Corporeidade indígena sob o ângulo da praxeologia

Neste estudo procumaos discutir a cororeidade indígena sob vários ângulos, incluindo a visão da praxiologia motriz. Sabemos que poucos estudos têm sido feitos sobre o corpo do indígena brasileiro e que estes muitas vezes nada propõem de novo, já que não conseguem ultrapassar certos limites, impostos pela sua própria condição de herdeiro de um pensamento que se propõe ser universalista. Alguns estudos sugerem novos elementos conceituais a serem desenvolvidos nas pesquisas de campo com populações indígenas, objetivando entender como o corpo aparece representado nas configurações ideológicas veiculadas por essas populações, sua relação com a pessoa e com as forças, espíritos e almas que povoam este e os outros "mundos" acessíveis à experiência. Logo, seu estudo tem como tarefa desvendar um corpo diferente do corpo do homem moderno, herança que se vem construindo desde a Grécia Antiga. Podemos concluir que o corpo é inegavelmente o locus em torno do qual gira a vida das sociedades indígenas brasileiras conforme comprovam estudos de inúmeros antropólogos sendo por isso considerado que para compreender adequadamente a organização social e a cosmologia de uma destas sociedades, é necessário levar-se em consideração a noção de pessoa e o lugar que o corpo humano ocupa na vida das mesmas, na visão que elas fazem de si próprias. Portanto, estudar estas sociedades é procurar nelas compreendê-las.

La talasocracia minoica como controversia

Los relatos de los escritores antiguos sobre el poder del rey Minos y su dominio del mar Mediterráneo fueron considerados mitológicos hasta el descubrimiento de la llamada "civilización minoica" a principios del siglo XX. En los años siguientes, las excavaciones arqueológicas revelaron una cultura capaz de edificar palacios, desarrollar la escritura, establecer contactos con estados orientales y de someter a las islas cercanas del mar Egeo. Sin embargo, la evidencia no manifestaba que los minoicos hayan efectuado un control directo sobre los territorios que se encontraban fuera de la isla de Creta. Esta situación generó que el término "Talasocracia" fuera revisado. Diferentes disciplinas han propuesto cambios conceptuales para estudiar la relación entre los minoicos y las culturas circundantes. Nuestra intención es comparar los argumentos de quienes critican y cuestionan la existencia efectiva de la hegemonía minoica con aquellos que la defienden. Luego, propondremos nuevas líneas de investigación teniendo en cuenta el avance de los estudios actuales

Lomografando a cidade : A experiência da flânerie através da fotografia

O presente artigo tem por motivação a aproximação da flânerie à lomografia na contemporaneidade. Por isso, parte se do conceito de flâneur, a figura do caminhante e explorador que surge nas cidades modernas, termo cunhado por Charles Baudelaire (1996) e revisitado posteriormente por Walter Benjamin (1995). Contemporaneamente, Susan Sontag (2004) associa o flâneur ao fotógrafo, conceituação que se aproxima da pesquisa empírica realizada neste paper. Por meio do rolé lomográfico, evento promovido pela loja Lomography, buscou-se analisar as impressões produzidas por meio do consumo imagético do cenário urbano, da cidade do Rio de Janeiro, e tentar relacionar com o conceito de Inteligência Territorial

Corporeidade indígena sob o ângulo da praxeologia

Neste estudo procumaos discutir a cororeidade indígena sob vários ângulos, incluindo a visão da praxiologia motriz. Sabemos que poucos estudos têm sido feitos sobre o corpo do indígena brasileiro e que estes muitas vezes nada propõem de novo, já que não conseguem ultrapassar certos limites, impostos pela sua própria condição de herdeiro de um pensamento que se propõe ser universalista. Alguns estudos sugerem novos elementos conceituais a serem desenvolvidos nas pesquisas de campo com populações indígenas, objetivando entender como o corpo aparece representado nas configurações ideológicas veiculadas por essas populações, sua relação com a pessoa e com as forças, espíritos e almas que povoam este e os outros "mundos" acessíveis à experiência. Logo, seu estudo tem como tarefa desvendar um corpo diferente do corpo do homem moderno, herança que se vem construindo desde a Grécia Antiga. Podemos concluir que o corpo é inegavelmente o locus em torno do qual gira a vida das sociedades indígenas brasileiras conforme comprovam estudos de inúmeros antropólogos sendo por isso considerado que para compreender adequadamente a organização social e a cosmologia de uma destas sociedades, é necessário levar-se em consideração a noção de pessoa e o lugar que o corpo humano ocupa na vida das mesmas, na visão que elas fazem de si próprias. Portanto, estudar estas sociedades é procurar nelas compreendê-las.

Coloquio Internacional Lenguaje, Discurso y Civilización (4 : 2006 : La Plata). Lenguaje, discurso y civilización

Tabla de contenidos: El rescate del discurso oral / Pedro Luis Barcia. Uma introduçao ao estudo e cultural da música na Grécia antiga / Fábio Vergara Cerqueira. Lenguaje, discurso y meta-teatralidad en los cantos corales de Séneca / Zelia de Almeida Cardoso. Actualidad y pervivencia del discurso político romano / Gregorio Hinojo Andrés. Lenguaje, discurso y civilización en Baquílides 11 / Ana María González de Tobia. Los ditirambos de Baquílides : Lenguaje, estructura y religiosidad / Fernando García Romero. La represión del adulterio por la Lex iulia de adulteriis coercendis / Marha Patricia Irigoyen Troconis. El imaginario empedocleo / Giuseppina Grammatico. El género lírico entre autoridad poética y prácticas enunciativas : De Goethe a Safo / Claude Calame. La isla y el exilio : Lenguaje y recuperación de la civilización en Odisea / Graciela Cristina Zecchin de Fasano. Homéridas y rehenes / Jaume Pòrtulas. Virgilio y la palabra poética / Antonio Alvar Ezquerra. Falsedad genuina y falsedad verbal en Platón / María Isabel Santa Cruz. El origen de las ideas sobre el espacio y el tiempo / Héctor Vucetich. Homero y Heródoto / Christopher Pelling. Traços teológicos comuns à tragédias de Esquilo : A Teologia de Esquilo no drama Prometheus Demótes / Jaa Torrano. Onoma, érgon y lógos en Helena de Eurípides / Juan Tobías Nápoli. Atenas y Delfos : Adivinación, ley y lenguaje en la Orestíada / Angus Bowie. Linguaggio, discorso e veritá nella Repubblica di Platone / Giovanni Casertano. El estribillo en la poesía clásica, o el poder de la repetición / David Konstan.

Foraminiferal assemblages and stable isotopes across the early Paleogene carbonate facies of Perth Abyssal Plain off Western Australia

Bulk carbonate content, planktic and benthic foraminiferal assemblages, stable isotope compositions of bulk carbonate and Nuttallides truempyi (benthic foraminifera), and non-carbonate mineralogy were examined across ~30 m of carbonate-rich Paleogene sediment at Deep Sea Drilling Project (DSDP) Site 259, on Perth Abyssal Plain off Western Australia. Carbonate content, mostly reflecting nannofossil abundance, ranges from 3 to 80% and generally exceeds 50% between 35 and 57 mbsf. A clay-rich horizon with a carbonate content of about 37% occurs between 55.17 and 55.37 mbsf. The carbonate-rich interval spans planktic foraminiferal zones P4c to P6b (~57-52 Ma), with the clay-rich horizon near the base of our Zone P5 (upper)-P6b. Throughout the studied interval, benthic species dominate foraminiferal assemblages, with scarce planktic foraminifera usually of poor preservation and limited species diversity. A prominent Benthic Foraminiferal Extinction Event (BFEE) occurs across the clay-rich horizon, with an influx of large Acarinina immediately above. The delta13C records of bulk carbonate and N. truempyi exhibit trends similar to those observed in upper Paleocene-lower Eocene (~57-52 Ma) sediment from other locations. Two successive decreases in bulk carbonate and N. truempyi delta13C of 0.5 and 1.0? characterize the interval at and immediately above the BFEE. Despite major changes in carbonate content, foraminiferal assemblages and carbon isotopes, the mineralogy of the non-carbonate fraction consistently comprises expanding clay, heulandite (zeolite), quartz, feldspar (sodic or calcic), minor mica, and pyrolusite (MnO2). The uniformity of this mineral assemblage suggests that Site 259 received similar non-carbonate sediment before, during and after pelagic carbonate deposition. The carbonate plug at Site 259 probably represents a drop in the CCD from ~57 to 52-51 Ma, as also recognized at other locations.

Grain-size and bulk and clay mineralogy of ODP Leg 204 sediments

We present grain size, granulometric statistical parameters, and calcium carbonate content of sediment samples from the summit and east and west flanks of southern Hydrate Ridge (Sites 1244-1250). These data are compared with magnetic susceptibility measurements from the same intervals. Bulk and clay mineralogy from Sites 1244 (east flank), 1247 (west flank), and 1250 (summit) are also presented. The integration of these data allows us to characterize the main sedimentary facies and composition of the Quaternary age sediments from southern Hydrate Ridge.

Maestrichtian through Neogene benthic foraminifers of Maud Rise

Upper abyssal to lower bathyal benthic foraminifers from ODP Sites 689 (present water depth 2080 m) and 690 (present water depth 2941 m) on Maud Rise (eastern Weddell Sea, Antarctica) are reliable indicators of Maestrichtian through Neogene changes in the deep-water characteristics at high southern latitudes. Benthic foraminiferal faunas were divided into eight assemblages, with periods of faunal change at the early/late Maestrichtian boundary (69 Ma), at the early/late Paleocene boundary (62 Ma), in the latest Paleocene (57.5 Ma), in the middle early Eocene to late early Eocene (55-52 Ma), in the middle middle Eocene (46 Ma), in the late Eocene (38.5 Ma), and in the middle-late Miocene (14.9-11.5 Ma). These periods of faunal change may have occurred worldwide at the same time, although specific first and last appearances of deep-sea benthic foraminifers are commonly diachronous. There were minor faunal changes at the Cretaceous/Tertiary boundary (less than 14?7o of the species had last appearances at Site 689, less than 9% at Site 690). The most abrupt benthic foraminiferal faunal event occurred in the latest Paleocene, when the diversity dropped by 50% (more than 35% of species had last appearances) over a period of less than 25,000 years; after the extinction the diversity remained low for about 350,000 years. The highest diversities of the post-Paleocene occurred during the middle Eocene; from that time on the diversity decreased steadily at both sites. Data on faunal composition (percentage of infaunal versus epifaunal species) suggest that the waters bathing Maud Rise were well ventilated during the Maestrichtian through early Paleocene as well as during the latest Eocene through Recent. The waters appeared to be less well ventilated during the late Paleocene as well as the late middle through early late Eocene, with the least degree of ventilation during the latest Paleocene through early Eocene. The globally recognized extinction of deep-sea benthic foraminifers in the latest Paleocene may have been caused by a change in formational processes of the deep to intermediate waters of the oceans: from formation of deep waters by sinking at high latitudes to formation of deep to intermediate water of the oceans by evaporation at low latitudes. Benthic foraminiferal data (supported by carbon and oxygen isotopic data) suggest that there was a short period of intense formation of warm, salty deep water at the end of the Paleocene (with a duration of about 0.35 m.y.), and that less intense, even shorter episodes might have occurred during the late Paleocene and early Eocene. The faunal record from the Maud Rise sites agrees with published faunal and isotopic records, suggesting cooling of deep to intermediate waters in the middle through late Eocene.

Benthic foraminifera and stable isotope composition in Paleocene-Eocene sediments

In the late Paleocene to early Eocene, deep sea benthic foraminifera suffered their only global extinction of the last 75 million years and diversity decreased worldwide by 30-50% in a few thousand years. At Maud Rise (Weddell Sea, Antarctica; Sites 689 and 690, palaeodepths 1100 m and 1900 m) and Walvis Ridge (Southeastern Atlantic, Sites 525 and 527, palaeodepths 1600 m and 3400 m) post-extinction faunas were low-diversity and high-dominance, but the dominant species differed by geographical location. At Maud Rise, post-extinction faunas were dominated by small, biserial and triserial species, while the large, thick-walled, long-lived deep sea species Nuttallides truempyi was absent. At Walvis Ridge, by contrast, they were dominated by long-lived species such as N. truempyi, with common to abundant small abyssaminid species. The faunal dominance patterns at the two locations thus suggest different post-extinction seafloor environments: increased flux of organic matter and possibly decreased oxygen levels at Maud Rise, decreased flux at Walvis Ridge. The species-richness remained very low for about 50 000 years, then gradually increased. The extinction was synchronous with a large, negative, short-term excursion of carbon and oxygen isotopes in planktonic and benthic foraminifera and bulk carbonate. The isotope excursions reached peak negative values in a few thousand years and values returned to pre-excursion levels in about 50 000 years. The carbon isotope excursion was about -2 per mil for benthic foraminifera at Walvis Ridge and Maud Rise, and about -4 per mil for planktonic foraminifera at Maud Rise. At the latter sites vertical gradients thus decreased, possibly at least partially as a result of upwelling. The oxygen isotope excursion was about -1.5 per mil for benthic foraminifera at Walvis Ridge and Maud Rise, -1 per mil for planktonic foraminifera at Maud Rise. The rapid oxygen isotope excursion at a time when polar ice-sheets were absent or insignificant can be explained by an increase in temperature by 4-6°C of high latitude surface waters and deep waters world wide. The deep ocean temperature increase could have been caused by warming of surface waters at high latitudes and continued formation of the deep waters at these locations, or by a switch from dominant formation of deep waters at high latitudes to formation at lower latitudes. Benthic foraminiferal post-extinction biogeographical patterns favour the latter explanation. The short-term carbon isotope excursion occurred in deep and surface waters, and in soil concretions and mammal teeth in the continental record. It is associated with increased CaC03-dissolution over a wide depth range in the oceans, suggesting that a rapid transfer of isotopically light carbon from lithosphere or biosphere into the ocean-atmosphere system may have been involved. The rapidity of the initiation of the excursion (a few thousand years) and its short duration (50 000 years) suggest that such a transfer was probably not caused by changes in the ratio of organic carbon to carbonate deposition or erosion. Transfer of carbon from the terrestrial biosphere was probably not the cause, because it would require a much larger biosphere destruction than at the end of the Cretaceous, in conflict with the fossil record. It is difficult to explain the large shift by rapid emission into the atmosphere of volcanogenic CO2, although huge subaerial plateau basalt eruptions occurred at the time in the northern Atlantic. Probably a complex combination of processes and feedback was involved, including volcanogenic emission of CO2, changing circulation patterns, changing productivity in the oceans and possibly on land, and changes in the relative size of the oceanic and atmospheric carbon reservoirs.

Analytical results from sediment core MD03-2698

It is well established that orbital scale sea-level changes generated larger transport of sediments into the deep-sea during the last glacial maximum than the Holocene. However, the response of sedimentary processes to abrupt millennial-scale climate variability is rather unknown. Frequency of distal turbidites and amounts of advected detrital carbonate are estimated off the Lisbon-Setúbal canyons, within a chronostratigraphy based on radiometric ages, oxygen isotopes and paleomagnetic key global anomalies. We found that: 1) Higher frequency of turbidites concurred with Northern Hemisphere coldest temperatures (Greenland Stadials [GS], including Heinrich [H] events). But more than that, an escalating frequency of turbidites starts with the onset of global sea-level rising (and warming in Antarctica) and culminates during H events, at the time when rising is still in its early-mid stage, and the Atlantic Meridional Overturning Circulation (AMOC) is re-starting. This short time span coincides with maximum gradients of ocean surface and bottom temperatures between GS and Antarctic warmings (Antarctic Isotope Maximum; AIM 17, 14, 12, 8, 4, 2) and rapid sea-level rises. 2) Trigger of turbidity currents is not the only sedimentary process responding to millennial variability; land-detrital carbonate (with a very negative bulk d18O signature) enters the deep-sea by density-driven slope lateral advection, accordingly during GS. 3) Possible mechanisms to create slope instability on the Portuguese continental margin are sea-level variations as small as 20 m, and slope friction by rapid deep and intermediate re-accommodation of water masses circulation. 4) Common forcing mechanisms appear to drive slope instability at both millennial and orbital scales.

Upper Maestrichtian to Eocene benthic foraminifera in ODP Leg 121 holes

Late Maestrichtian to late Eocene bathyal benthic foraminiferal faunas at Sites 752,753, and 754 on Broken Ridge in the eastern Indian Ocean were analyzed as to their stratigraphic distribution of species to clarify the relation between faunal turnovers and paleoceanographic changes. Based on Q-mode factor analysis, eight varimax assemblages were distinguished: the Stensioina beccariiformis assemblage in the upper Maestrichtian to upper Paleocene; the Cibicidoides hyphalus assemblage in the upper Maestrichtian; the Cibicidoides cf. pseudoperlucidus assemblage in the upper Paleocene; the Anomalinoides capitatusldanicus assemblage in the uppermost Paleocene to lower Eocene; the Cibicidoides subspiratus assemblage in the lower Eocene; the Nuttallides truempyi assemblage in the lower and middle Eocene; the Osangularia sp. 1 - Hanzawaia ammophila assemblage in the upper Eocene; and the Lenticulina spp. assemblage in the uppermost Eocene, Oligocene, and lower Miocene. The presence of the Osangularia sp. 1 - Hanzawaia ammophila assemblage is related to the shallowing episode on Broken Ridge (upper bathyal), as a result of the rifting event that occurred in the middle Eocene. The most distinct faunal change (the disappearance of about 37% of the species) occurred between the S. beccariiformis assemblage and the A. capitatusldanicus assemblage, at the end of the upper Paleocene. A. capitatusldanicus, Lenticulina spp., and varied forms of Cibicidoides replaced the Velasco-type fauna at this time. The timing of this event is well correlated with the known age at South Atlantic sites (Thomas, 1990 doi:10.2973/odp.proc.sr.113.123.1990; Kennett and Stott, 1990 doi:10.2973/odp.proc.sr.113.188.1990; Katz and Miller, 1990 doi:10.2973/odp.proc.sr.114.147.1991). The primary cause of the extinction of the Stensioina beccariiformis assemblage is elusive, but may have resulted from the cessation of deep-water formation in the Antarctic (Katz and Miller, 1990), and subsequent arrival of warm saline deep water (Thomas, 1990; Kennett and Stott, 1990). Another possibility may be a weakened influence of high-salinity water formed at the low latitudes such as the Tethys Sea. The extinction event corresponds to the change from higher delta13C values in benthic foraminifers to lower ones. An interpretation of delta13C values is that the eastern Indian deep water, characterized by young and nutrient-depleted water, became old water which was devoid of a supply of new water during the latest Paleocene to early Eocene. Prior to this benthic event, signals of related faunal change were detected in the following short periods: early and late Paleocene, near the boundary of nannofossil Zone CP4, and Zone CP5 of the late Paleocene at Site 752. Among common taxa in the upper Maestrichtian, only seven species disappeared or became extinct at the Cretaceous/ Tertiary boundary at Site 752. The benthic foraminiferal population did not change for up to 2 m above the boundary, in contrast to the rapid decrease of the plankt onic foraminiferal population at the boundary. A decrease in the number of benthic foraminifers occurs after that level, corresponding to an interval of decreased numbers of planktonic foraminifers and higher abundance of volcanic ash. Reduced species diversity (H') suggests a secondary effect attributable to the dissolution of foraminiferal tests. The different responses of planktonic and benthic foraminifers to the event just above the boundary suggest that the Cretaceous/Tertiary event was a surface event as also suggested by Thomas (1990). In addition, a positive shift of delta13C in benthic foraminifers after the event indicates nutrient-depleted bottom water at Site 752.

Paleogene benthic foraminifera from the Kerguelen Plateau

Benthic foraminifers were studied from lower Paleocene through upper Oligocene sections from Sites 747 and 748. The composition of the benthic foraminifer species suggests a middle to lower bathyal (600-2000 m) paleodepth during the Neogene and a probable upper abyssal (2000-3000 m) paleodepth during the Paleocene at Site 747. Site 748 is thought to have remained at middle to lower bathyal paleodepths throughout the Cenozoic. Principal component analysis distinguished four major benthic foraminifer assemblages: (1) a Paleocene Stensioina beccariiformis assemblage at Sites 747 and 748, (2) an early Eocene Nuttallides truempyi assemblage at lower bathyal Site 747, (3) an early through middle Eocene Stilostomella-Lenticulina assemblage at middle bathyal Site 748, and (4) a latest Eocene through Oligocene Cibicidoides-Astrononion pusillum assemblage at both sites. Major benthic foraminifer changes, as indicated by the principal components and first and last appearances, occurred at or close to the Paleocene/Eocene boundary, and in the late Eocene close to the middle/late Eocene boundary.