Eletrodo modificado com filme de poli aminoácido para determinação de hidrazina em água de caldeira

Fundação de Amparo à Pesquisa do Estado de São Paulo (FAPESP)

Um súdito capaz no Vale Amazônico (ou Landi, esse conhecido): um outro significado da descrição das plantas e animais do Grão-Pará

Elaborada em meio às intervenções da administração portuguesa no Vale Amazônico, a Descrição de várias Plantas, Frutas, Animais, Aves, Peixes, Cobras, raízes, e outras coisas semelhantes que se acham nesta Capitania do Grão Pará, de Antonio Landi, escrita entre os anos de 1772 e 1773, tem sido vista pela historiografia como resultante dos interesses da Coroa portuguesa. Este trabalho tem por objeto de estudo tal descrição, propondo uma compreensão distinta da comumente aceita, de que a Descrição das plantas e dos animais da capitania do Grão Pará surgiu como um desdobramento lógico das políticas metropolitanas. Sendo assim, não se trata de uma formulação sugerida ou determinada pela burocracia colonial, mas de um trabalho motivado a partir das demandas coloniais. Por outro lado, esta dissertação buscou compreender as intenções próprias da condição de colono do arquiteto italiano, evitando conceber sua produção como naturalista apenas como um reflexo do pensamento científico europeu. Antes, buscando entender essa atividade como relacionada ao contexto da dinâmica colonial local. Dessa forma, este estudo procura evidenciar que as práticas e contornos próprios da sociedade do Vale Amazônico foram determinantes para a elaboração do trabalho de História Natural de Antonio Landi.

"Daring to be foolish". L'opera poetica di Robert Kroetsch dal 2001 al 2010

La presente dissertazione si pone come oggetto di analisi la produzione poetica di Robert Kroetsch (1927-2011), scrittore e critico letterario canadese nativo dell’Alberta (Canada), che tra il 1960 e il 2010 ha pubblicato un numero notevole di opere (nove romanzi, più di venti opere poetiche tra componimenti singoli e in raccolta, due volumi di saggi e diverse interviste). In particolare si è scelto di focalizzare l’attenzione sulle ultime tre raccolte di poesia – rispettivamente The Hornbooks of Rita K (2001), The Snowbird Poems (2004) e Too Bad: Sketches Toward a Self-Portrait (2010) – che, se confrontate con la produzione precedente, forniscono prova di alcuni elementi di novità all’interno della prospettiva poetica di Kroetsch. L’ipotesi dalla quale trae origine il presente studio è infatti che, a partire dalla raccolta The Hornbooks of Rita K, Kroetsch abbia imboccato un percorso di evoluzione stilistica che corre in parallelo con la formulazione di una nuova poetica. Nello specifico, si osserva che, negli ultimi dieci anni, da un punto di vista formale i componimenti si frammentano progressivamente, passando da una forma lunga – quella del long poem – a una breve – lo sketch, che risulta più adatta a rappresentare sul piano espressivo una mutata percezione dell’Io poetico. A un simile aspetto si aggiunge poi il fatto che la raffigurazione della propria vicenda umana diventa, con sempre maggiore evidenza, motivo di riflessione su una condizione universale dell’umano e sulla dimensione etica del suo agire.

Abflusslose Senken – Instrumente in der Landschaftsanalyse und Indikatoren rezenter Krustenbewegungen

Innerhalb des Untersuchungsgebiets Schleswig-Holstein wurden 39.712 topographische Hohlformen detektiert. Genutzt wurden dazu ESRI ArcMap 9.3 und 10.0. Der Datenaufbereitung folgten weitere Kalkulationen in MATLAB R2010b. Jedes Objekt wurde räumlich mit seinen individuellen Eigenschaften verschnitten. Dazu gehörten Fläche, Umfang, Koordinaten (Zentroide), Tiefe und maximale Tiefe der Hohlform und Formfaktoren wie Rundheit, Konvexität und Elongation. Ziel der vorgestellten Methoden war die Beantwortung von drei Fragestellungen: Sind negative Landformen dazu geeignet Landschaftseinheiten und Eisvorstöße zu unterscheiden und zu bestimmen? Existiert eine Kopplung von Depressionen an der rezenten Topographie zu geologischen Tiefenstrukturen? Können Senken unterschiedlicher Entstehung anhand ihrer Formcharakteristik unterteilt werden? Die vorgenommene Klassifikation der großen Landschaftseinheiten basiert auf der Annahme, dass sowohl Jungmoränengebiete, ihre Vorflächen als auch Altmoränengebiete durch charakteristische, abflusslose Hohlformen, wie Toteislöcher, Seen, etc. abgegrenzt werden können. Normalerweise sind solche Depressionen in der Natur eher selten, werden jedoch für ehemalige Glaziallandschaften als typisch erachtet. Ziel war es, die geologischen Haupteinheiten, Eisvorstöße und Moränengebiete der letzten Vereisungen zu differenzieren. Zur Bearbeitung wurde ein Detektionsnetz verwendet, das auf quadratischen Zellen beruht. Die Ergebnisse zeigen, dass durch die alleinige Nutzung von Depressionen zur Klassifizierung von Landschaftseinheiten Gesamtgenauigkeiten von bis zu 71,4% erreicht werden können. Das bedeutet, dass drei von vier Detektionszellen korrekt zugeordnet werden können. Jungmoränen, Altmoränen, periglazialeVorflächen und holozäne Bereiche können mit Hilfe der Hohlformen mit großer Sicherheit voneinander unterschieden und korrekt zugeordnet werden. Dies zeigt, dass für die jeweiligen Einheiten tatsächlich bestimmte Senkenformen typisch sind. Die im ersten Schritt detektierten Senken wurden räumlich mit weiterreichenden geologischen Informationen verschnitten, um zu untersuchen, inwieweit natürliche Depressionen nur glazial entstanden sind oder ob ihre Ausprägung auch mit tiefengeologischen Strukturen in Zusammenhang steht. 25.349 (63,88%) aller Senken sind kleiner als 10.000 m² und liegen in Jungmoränengebieten und können vermutlich auf glaziale und periglaziale Einflüsse zurückgeführt werden. 2.424 Depressionen liegen innerhalb der Gebiete subglazialer Rinnen. 1.529 detektierte Hohlformen liegen innerhalb von Subsidenzgebieten, von denen 1.033 innerhalb der Marschländer im Westen verortet sind. 919 große Strukturen über 1 km Größe entlang der Nordsee sind unter anderem besonders gut mit Kompaktionsbereichen elsterzeitlicher Rinnen zu homologisieren.344 dieser Hohlformen sind zudem mit Tunneltälern im Untergrund assoziiert. Diese Parallelität von Depressionen und den teils über 100 m tiefen Tunneltälern kann auf Sedimentkompaktion zurückgeführt werden. Ein Zusammenhang mit der Zersetzung postglazialen, organischen Materials ist ebenfalls denkbar. Darüber hinaus wurden in einer Distanz von 10 km um die miozän aktiven Flanken des Glückstadt-Grabens negative Landformen detektiert, die Verbindungen zu oberflächennahen Störungsstrukturen zeigen. Dies ist ein Anzeichen für Grabenaktivität während und gegen Ende der Vereisung und während des Holozäns. Viele dieser störungsbezogenen Senken sind auch mit Tunneltälern assoziiert. Entsprechend werden drei zusammenspielende Prozesse identifiziert, die mit der Entstehung der Hohlformen in Verbindung gebracht werden können. Eine mögliche Interpretation ist, dass die östliche Flanke des Glückstadt-Grabens auf die Auflast des elsterzeitlichen Eisschilds reagierte, während sich subglazial zeitgleich Entwässerungsrinnen entlang der Schwächezonen ausbildeten. Diese wurden in den Warmzeiten größtenteils durch Torf und unverfestigte Sedimente verfüllt. Die Gletschervorstöße der späten Weichselzeit aktivierten erneut die Flanken und zusätzlich wurde das Lockermaterial exariert, wodurch große Seen, wie z. B. der Große Plöner See entstanden sind. Insgesamt konnten 29 große Depressionen größer oder gleich 5 km in Schleswig-Holstein identifiziert werden, die zumindest teilweise mit Beckensubsidenz und Aktivität der Grabenflanken verbunden sind, bzw. sogar auf diese zurückgehen.Die letzte Teilstudie befasste sich mit der Differenzierung von Senken nach deren potentieller Genese sowie der Unterscheidung natürlicher von künstlichen Hohlformen. Dazu wurde ein DEM für einen Bereich im Norden Niedersachsens verwendet, das eine Gesamtgröße von 252 km² abdeckt. Die Ergebnisse zeigen, dass glazial entstandene Depressionen gute Rundheitswerte aufweisen und auch Elongation und Exzentrizität eher kompakte Formen anzeigen. Lineare negative Strukturen sind oft Flüsse oder Altarme. Sie können als holozäne Strukturen identifiziert werden. Im Gegensatz zu den potentiell natürlichen Senkenformen sind künstlich geschaffene Depressionen eher eckig oder ungleichmäßig und tendieren meist nicht zu kompakten Formen. Drei Hauptklassen topographischer Depressionen konnten identifiziert und voneinander abgegrenzt werden: Potentiell glaziale Senken (Toteisformen), Flüsse, Seiten- und Altarme sowie künstliche Senken. Die Methode der Senkenklassifikation nach Formparametern ist ein sinnvolles Instrument, um verschiedene Typen unterscheiden zu können und um bei geologischen Fragestellungen künstliche Senken bereits vor der Verarbeitung auszuschließen. Jedoch zeigte sich, dass die Ergebnisse im Wesentlichen von der Auflösung des entsprechenden Höhenmodells abhängen.

The construal of constructions: causal and temporal interpretations in change constructions

In this paper I first discuss some non-causal change constructions which have largely gone unnoticed in the literature, such as The butler bowed the guests in (which is said to code mild causation) and The supporters booed Newcastle off at the interval (which only codes temporal coextension between its two constitutive subevents). Since the same structure (i.e. the transitive object-oriented change construction) can be used to code a wide spectrum of causal and temporal relations, the question arises of what cognitive mechanisms may be involved in such meaning shifts. I argue that variation can be motivated on the basis of the figure/ground segregation which the conceptualiser can impose upon the integrated scene coded by the change construction. The integrated scene depicts a force-dynamic scenario but also evokes a unique temporal setting (i.e. temporal overlap or coextension between the constitutive subevents). Such a “bias” towards temporal overlap can be used by the conceptualiser to background causation and highlight temporal overlap interpretations. It is also shown that figure/ground segregation can be appealed to to account for the causal interpretation of intransitive change constructions, e.g. The kettle boiled dry. If the conceptual distance between the verbal event and the non-verbal event is (relatively) great, causality can be highlighted even in intransitive patterns.

Law in a Linguistic Battlefield: The Language of the New State Versus the ‘Language of the Oppressors’ in Ukraine

Article 10 of the 1996 Ukrainian Constitution proclaims that “The state language of Ukraine shall be the Ukrainian language” but continues: “Free development, use, and protection of Russian and other languages of national minorities of Ukraine shall be guaranteed in Ukraine.” Consolidating the position of the state language was at the centre of the "Orange Revolution", but President Yanukovich, elected in February 2010, has committed himself to a defence of the Russian language, as a regional language of Ukraine, and the battle is on to replace the Law on Languages of the Ukrainian SSR of 1989, which is still in force. Ukraine has ratified the Council of Europe’s European Charter for Regional or Minority Languages. This article reflects on the relation between language and law, and endeavours to bring clarity to a situation which at times resembles an overheated kettle about to explode.

Pollen records from Elbe-Weser Dreieck

A long-running interdisciplinary research project on the development of landscape, prehistoric habitation and the history of vegetation within a "siedlungskammer" (limited habitation areal from neolithic to modern times has been carried out in the NW German lowlands, The siedlungskammer Flögeln is situated between the rivers Weser and EIbe and comprises about 23.5 km^2. It is an isolated pleistocene area surrounded by bogs, the soils consisting mainly of poor sands. In this siedlungskammer large-seale archaeological excavations and mappings have been performed, parallel to pedological, historical and above all pollen analytical investigations. The aim of the project is to record the individual phases in time, to delimit the respective settlement areas and to reconstruct the conditions of life and economy for each time period. A dense network of 10 pollen diagrams has been constructed. Several of them derive from the marginal area and from the centre of the large raised bog north of the siedlungskammer. These diagrams reflect the history of vegetation and habitation of a large region; due to the large pollen source area the habitation phases in the diagrams are poorly defined. Even in the utmost marginal diagram of this woodless bog, a great village with adjoining fields, situated only 100 m away from it, is registered with only low values of anthropogenic indicators. In contrast to this, the numerous pollen diagrams from kettle-hole bogs inside the siedlungskammer yield an exact picture of the habitation of the siedlungskammer and their individual parts. Early traces of habitation can be identified in the pollen diagram soon after the elm decline (around 5190 BP). Some time later in the middle neolithic period there follows a marked habitation phase, which starts between 4500 and 4400 BP and reflects the immigration of the trichterbecher culture. It corresponds to the landnam phase of Iversen in Denmark and begins with a sharp decline of the pollen curves of lime and oak, followed by the increase of anthropogenic indicators pointing to arable and pastural farming. High values of wild grasses and Calluna witness extensive forest grazing. This middle to late neolithic habitation is also registered archaeologically by settlements and numerous graves. After low human activity during Bronze Age and Older Iron Age times the archaeological and pollen analytical records of Roman and Migration periods is again very strong. This is followed by a gap in habitation during the 6th and 7th centuries and afterwards in the western part of the siedlungskammer from about 700 AD until the 14th century by the activity of the medieval village of Dalem, that was also excavated and whose fields were recorded by phosphate mapping to a size of 117 hectares. This medieval settlement phase is marked by much cereal cultivation (mainly rye). The dense network of pollen diagrams offers an opportunity to register the dispersion of the anthropogenic indicators from the areas of settlement to different distances and thus to obtain quantitative clues for the assessment of these anthropogenic indicators in pollen diagrams. In fig. 4 the reflection of the neolithic culture in the kettle-hole bogs and the large raised bog is shown in 3 phases: a) pre landnam, b) TRB-landnam, c) post landnam. Among arboreal pollen the reaction of Quercus is sharp close to the settlement but is not found at more distant profiles, whilst in contrast to this Tilia shows a significant decline even far away from the settlements. The record of most anthropogenic indicators outside the habitation area is very low, in particular cereal pollen is poorly dispersed; much more certain as an indicator for habitation (also for arable farming!) is Plantago lanceolata. A strong increase of wild grasses (partly Calluna aswell) some distance from the habitation areas indicates far reaching forest grazing. Fig. 5 illustrates the reflection of the anthropogenie indicators from the medieval village Dalem. In this instance the field area could be mapped exactly using phosphate investigations, and it has been possible to indicate the precise distances of the profile sites from the medieval fields. Here also, there is a clear correlation between decreasing anthropogenic indicators and increasing distance. In a kettle-hole bog (FLH) a distance of 3000 m away this marked settlement phase is not registered. The contrast between the pollen diagrams SWK and FLH (fig. 2 + 3, enclosure), illustrates the strong differences between diagrams from kettlehole bogs close to and distant from the settlements, for the neolithic as well as for the medieval period. On the basis of the examples presented here, implications concerning the interpretation of pollen diagrams with respect to habitation phases are discussed.

Pollen records and lithology of profiles from Lobsigensee, Switzerland

Lobsigensee is a small kettle hole lake 15 km north-west of Bern on the Swiss Plateau, at an altitude of 514 m asl. Its surface is 2ha today, its maximum depth 2.7 m; it has no inlet and the overflow functions mainly during snow melting. The area was covered by Rhone ice during the Last Glaciation (map in Fig.2). Local geology, climate and vegetation are summarized in Figure 3A-C, the history of settlement in Figures 5-7. In order to reconstruct the vegetational and environmental history of the lake and its surroundings pollen analysis and other bio- and isotope stratigraphies were applied to twelve profiles cored across the basin with modified Livingstone corers (Fig.3 D). (1) The standard diagram: The central core LQ-90 is described as the standard pollen diagram (Chapter 3) with 10 local pollen assemblage zones of the Late-Glacial (local PAZ Ll to Ll0, from about 16'000(7) to 10'000 years BP) and 20 PAZ of the Holocene (local PAZ L11 to L30), see Figs. 8-10 and 20-24. Local PAZ L 1 to L3 are in the Late-Glacial clay and record the vegetational development after the ice retreat: L1 shows very low pollen concentration and high Pinus percentages due to long-distance transport and reworking; the latter mechanism is corroborated by the findings of thermophilous and pre-Quaternary taxa. Local PAZ L2 has a high di versi ty of non-arboreal pollen (NAP) and reflects the Late-Glacial steppe rich in heliophilous species. Local PAZ L3 is similar but additionally rich in Betula nana and Sal1x, thus reflecting a "shrub tundra". The PAZ L1 to L3 belong to the Oldest Dryas biozone. Local PAZ L4 to L 10 are found in the gyttja of the profundal or in the lake marl of the littoral and record the Late-Glacial forests. L4 is the shrub phase of reforestation with very high Junlperus and rapidly increasing Betula percentages. L5 is the PAZ with a first, L7 with a second dominance of tree-birches, separated by L6 showing a depression in the Betula curve. L4 to L7 can be assigned to the Balling biozone. Possible correlation of the Betula depression to the Older Dryas biozone is discussed. In local PAZ L8 Plnus immigrates and expands. L9 shows a facies difference in that Plnus dominates over Betula in littoral but not in profundal spectra. L8 and L9 belong to the Allerod biozone. In its youngest part the volcanic ash from Laach/Eifel is regularly found (11,000 BP). The local PAZ Ll0 corresponds to the Younger Dryas blozone. The merely slight increase of the NAP indicates that the pine forests of the lowland were not strongly affected by a cooler climate. In order to evaluate the significance of the littoral accumulation of coniferous pollen the littoral profile LQ-150 is compared to the profundal. Radiocarbon stratigraphies derived from different materials are presented in Figures 13 and 14 and in Tables 2 and 3. The hard-water errors in the gyttja samples and the carbonate samples are similar. The samples of terrestrial plant macrofossils are not affected by hard-water errors. Two plateaux of constant age appear in the age-depth relationship; their consequence for biostratigraphy as well as pollen concentration and influx diagrams are discussed. Radiocarbon ages of the Late-Glacial pollen zones are shown in Table 10. The Holocene vegetational history is recorded in the local PAZ L 11 to L30. After a Preboreal (PAZ L11) dominated by pine and birch the expansions of Corylus, Ulmus and Quercus are very rapid. Among these taxa Corylus dominates dur ing the Boreal (PAZ L 12 and L 1 3), whereas the components of the mixed oak forest dominate in the Older Atlantic (PAZ L14 to L16). In the Younger Atlantic (PAZ L 17 to L 19) Fagus and Alnus play an increasing, the mixed oak forest a decreasing role. During the period of local PAZ L19 Neolithic settlers lived on the shore of Lobsigensee. During the Subboreal (PAZ L20 and L21) and the Older Subatlantic (L22 to L25) strong fluctuations of Fagus and often antagonistic peaks of NAP, Alnus, Betula and Corylus can be interpreted as signs of human impact on vegetation. L23 is characterized not only by high values of NAP (especially apophytes and anthropochorous species) but also by the appearance of Juglans, Castanea and Secale which point to the Roman colonization of the area. For a certain period during the Younger Subatlantic (PAZ L26 to L30) the lake was used for retting hemp (Cannabis). Later the dominance of Quercus pollen indicates the importance of wood pastures. The youngest sediments reflect the wide-spread agricultural grass lands and the plantation of Pinus and Picea. Radiocarbon dates for the Holocene are given in Figure 23 and Table 4, the extrapolated ages of the Holocene pollen zones in Table 15. (2) The cross sections: Figures 25 and 26 give a summary of the litho- and palynostratigraphy of the two cross sections. Based on 11 Late-Glacial and 9 Holocene pollen diagrams (in addition to the standard ones), the consistency of the criteria for the definition of the pollen zones is examined in Tables 7 and 8 for the Late-Glacial and in Tables 11 to 14 for the Holocene. Sediment thicknesses across the basin for each pollen zone are presented in these tables as well as in Figures 43 to 45 for the Late-Glacial and in Figures 59 to 65 for the Holocene. Sediment focusing can explain differences between the gyttja cores of the profundal. Focusing is more than compensated for through "stretching" by carbonate precipitation on the littoral terrace. Pollen influx to the cross section are discussed (Chapters 4.1.5. and 4.2.3.). (3) The regional pollen zones: Based on some selected sites between Lake Geneva and Lake Constance regional pollen zones are proposed (Table 16, 17 and 19). (4) Paleoecology: Climatic change in the Late-Glacial can be inferred from Coleoptera, Trichoptera, Chironomidae and d18O of carbonates: a distinct warming is recorded around 12' 600 BP and around 10' 000 BP. The Younger Dryas biozone (10'700-10'000 BP) was the only cooling found in the Late-Glacial. The Betula depression often correlated wi th the Older Dryas biozone was possibl not colder but dryer than the previous period. During the Holocene the lowland site is not very sensitive to the minor climatic changes. Table 22 summarizes climatic and trophic changes before 8'000 BP as deduced from various biostratigraphies studied by a number of authors. Ostracods, Chironomids and fossil pigments indicate that anoxic conditions prevailed during the BoIling (possibly meromixis). Changes in the lake level are illustrated in Figure 74. A first lake-level lowering occurred in the early Holocene (10'000 to 9'000 BP), a second during the Atlantic (about 6'800 to 5'200 BP). The first "shrinking" of the lake volume resulted in a eutrophication recorded by laminations in the profundal and by pigments of Cyanophyceae. The second fall in water level corresponds to an increase of Nymphaeaceae. Human impact can be inferred in three ways: eutrophication of the lake (since the Neolithic), changes of terrestrial vegetation by deforestations (cyclicity of Fagus, see Figures 78 to 80), and enhanced erosion (increasing sedimentation rates by inwashed clay, particularly since the Roman Colonization, see Figures 49 and 81). Summary: This paper was planned as the final report on Lobsigensee. However, a number of issues are not answered but can only be asked more precisely, for example: (1) For the two periods with the highest rates of change, Le. the Bolling and the Preboreal biozones, pollen influx may reflect vegetation dynamics. Detailed investigations of these periods in annually laminated sediments are planned. (2) Biostratigraphies other than palynostratigraphy are needed to estimate the degree of linkage or independence in the development of terrestrial and lacustrine ecosystems. Often our sampling intervals were not identical, thus influencing our temporal resolution. (3) 6180- and 14C-stratigraPhies with high resolution will elucidate the leads and lags of these dynamic periods. Plateaux of constant age in the age-depth relationship have a strong bearing on both biological and geophysical understanding of Late-Glacial and early Holocene developments. (4) Numerical methods applied to the pollen diagrams of the cross section will help to quantify the significance of similari ties and dissimilarities across a single basin (with Prof. Birks). (5) Numerical methods applied to different sites on the Swiss Plateau and on the transect across the Alps will be helpful in evaluating the influence of different environmental factors (with Prof. Birks). (6) A new map 1: 1000 with 50cm-contour lines prov ided by Prof. Zurbuchen will be combined with a grid of cores sampling the transition from lake marl to peat enabling us to calculate paleo-volumes of the lake. This is interesting for the two "shrinking periods" (in Fig. 74A numbers 2-6 and 7-10), both accompanied by eutrophication. The pal eo-volume during the Neoli thic set tlement of the Cortaillod culture linked wi th an est l.mate of trophic change derived from diatoms (Prof. Smol in prep.) could possibly give an indication of the size of the human population of this period. (7) For the period with the antagonism between Fagus peaks and ABC-peaks close collaboration between palynologists, geochemists and archeologists should enable us to determine the influence of prehistoric and historic people on vegetation (collaboration with Prof. Stockli and Prof. Herzig). (8) The core LL-75 taken with a "cold letter box" will be analysed for major and trace elements by Dr. Sturm for 210pb and 137Cs by Prof.von Gunten and for pollen. We will see if our local PAZ L30 really corresponds to the surface sediment and if the small seepage lake reflects modern pollution.

Pollen and macrofossils profiles and age determination from the Pittsburg Basin in the lowlands of south-central Illinois

Pollen and macrofossil evidence for the nature of the vegetation during glacial and interglacial periods in the regions south of the Wisconsinan ice margin is still very scarce. Modern opinions concerning these problems are therefore predominantly derived from geological evidence only or are extrapolated from pollen studies of late Wisconsinan deposits. Now for the first time pollen and macrofossil analyses are available from south-central Illinois covering the Holocene, the entire Wisconsinan, and most probably also Sangamonian and late Illinoian time. The cores studied came from three lakes, which originated as kettle holes in glacial drift of Illinoian age near Vandalia, Fayette County. The Wisconsinan ice sheet approached the sites from the the north to within about 60 km distance only. One of the profiles (Pittsburg Basin) probably reaches back to the late Illinoian (zone 1), which was characterized by forests with much Picea. Zone 2, most likely of Sangamonian age, represents a period of species-rich deciduous forests, which must have been similar to the ones that thrive today south and southeast of the prairie peninsula. During the entire Wisconsinan (14C dates ranging from 38,000 to 21,000 BP) thermophilous deciduous trees like Quercus, Carya, and Ulmus occurred in the region, although temporarily accompanied by tree genera with a more northerly modern distribution, such as Picea, which entered and then left south-central Illinois during the Woodfordian. Thus it is evident that arctic climatic conditions did not prevail in the lowlands of south-central Illinois (about 38°30' lat) during the Wisconsinan, even at the time of the maximum glaciation, the Woodfordian. The Wisconsinan was, however, not a period of continuous forest. The pollen assemblages of zone 3 (Altonian) indicate prairie with stands of trees, and in zone 4 the relatively abundant Artemisia pollen indicates the existence of open vegetation and stands of deciduous trees, Picea, and Pinus. True tundra may have existed north of the sites, but if so its pollen rain apparently is marked by pollen from nearby stands of trees. After the disappearance of Pinus and Picea at about 14,000 BP (estimated!), there developed a mosaic of prairies and stands of Quercus, Carya, and other deciduous tree genera (zone 5). This type of vegetation persisted until it was destroyed by cultivation during the 19th and 20th century. Major vegetational changes are not indicated in the pollen diagram for the late Wisconsinan and the Holocene. The dating of zones 1 and 2 is problematical because the sediments are beyond the14C range and because of the lack of stratigraphic evidence. The zones dated as Illinoian and Sangamonian could also represent just a Wisconsinan stadial and interstadial. This possibility, however, seems to be contradicted by the late glacial and interglacial character of the forest vegetation of that time.

Letters on the Irish question /

"Letters are ... from the Freeman's Journal."--p. iv.

[Culinary ephemera : gelatin and tapioca].

Corporate contributors include: Genesee Pure Food Company; Jell-O-Co. Inc.

If the Germans conquered England, and other essays,

"Practically all the essays in this book have appeared in the New statesman ... The sketch of T. M. Kettle appeared in the Daily news, and that of the Sheehy-Skeffington in the Ploughshare. The essay, "On nationalism and nationality," was written as a preface to a report of the Nationalities and subject races conference as long ago as 1910."--Pref. note.

The day's burden

Mode of access: Internet.

Water chemistry controls on minor elemental concentrations and strontium isotopic compositions of freshwater biogenic carbonate in northeastern Washington streams

Tracking the movement of migratory freshwater fish is essential to those invested in rebuilding declining fish populations. Using strontium isotopic signatures to match calcified fish tissues to streams where fish spawn is a useful method of tracking migratory fish where physical tracking methods such as radio, acoustic, or external tags, have proven unsuccessful. In this study, we develop tools to practice this method of tracking fish in Lake Roosevelt and its upstream tributaries in Washington State by analyzing the elemental concentrations and 87Sr/86Sr ratios of water samples, and mussel shell samples. This study evaluates whether mussel shells act as an appropriate proxy for water chemistry by comparing the 87Sr/86Sr isotope ratios of water samples to the 87Sr/86Sr isotope ratios of mussel shells sampled from the same, or nearby, locations. We compare concentrations of Ba, Ca, Cd, Cu, Fe, Mg, Pb, Sr, and U in the water and mussel shell samples to determine the feasibility of using mussel shells as a proxy for water chemistry. If it is determined that the concentrations of these elements in mussel shells reflect that of the surrounding water composition, the elemental composition of mussel shells can be compared to that of calcified tissues in fish, such as otoliths, to infer the location of the natal stream. We report analyses of water and mussel shell samples collected from Lake Roosevelt, Sanpoil River, Spokane River, Colville River, Kettle River, Pend Oreille River, Kootenay River, and Columbia River in Washington State. Each of these rivers is a tributary to Lake Roosevelt, and each flows through different geologic units. We hypothesize that the differences in the rock units of each stream’s watershed are reflected in the elemental concentrations and strontium isotopic ratios of water in each stream and in the lake. We also hypothesize that the composition of the mussel shells will match the composition of the water samples, therefore allowing us to use the mussel shells as a proxy for local water chemistry. Additionally, we hypothesize that the composition of the mussel shells will vary by location, and that we will be able to then infer where a fish is from by matching the composition of the fish in question to the mussels we have analyzed. We found that 87Sr/86Sr values for water and mussel hinge samples collected from tributaries east of Lake Roosevelt are significantly higher than the 87Sr/86Sr values for samples collected from tributaries west of Lake Roosevelt with averages of 0.7235 and 0.7089, respectively. The average 87Sr/86Sr ratios for water and mussel hinge samples collected within Lake Roosevelt is 0.7158, which is between the averages for samples collected east and west of the lake. Generally, older rocks are exposed on the east side of the lake, and younger rocks on the west side of the lake, so our 87Sr/86Sr values support the hypothesis that geologic units are a primary control on water chemistry, and that tributary compositions mix to form an average weighed by flow in Lake Roosevelt. The 87Sr/86Sr values for water and mussel shell samples collected from the same locations have a strong, positive linear correlation, suggesting that mussel shell 87Sr/86Sr ratios reflect the 87Sr/86Sr ratios of the ambient water. With these data, we can distinguish between different streams and the lake, but cannot distinguish between samples from within the same stream or within Lake Roosevelt. The Sr:Ca and Fe:Ca ratios of water samples show positive correlations with mussel shell compositions, with R2 values of 0.82 and 0.52, respectively. Ratios of Mg, Ba, Cu, Cd, Pb, and U to Ca showed little or no positive correlation between water and mussel shell samples. The elemental concentration data collected for this study do not demonstrate whether a correlation between elemental ratios in water samples and elemental ratios in mussel shell samples collected from the same location exists. Positive Sr:Ca and Fe:Ca correlations for water versus mussel shell samples indicate that perhaps for some elements, the composition of mussel shells are representative of the composition of ambient water. Using elemental concentration ratios to complement 87Sr/86Sr isotopic data may enhance our ability to identify correlations between water and mussel shell samples, and ultimately between mussel shell and otolith samples. The hinge part of a mussel shell may be used as a proxy for local water composition because the mussel shell composition reflects that of the local ambient water. The hinge of the mussel has the same composition as the whole mussel shell. We measured variation of 87Sr/86Sr ratios in the water among different streams and Lake Roosevelt. The 87Sr/86Sr values for samples collected in tributaries east of Lake Roosevelt, which erode older rocks, are higher for mussel shell and water samples than the average 87Sr/86Sr values for mussel shell and water samples collected in tributaries west of Lake Roosevelt, which flow through younger rocks.