Descriptions of 104 gravity and piston sediment cores from POLARSTERN expedition ARK-VIII/3 to the Arctic Ocean

Sediment descriptions and lithostratigraphy (chapter 6.4) NANSEN BASIN The upperrnost 20-50 cm of sedirnents in the Nansen Basin norrnally cornprise soft dark brown, brown-grayish and brown clay. Except for the toprnost clay, the four piston cores retrieved, contained quite different lithologies: a rnuddy diarnicton with outsized clasts (PS2157-6), sandy-silt beds alternating with clay beds (PS2159-6), and silty clay beds of brownish and grayish colours (PS2161-3). Core PS2208-3 was retrieved frorn a plateau on a searnount. The plateau was serni-encircled by hills. The upper 250 cm of this core cornprise brown and olive brown clays. Below these are several sandlayers and a 74 cm thick unit of a sandy mud with rnud-clasts up to 20 cm in diameter. GAKKEL RIDGE The uppermost 20-50 cm of sediments on the Gakkel Ridge comprise soft dark brown, brown, grayish brown clay. In most of the cores there are two horizons of brown clay separated by olive brown clay. The upper horizon is darker. The older stratigraphy is rather varied. Core PS2165-1 contains several thin gray sandlsilt layers, probably distal turbidites. The sarne is found in Core PS2167-1. This core also has a thick (approx. 2 rn) coarse grained turbidite containing large rnud clasts and basaltic rock fragrnents. The color of the turbiditic layers is dark gray. There are several horizons of hernipelagic sandylsilty clays with quite a variety in colours; black, gray, olive, brown, yellowish brown and reddish. The colour variation rnay be due to hydrotherrnal activity or provenance or a shift in redox potential. Cores PS2168-2 and PS2169-1 have typical sequences of very dark gray sandy mud with sharp lower boundaries grading upwards into olive brown clay. Below the lower boundary is often a thin (1-2 cm) gray clay layer. AMUNDSEN BASIN The giant box cores (GKG) provided in most cases excellently preserved sedirnent surfaces which consisted in the entire Amundsen Basin of dark brown to dark grayish brown silty clay with few dropstones and common calcareous microfossils (foraminifers and calcareous nannofossils). The brown and grayish brown color of the sediment surface is a result of the oxidizing conditions at the seafloor due to the rapid renewal of the bottom water rnasses. Planktic forarninifers and calcareous nannofossils are relatively frequent and well preserved despite the rernote location of the basin and its water depths of >4000 rn. Srnear slide descriptions have shown that the surface sedirnents consist dorninantly of clays to silty rnuds with clay rninerals and quartz as the rnost important constituents. The coarse fractions contained besides planktic and benthic forarninifers and coarse clastic rnaterials, rare bivalves, dropstones and mud clasts. The Station PS2190 at the North Pole is a particular good exarnple of the type of sedirnents deposited at the sea floor surface of the Arnundsen Basin, with hornogenous dark brown soft clay covering a sedirnent sequence of highly variable cornposition. Nurnerous giant box cores also provide insight into the detailed lithostratigraphy of the upperrnost sedirnent layers. Twelve box cores have been collected frorn the Arnundsen Basin. Below the youngest unit of 5-20 crn thick silty clays deposits of variable stratigraphies have been found, rnostly consisting of clays or silty clays. In a few instances turbidites have been observed. Benthic forarninifers have not been found in the surface sedirnents. Other fossils were extrernely rare. Bioturbation is weakly developed on all stations. Benthic anirnals seern to live only in and on the upperrnost 2 cm of the uppermost sediment layer. They cornprise amphipods (on all stations) and holothurians, bryozoans, polychaetes, and porifers at one station each. LOMONOSOV RIDGE Sediments from the Lomonosov Ridge show a variety of colors and textures. Following smear slide analyses they are composed mostly of clay minerals and quartz with mica and feldspars, especially in the siltier and sandier parts. Volcanic glass, microcrystalline carbonate, opaque minerals and green amphibole are occasional accessories. The sediments from the Lomonosov Ridge show a noticeable difference from sediments collected from the surrounding basins. Lomonosov Ridge sediments are richer in silt and sand than basin sediments. Occasional turbidites occur in ridge sediments but these must be of entirely local origin. The ridge sediments include frequent layers of "cottage cheese" texture made up of what appear to be small, angular mud clasts of a variety of colors.

Biomarker distributions in sediment core PS2767-4

Here, we present a first (low-resolution) biomarker sea-ice proxy record from the High Arctic (southern Lomonosov Ridge), going back in time to about 60 ka (MIS 3 to MIS 1). Variable concentrations of the sea-ice diatom specific highly branched isoprenoid (HBI) with 25 carbon atoms ("IP25"), in combination with the phytoplankton biomarker brassicasterol, suggest variable seasonal sea-ice coverage and open-water productivity during MIS 3. During most of MIS 2, the spring to summer sea-ice margin significantly extended towards the south, resulting in a drastic decrease in phytoplankton productivity. During the Early Holocene Climate Optimum, brassicasterol reached its maximum, interpreted as signal for elevated phytoplankton productivity due to a significantly reduced sea-ice cover. During the mid-late Holocene, IP25 increased and brassicasterol decreased, indicating extended sea-ice cover and reduced phytoplankton productivity, respectively. The HBI diene/IP25 ratios probably reached maximum values during the Bølling-Allerød warm period and decreased during the Holocene, suggesting a correlation with sea-surface temperature.

(Table 3) Geochemistry of borehole fluids of ODP Hole 137-504B

Circulation of seawater through basaltic basement for several million years after crustal emplacement has been inferred from studies of surface heat flow, and may play a significant role in the exchange of elements between the oceanic crust and seawater. Without direct observation of the fluid chemistry, interpretations regarding the extent and timing of this exchange must be based on the integrated signal of alteration found in sampled basalts. Much interest has thus been expressed in obtaining and analyzing fluids directly from basaltic formations. It has been proposed that open oceanic boreholes can be used as oceanic groundwater wells to obtain fluids that are circulating within the formation. Water samples were collected from the open borehole in Hole 504B prior to drilling operations on Leg 137, with the original intention of collecting formation fluids from the surrounding basaltic rocks. Past results have yielded ambiguous conclusions as to the origin of the fluids recovered-specifically, whether or not the fluids were true formation fluids or merely the result of reaction of seawater in the borehole environment. The chemistry of eight borehole fluid samples collected during Leg 137 is discussed in this paper. Large changes in major, minor, and isotopic compositions relative to unaltered seawater were observed in the borehole fluids. Compositional changes increased with depth in the borehole. The samples exhibit the effect of simple mixing of seawater, throughout the borehole, with a single reacted fluid component. Analysis and interpretation of the results from Leg 137 in light of past results suggest that the chemical signals observed may originate predominantly from reaction with basaltic rubble residing at the bottom of the hole during the interim between drilling legs. Although this endeavor apparently did not recover formation waters, information on the nature of reaction between seawater and basalt at the prevalent temperatures in Hole 504B (>160°C) has been gained that can be related to reconstruction of the alteration history of the oceanic crust. Isotopic analyses allow calculation of element-specific water/rock mass ratios (Li and Sr) and are related to the extent of chemical exchange between the borehole fluids and basalt.

(Table 3) Oxygen and carbon isotopic record of living (Rose Bengal Stained) benthic foraminifera of North Atlantic surface sediments

Variation of the d13C of living (Rose Bengal stained) deep-sea benthic foraminifera is documented from two deep-water sites (~2430 and ~3010 m) from a northwest Atlantic Ocean study area 275 km south of Nantucket Island. The carbon isotopic data of Hoeglundina elegans and Uvigerina peregrina from five sets of Multicorer and Soutar Box Core samples taken over a 10-month interval (March, May, July, and October 1996 and January 1997) are compared with an 11.5 month time series of organic carbon flux to assess the effect of organic carbon flux on the carbon isotopic composition of dominant taxa. Carbon isotopic data of Hoeglundina elegans at 3010 m show 0.3 per mil lower mean values following an organic carbon flux maximum resulting from a spring phytoplankton bloom. This d13C change following the spring bloom is suggested to be due to the presence of a phytodetritus layer on the seafloor and the subsequent depletion of d13C in the pore waters within the phytodetritus and overlying the sediment surface. Carbon isotopic data of H. elegans from the 2430 m site show an opposite pattern to that found at 3010 m with a d13C enrichment following the spring bloom. This different pattern may be due to spatial variation in phytodetritus deposition and resuspension or to a limited number of specimens recovered from the March 1996 cruise. The d13C of Uvigerina peregrina at 2430 m shows variation over the 10 month interval, but an analysis of variance shows that the variability is more consistent with core and subcore variability than with seasonal changes. The isotopic analyses are grouped into 100 µm size classes on the basis of length measurements of individual specimens to evaluate d13C ontogenetic changes of each species. The data show no consistent patterns between size classes in the d13C of either H. elegans or U. peregrina. These results suggest that variation in organic carbon flux does not preferentially affect particular size classes, nor do d13C ontogenetic changes exist within the >250 to >750 µm size range for these species at this locality. On the basis of the lack of ontogenetic changes a range of sizes of specimens from a sample can be used to reconstruct d13C in paleoceanographic studies. The prediction standard deviation, which is composed of cruise, core, subcore, and residual (replicate) variability, provides an estimate of the magnitude of variability in fossil d13C data; it is 0.27 per mil for H. elegans at 3010 m and 0.4 per mil for U. peregrina at the 2430 m site. Since these standard deviations are based on living specimens, they should be regarded as minimum estimates of variability for fossil data based on single specimen analyses. Most paleoceanographic reconstructions are based on the analysis of multiple specimens, and as a result, the standard error would be expected to be reduced for any particular sample. The reduced standard error resulting from the analysis of multiple specimens would result in the seasonal and spatial variability observed in this study having little impact on carbon isotopic records.

(Table 3, page 309) Mercury content of concretions from Grand Lake (GL) and Ship Harbour Lake (SH), Nova Scotia and Mosque Lake (ML), Ontario

Ferromanganese concretions from Grand Lake and Ship Harbour Lake in Nova Scotia and Mosque Lake in Ontario are most common in water 0.5 to 2 m deep. X-ray diffraction studies show the ferromanganese portions of the concretions to he amorphous. Petrographic and electron probe studies of the ferromanganese material reveal chemical banding of iron and manganese. Bulk chemical analyses indicate that the Fe:Mn ratios of concretions from different sites within a single lake are similar, whereas concretions from different lakes have characteristic Fe:Mn ratios. Trace element concs are different in different lakes and are generally several orders of magnitude less than those of oceanic nodules.

Physical oceanography from CTD during Maria S. Merian cruise MSM20/4 in spring 2012

With an extension of > 40 km**2 the recently discovered Campeche cold-water coral province located at the northeastern rim of the Campeche Bank in the southern Gulf of Mexico belongs to the largest coherent cold-water coral areas discovered so far. The Campeche province consists of numerous 20-40 m-high elongated coral mounds that are developed in intermediate water depths of 500 to 600 m. The mounds are colonized by a vivid cold-water coral ecosystem that covers the upper flanks and summits. The rich coral community is dominated by the framework-building Scleractinia Enallopsammia profunda and Lophelia pertusa, while the associated benthic megafauna shows a rather scarce occurrence. The recent environmental setting is characterized by a high surface water production caused by a local upwelling center and a dynamic bottom-water regime comprising vigorous bottom currents, obvious temporal variability, and strong density contrasts, which all together provide optimal conditions for the growth of cold-water corals. This setting - potentially supported by the diel vertical migration of zooplankton in the Campeche area - controls the delivering of food particles to the corals. The Campeche cold-water coral province is, thus, an excellent example highlighting the importance of the oceanographic setting in securing the food supply for the development of large and vivid cold-water coral ecosystems.

Granulometry, mineralogy and organic matter content of permafrost core 5011-3

The combination of permafrost history and dynamics, lake level changes and the tectonical framework is considered to play a crucial role for sediment delivery to El'gygytgyn Crater Lake, NE Russian Arctic. The purpose of this study is to propose a depositional framework based on analyses of the core strata from the lake margin and historical reconstructions from various studies at the site. A sedimentological program has been conducted using frozen core samples from the 141.5 m long El'gygytgyn 5011-3 permafrost well. The drill site is located in sedimentary permafrost west of the lake that partly fills the El'gygytgyn Crater. The total core sequence is interpreted as strata building up a progradational alluvial fan delta. Four macroscopically distinct sedimentary units are identified. Unit 1 (141.5-117.0 m) is comprised of ice-cemented, matrix-supported sandy gravel and intercalated sandy layers. Sandy layers represent sediments which rained out as particles in the deeper part of the water column under highly energetic conditions. Unit 2 (117.0-24.25 m) is dominated by ice-cemented, matrix-supported sandy gravel with individual gravel layers. Most of the Unit 2 diamicton is understood to result from alluvial wash and subsequent gravitational sliding of coarse-grained (sandy gravel) material on the basin slope. Unit 3 (24.25-8.5 m) has ice-cemented, matrix-supported sandy gravel that is interrupted by sand beds. These sandy beds are associated with flooding events and represent near-shore sandy shoals. Unit 4 (8.5-0.0 m) is ice-cemented, matrix-supported sandy gravel with varying ice content, mostly higher than below. It consists of slope material and creek fill deposits. The uppermost metre is the active layer (i.e. the top layer of soil with seasonal freeze and thaw) into which modern soil organic matter has been incorporated. The nature of the progradational sediment transport taking place from the western and northern crater margins may be related to the complementary occurrence of frequent turbiditic layers in the central lake basin, as is known from the lake sediment record. Slope processes such as gravitational sliding and sheet flooding occur especially during spring melt and promote mass wasting into the basin. Tectonics are inferred to have initiated the fan accumulation in the first place and possibly the off-centre displacement of the crater lake.

Description of manganese nodules and crust collected from the Hakuho Maru Cruise KH-68-3, July-August, 1968, in Northwestern Pacific Ocean

The cores and dredges described in this report were taken on the KH-68-3 Expedition in July-August, 1968 by the Ocean Research Institute, University of Tokyo from the Hakuho Maru. A total of 16 cores and dredges sites have been were.

Sea-surface reconstructions of the western Pacific Ocean during the last 5.3 million years

The late Neogene was a time of cryosphere development in the northern hemisphere. The present study was carried out to estimate the sea surface temperature (SST) change during this period based on the quantitative planktonic foraminiferal data of 8 DSDP sites in the western Pacific. Target factor analysis has been applied to the conventional transfer function approach to overcome the no-analog conditions caused by evolutionary faunal changes. By applying this technique through a combination of time-slice and time-series studies, the SST history of the last 5.3 Ma has been reconstructed for the low latitude western Pacific. Although the present data set is close to the statistical limits of factor analysis, the clear presence of sensible variations in individual SST time-series suggests the feasibility and reliability of this method in paleoceanographic studies. The estimated SST curves display the general trend of the temperature fluctuations and reveal three major cool periods in the late Neogene, i.e. the early Pliocene (4.7 3.5 Ma), the late Pliocene (3.1-2.7 Ma), and the latest Pliocene to early Pleistocene (2.2-1.0 Ma). Cool events are reflected in the increase of seasonality and meridional SST gradient in the subtropical area. The latest Pliocene to early Pleistocene cooling is most important in the late Neogene climatic evolution. It differs from the previous cool events in its irreversible, steplike change in SST, which established the glacial climate characteristic of the late Pleistocene. The winter and summer SST decreased by 3.3-5.4°C and 1.0 2.1C in the subtropics, by 0.9°C and 0.6C in the equatorial region, and showed little or no cooling in the tropics. Moreover, this cooling event occurred as a gradual SST decrease during 2.2 1.0 Ma at the warmer subtropical sites, while that at cooler subtropical site was an abrupt SST drop at 2.2 Ma. In contrast, equatorial and tropical western Pacific experienced only minor SST change in the entire late Neogene. In general, subtropics was much more sensitive to climatic forcing than tropics and the cooling events were most extensive in the cooler subtropics. The early Pliocene cool periods can be correlated to the Antarctic ice volume fluctuation, and the latest Pliocene early Pleistocene cooling reflects the climatic evolution during the cryosphere development of the northern hemisphere.

Neue und selektive GSTP1-Inhibitoren mit 1,2,4-Trioxanstruktur als Grundlage für die Entwicklung einer effektiven Tumortherapie

Im Rahmen dieser Arbeit wurden selektive Inhibitoren der Glutathion-Transferase P1 (GSTP1) mit 1,2,4-Trioxanstruktur als potentielle Wirkstoffe gegen multiresistente Tumore synthetisiert. Die Darstellung dieser Substanzen erfolgte über Typ-II-Photooxygenierung allylischer Alkohole mit anschließender Säure-katalysierter Peroxyacetalisierung unter Verwendung von 4-Nitrobenzaldehyd. Über diesen Syntheseweg konnten unterschiedlich substituierte 1,2,4-Trioxane dargestellt werden. Die höchste biologische Aktivität zeigten Verbindungen mit aromatischen Estersubstituenten am 1,2,4-Trioxanring. Es wurde eine Leitstruktur entwickelt, die einen α,β-ungesättigten aromatischen Estersubstituenten in Position 6 des 1,2,4-Trioxangerüsts und in Position 3 einen 4-Nitrophenylsubstituenten aufweist. Die Verbindungen dieser Substanzklasse zeigen Inhibition der GSTP1 im niedrig mikromolaren Bereich. Durch Aktivitätsstudien an den GST-Klassen A und M konnte gezeigt werden, dass die Verbindungen selektiv GSTP1 inhibieren. Nachdem mittels quantitativer PCR 12 Krebszelllinien, die hohe GSTP1-Expressionsniveaus zeigen, identifiziert worden waren, wurde die Aktivität der 1,2,4-Trioxane gegenüber GST, die in Krebszelllysaten vorkommt, nachgewiesen. Die GST in der Brustkrebsepithelzelllinie HBL100 und der Lungenkarzinomzelllinie SK-MES-1 wird durch 1,2,4-Trioxane noch effektiver inhibiert als aufgereinigte GSTP1 (IC50 im nanomolaren Bereich).

Matriz Input-Output da região Alentejo: Acerca da Distribuição de Rendimento (3º quadrante)

No número 18 do “Boletim Trimestral” apresentámos os principais resultados do estudo que elaborou a Matriz Input-Output da Região Alentejo (MIO-Alentejo). Com este texto prosseguimos o propósito de divulgação dos resultados e conclusões do projeto, mas adotando agora uma perspectiva mais focalizada. Em particular, interessa-nos de momento olhar para o processo de formação do valor acrescentado, ou, de forma equivalente, para a distribuição do rendimento gerado na produção, sob a forma de remuneração dos diferentes fatores produtivos (3º quadrante). Nos pontos 2, 3, e 4 apresentamos os resultados e, em conclusão, deixamos algumas considerações finais no ponto 5. Anexamos um glossário com uma breve descrição metodológica.

Sintese de derivados 3 - substituídos de coumarinas

Este trabalho descreve a síntese de novos derivados de coumarinas 3-substituídas por grupos arilo, etenilarilo e etenil-organometálicos, através de novas metodologias via reacções de Heck e de metátese (Grubbs), com controlo da regioquímica e com significativos rendimentos reaccionais. A aplicação destas metodologias permitiu a síntese dos derivados, 3-fenilcoumarina (131), 3-(4-bromofenil)coumarina, (132), 3-(4-iodofenil)­coumarina (134), 3-(4-nitrofenil)coumarina (136), 3-(4-etilfenil)coumarina (133), 4-(coumarin-3-il)benzaldeído (135), 3-(4-metoxifenil)coumarina (137), (E)-3-acrilato-[4-(coumarin-3-il)fenil] de metilo (138), 6,7-metileno­dioxi-[3-(E)-2'-feniletenil]coumarina (145), 6,7-dimetoxi-[-(E)-2'-fenil­etenil]coumarina (146), 6,7-dimetoxi-[3-(E)-2'-(6'-nitrofenil)etenil]coumarina (147), 4-[2-(E)-(6,7-dimetoxicoumarin-3-il)etenil]benzaldeído (148) e 6,7-dimetoxi-[3-(E)-2'-ferroceniletenil]coumarina (149), dos quais os últimos nove, são compostos novos, identificados e caracterizados pela primeira vez. A deslocalização do sistema de electrões  conjugados, induzida pelos diversos substituintes das coumarinas, foi igualmente avaliada através da espectroscopia de UV/Vis. De referir que parte deste trabalho foi publicado como: "New Methodology for the Synthesis of 3-Substituted Coumarins via Pd-Catalyzed Site-Se/ective Cross-Coupling Reactions”, Sérgio Martins, Paula S. Branco, María C. de la Torre, Miguel A. Sierra e António Pereira, Synlett, 2010 (https://www.thieme-connect.com/ejournals/abstract/ synlett/doi/1 O.1 OS5/s-0030-1259014). ABSTRACT: This work describes the synthesis of new 3-aryl, ethenylaryl and ethenyl-organometallics coumarin derivatives, using a new methodology via Heck and metathesis (Grubbs) reactions, with regiochemistry control and significant reaction yields. The application of these methodologies allowed the synthesis of derivatives, 3-phenylcoumarin (131), 3-(4-bromophenyl)coumarin (132), 3-(4-iodophenyl)coumarin (134), 3-(4-nitrophenyl)coumarin (136), 3-(4-ethylphenyl)coumarin {133), 4-(coumarin-3-yl)benzaldehyde {135), 3-(4-methoxiphenyl)coumarin (137), (E)-ethyl 3-[4(coumarin-3-yl)phenyl]­acrylate (138), 6,7-methylenedioxy-[3-(E)-2'-phenylethenyl]coumarin (145), 6,7-dimethoxy-[-(E)-2'-phenylethenyl]coumarin (146), 6,7-dimethoxy-[3-(E)­-2'-(6'-nitrophenyl)ethenyl]coumarin (147), 4-[2-(E)-(6,7-dimethoxy­coumarin-3-yl)ethenyl]benzaldehyde {148) e 6,7-dimethoxy-[3-(E)-2'-(ferro­ cene)ethenyl]coumarin (149), the last nine of these are new compounds, identified and characterized for the first time. The delocalization of conjugated -electron system, induced by different substituents of coumarins, was also assessed by spectroscopy UV/Vis. Part of this work was published at: "New Methodology for the Synthesis of 3-Substituted Coumarins via Pd-Catalyzed Site-Selective Cross-Coupling Reactions", Sérgio Martins, Paula S. Branco, María C. de la Torre, Miguel A. Sierra e António Pereira, Synlett, 2010 (https://www.thieme­connect.com/ejournaIs/abstract/synlett/doi/1O.1 055/s-0030-1259014).