2045–2060) results primarily from upper stratospheric cooling and resultant increases in ozone. The return of polar halogen loading to 1980 levels (2050–2070) in CCMs is earlier than in empirical models that exclude the effects of GHG-induced changes in circulation. Our confidence in the drivers of changes in Antarctic ozone is higher than for other regions because (i) ODSs exert a strong influence on Antarctic ozone, (ii) the effects of changes in GHG abundances are comparatively small, and (iii) projections of ODS emissions are more certain than those for GHGs. Small Antarctic ozone holes (areas of ozone <220 Dobson units, DU) could persist to the end of the 21st century. • March-mean Arctic total column ozone is projected to return to 1980 levels two to three decades before polar halogen loading returns to 1980 levels, and to exceed 1980 levels thereafter. While CCM simulations project a return to 1980 levels between 2020 and 2035, most models tend not to capture observed low temperatures and thus underestimate present-day Arctic ozone loss such that it is possible that this return date is biased early. Since the strengthening of the Brewer-Dobson circulation through the 21st century leads to increases in springtime Arctic column ozone, by 2100 Arctic ozone is projected to lie well above 1960 levels. Uncertainties in Projections • Conclusions dependent on future GHG levels are less certain than those dependent on future ODS levels since ODS emissions are controlled by the Montreal Protocol. For the six GHG scenarios considered by a few CCMs, the simulated differences in stratospheric column ozone over the second half of the 21st century are largest in the northern midlatitudes and the Arctic, with maximum differences of 20–40 DU between the six scenarios in 2100. • There remain sources of uncertainty in the CCM simulations. These include the use of prescribed ODS mixing ratios instead of emission fluxes as lower boundary conditions, the range of sea surface temperatures and sea ice concentrations, missing tropospheric chemistry, model parameterizations, and model climate sensitivity. • Geoengineering schemes for mitigating climate change by continuous injections of sulfur-containing compounds into the stratosphere, if implemented, would substantially affect stratospheric ozone, particularly in polar regions. Ozone losses observed following large volcanic eruptions support this prediction. However, sporadic volcanic eruptions provide limited analogs to the effects of continuous sulfur emissions. Preliminary model simulations reveal large uncertainties in assessing the effects of continuous sulfur injections. Expected Future Changes in Surface UV. While a number of factors, in addition to ozone, affect surface UV irradiance, the focus in this chapter is on the effects of changes in stratospheric ozone on surface UV. For this reason, clear-sky surface UV irradiance is calculated from ozone projections from CCMs. • Projected increases in midlatitude ozone abundances during the 21st century, in the absence of changes in other factors, in particular clouds, tropospheric aerosols, and air pollutants, will result in decreases in surface UV irradiance. Clear-sky erythemal irradiance is projected to return to 1980 levels on average in 2025 for the northern midlatitudes, and in 2035 for the southern midlatitudes, and to fall well below 1980 values by the second half of the century. However, actual changes in surface UV will be affected by a number of factors other than ozone. • In the absence of changes in other factors, changes in tropical surface UV will be small because changes in tropical total column ozone are projected to be small. By the middle of the 21st century, the model projections suggest surface UV to be slightly higher than in the 1960s, very close to values in 1980, and slightly lower than in 2000. The projected decrease in tropical total column ozone through the latter half of the century will likely result in clear-sky surface UV remaining above 1960 levels. Average UV irradiance is already high in the tropics due to naturally occurring low total ozone columns and high solar elevations. • The magnitude of UV changes in the polar regions is larger than elsewhere because ozone changes in polar regions are larger. For the next decades, surface clear-sky UV irradiance, particularly in the Antarctic, will continue to be higher than in 1980. Future increases in ozone and decreases in clear-sky UV will occur at slower rates than those associated with the ozone decreases and UV increases that occurred before 2000. In Antarctica, surface clear-sky UV is projected to return to 1980 levels between 2040 and 2060, while in the Arctic this is projected to occur between 2020 and 2030. By 2100, October surface clear-sky erythemal irradiance in Antarctica is likely to be between 5% below to 25% above 1960 levels, with considerable uncertainty. This is consistent with multi-model-mean October Antarctic total column ozone not returning to 1960 levels by 2100. In contrast, by 2100, surface clear-sky UV in the Arctic is projected to be 0–10% below 1960 levels.