A partir do padrão de distribuição das associações de foraminíferos ao longo de dois testemunhos e da sua correlação com características abióticas do sedimento, detectaram-se variações ambientais holocênicas ocorridas em dois embaiamentos marinhos rasos: as enseadas do Flamengo (Testemunho UB1) e da Fortaleza (Testemunho UB3), em Ubatuba, SP. Posteriormente, correlações foram estabelecidas entre as mudanças da composição faunística e curvas de variação do nível do mar existentes na literatura. O testemunho UB1 possui 222 cm de profundidade e foi coletado no Saco da Ribeira sob lâmina de água de 3,10 m. É constituído predominantemente por sedimentos sílticos que contêm fragmentos vegetais e biodetríticos. Camadas arenosas são encontradas em sua base, datada em 7290 + 40 anos A.P., e à profundidade compreendida entre 32 e 12 cm. O testemunho UB3 tem 342 cm de profundidade e foi coletado na Praia do Lázaro sob lâmina de água de 3,80 m. Seus sedimentos são predominantemente sílticos, contendo fragmentos vegetais, fragmentos vegetais oxidados e fragmentos biodetríticos. Seqüências arenosas e arenosiltosas são encontradas em sua base, datada em 7.530 + 40 anos A.P., e entre 32 e 12 cm de profundidade. Foram identificados 76 espécies e 40 gêneros de foraminíferos bentônicos e uma espécie de foraminífero planctônico nas 58 amostras analisadas, a cada 10 cm, ao longo dos dois testemunhos (23 amostras em UB1 e 35 em UB3). As associações observadas são típicas de ambiente marinho normal, de plataforma interna, com tendência redutora. Foraminíferos de testas hialinas predominam sobre foraminíferos de testas porcelanosas. Somente uma espécie de testa aglutinante foi encontrada em cinco amostras dispersas ao longo do testemunho UB3. As espécies bioindicadoras indicam ambientes com predominância da massa de Água Costeira, com energia de fundo moderada, alta acumulação de matéria orgânica e baixas concentrações de oxigênio, tanto para a Praia do Lázaro quanto para o Saco da Ribeira, nos últimos 7.500 anos A.P. Evidenciam, também, que a circulação de fundo no Saco da Ribeira se tornou cada vez mais restrita, enquanto na Praia do Lázaro a circulação hidrodinâmica não sofreu forte alteração. Os dados tafonômicos indicam que não houve processos post mortem capazes de alterar por completo as associações de foraminíferos analisadas ao longo de ambos os testemunhos. Todas as evidências microfaunísticas sugerem que houve, pelo menos, duas fases distintas de comportamento marinho para as duas enseadas ao longo dos últimos 7.500 anos A.P.: uma primeira, transgressiva, que teria durado até a, aproximadamente, 5.100 anos A.P., durante a qual as enseadas se encontravam conectadas; e outra de caráter geral regressivo, que se estendeu até a, pelo menos, 32 cm de profundidade em ambos os testemunhos, durante a qual teria surgido o Tômbolo do Saco da Ribeira, que passou a impedir a circulação entre a Praia do Lázaro e o Saco da Ribeira. / Variations in Holocene environments in the marine bays of Flamengo and Fortaleza at Ubatuba, State of São Paulo, southeast Brazil, were detected in cores UB1 and UB3, respectively, on the basis of the distribution pattern of foraminiferal associations and their correlation with abiotic characteristics of the sediments. Correlations were then established between changes in faunistic composition and existing sea-level variation curves. The UB1 Core measures 222 cm and was collected at Saco da Ribeira at a water depth of 3.1 m. This core is predominantly made up of silty sediments with biodetritus and plant fragments. Arenaceous layers at its base were dated by radiocarbon at 7.290 + 40 years B.P., and also occur between 32 and12 cm depth. The UB3 Core measures 342 cm and was collected at Praia do Lázaro at a water depth of 3.8 m. It is predominantly silty and contains fragments of plants, oxidized plants and biodetritus. Sandy and muddy sand layers were encountered at its base, with a radiocarbon age of 7.530 + 40 years B.P., and between 32 and 12 cm of depth. 76 species and 40 genera of benthic foraminifera and one species of planktonic foraminifera were identified in the cores. The observed associations are typical of normal marine, inner shelf environments, with low oxygen. Hyaline foraminifera predominate over porcelaneous species. Only one species of agglutinated test was found within the five samples of the UB3 Core. The bioindicator species indicate environments with a predominance of Coastal Water (CA), moderate hydrodynamic energy, high organic matter accumulation and low oxygen concentrations for both Praia do Lázaro and Saco da Ribeira since early on. They also show that the deep marine circulation in Saco da Ribeira has become ever more restricted from approximately 7.500 years B.P. until the present, while in Praia do Lázaro, deep circulation has not suffered any strong alteration. Taphonomical data suggest that there is no post mortem process capable of completely modifying the foraminiferal associations analyzed in the cores. All the microfaunistic evidence suggests at least two distinct phases of marine behavior for the two bays over the past 7.500 years: a former transgressive phase, that lasted until approximately 5.100 years B.P., during which the bays were connected; and a latter generally regressive phase, that would have extended itself until, at least, the depth of 32 cm in both cores, during which the appearance of the Tômbolo do Saco da Ribeira would have begun to hinder circulation between Praia do Lázaro and Saco da Ribeira.

A partir do padrão de distribuição das associações de foraminíferos ao longo de dois testemunhos e da sua correlação com características abióticas do sedimento, detectaram-se variações ambientais holocênicas ocorridas em dois embaiamentos marinhos rasos: as enseadas do Flamengo (Testemunho UB1) e da Fortaleza (Testemunho UB3), em Ubatuba, SP. Posteriormente, correlações foram estabelecidas entre as mudanças da composição faunística e curvas de variação do nível do mar existentes na literatura. O testemunho UB1 possui 222 cm de profundidade e foi coletado no Saco da Ribeira sob lâmina de água de 3,10 m. É constituído predominantemente por sedimentos sílticos que contêm fragmentos vegetais e biodetríticos. Camadas arenosas são encontradas em sua base, datada em 7290 + 40 anos A.P., e à profundidade compreendida entre 32 e 12 cm. O testemunho UB3 tem 342 cm de profundidade e foi coletado na Praia do Lázaro sob lâmina de água de 3,80 m. Seus sedimentos são predominantemente sílticos, contendo fragmentos vegetais, fragmentos vegetais oxidados e fragmentos biodetríticos. Seqüências arenosas e arenosiltosas são encontradas em sua base, datada em 7.530 + 40 anos A.P., e entre 32 e 12 cm de profundidade. Foram identificados 76 espécies e 40 gêneros de foraminíferos bentônicos e uma espécie de foraminífero planctônico nas 58 amostras analisadas, a cada 10 cm, ao longo dos dois testemunhos (23 amostras em UB1 e 35 em UB3). As associações observadas são típicas de ambiente marinho normal, de plataforma interna, com tendência redutora. Foraminíferos de testas hialinas predominam sobre foraminíferos de testas porcelanosas. Somente uma espécie de testa aglutinante foi encontrada em cinco amostras dispersas ao longo do testemunho UB3. As espécies bioindicadoras indicam ambientes com predominância da massa de Água Costeira, com energia de fundo moderada, alta acumulação de matéria orgânica e baixas concentrações de oxigênio, tanto para a Praia do Lázaro quanto para o Saco da Ribeira, nos últimos 7.500 anos A.P. Evidenciam, também, que a circulação de fundo no Saco da Ribeira se tornou cada vez mais restrita, enquanto na Praia do Lázaro a circulação hidrodinâmica não sofreu forte alteração. Os dados tafonômicos indicam que não houve processos post mortem capazes de alterar por completo as associações de foraminíferos analisadas ao longo de ambos os testemunhos. Todas as evidências microfaunísticas sugerem que houve, pelo menos, duas fases distintas de comportamento marinho para as duas enseadas ao longo dos últimos 7.500 anos A.P.: uma primeira, transgressiva, que teria durado até a, aproximadamente, 5.100 anos A.P., durante a qual as enseadas se encontravam conectadas; e outra de caráter geral regressivo, que se estendeu até a, pelo menos, 32 cm de profundidade em ambos os testemunhos, durante a qual teria surgido o Tômbolo do Saco da Ribeira, que passou a impedir a circulação entre a Praia do Lázaro e o Saco da Ribeira. / Variations in Holocene environments in the marine bays of Flamengo and Fortaleza at Ubatuba, State of São Paulo, southeast Brazil, were detected in cores UB1 and UB3, respectively, on the basis of the distribution pattern of foraminiferal associations and their correlation with abiotic characteristics of the sediments. Correlations were then established between changes in faunistic composition and existing sea-level variation curves. The UB1 Core measures 222 cm and was collected at Saco da Ribeira at a water depth of 3.1 m. This core is predominantly made up of silty sediments with biodetritus and plant fragments. Arenaceous layers at its base were dated by radiocarbon at 7.290 + 40 years B.P., and also occur between 32 and12 cm depth. The UB3 Core measures 342 cm and was collected at Praia do Lázaro at a water depth of 3.8 m. It is predominantly silty and contains fragments of plants, oxidized plants and biodetritus. Sandy and muddy sand layers were encountered at its base, with a radiocarbon age of 7.530 + 40 years B.P., and between 32 and 12 cm of depth. 76 species and 40 genera of benthic foraminifera and one species of planktonic foraminifera were identified in the cores. The observed associations are typical of normal marine, inner shelf environments, with low oxygen. Hyaline foraminifera predominate over porcelaneous species. Only one species of agglutinated test was found within the five samples of the UB3 Core. The bioindicator species indicate environments with a predominance of Coastal Water (CA), moderate hydrodynamic energy, high organic matter accumulation and low oxygen concentrations for both Praia do Lázaro and Saco da Ribeira since early on. They also show that the deep marine circulation in Saco da Ribeira has become ever more restricted from approximately 7.500 years B.P. until the present, while in Praia do Lázaro, deep circulation has not suffered any strong alteration. Taphonomical data suggest that there is no post mortem process capable of completely modifying the foraminiferal associations analyzed in the cores. All the microfaunistic evidence suggests at least two distinct phases of marine behavior for the two bays over the past 7.500 years: a former transgressive phase, that lasted until approximately 5.100 years B.P., during which the bays were connected; and a latter generally regressive phase, that would have extended itself until, at least, the depth of 32 cm in both cores, during which the appearance of the Tômbolo do Saco da Ribeira would have begun to hinder circulation between Praia do Lázaro and Saco da Ribeira.

A dissolução do carbonato está ligada à circulação dos oceanos e às variações climáticas. Através desse estudo foi possível identificar, durante o último ciclo glacial (150 mil anos), três eventos de dissolução na Bacia de Santos, durantes os estágios isotópicos marinhos 5d, 5b e 4. Para isso foram utilizados indicadores de dissolução micropaleontológicos, geoquímicos e sedimentares. Através destes indicadores foi possível inferir quais processos estão associados à dissolução do carbonato durante estes períodos. Os indicadores micropaleontológicos densidade área (ρA), espécies resistentes à dissolução (ERD e BDI) e índice de fragmentação (IF) foram capazes de identificar o início dos eventos de dissolução, enquanto os indicadores de variação tamanho de grão no sedimento bruto, teor de carbonato de cálcio (%CaCO3) em diferentes frações de tamanho, razão entre foraminíferos bentônicos e planctônicos (B/P) e peso normalizado (SBW) foram relacionados ao auge da dissolução. Os indicadores com base em cocolitoforídeos (CEX\'), índice Broecker/Clark e índice Chiu/Broecker apresentaram resultados inconclusivos. Observou-se que durante os três eventos de dissolução houve um aumento na contribuição de uma massa d\'água de origem sul (mais corrosiva ao carbonato) na região, indicado a partir da variação de δ13Cbentônico. Os eventos de dissolução também coincidiram com o aumento do aporte de sedimento não-carbonático (indicador de aporte continental, Fe/Ti e Ti/Ca). Os indicadores de paleoprodutividade (PP, RN e razão G. bulloides/G. ruber) não indicaram um aumento de produtividade primária durante os eventos de dissolução, de modo que a produtividade não foi considerada como um dos processos principais que induziram os eventos de dissolução neste estudo. As profundidades em que estes testemunhos se encontram (∼2000 m) também eliminam a possibilidade de que a dissolução tenha ocorrido em função da variação da posição da lisoclina, mesmo considerando que esta tenha estado ∼1000 m mais rasa durante o último período glacial. Desta forma, acreditamos que os eventos de dissolução estejam relacionados com a maior contribuição de uma massa d\'água de sul, mais corrosiva ao carbonato, em torno de 2000 m de profundidade, durante os MIS 5d, 5b e 4, como resultado da reorganização das massas d\'água profundas na região (uma redução na intensidade da AMOC) nestes períodos. / The calcium carbonate dissolution is linked to ocean circulation and climate change. Through this study it was possible to identify, during last glacial cycle (150 kyrs), three dissolution events occurring in the Santos Basin, during MIS 5d, 5b and 4. For this, micropaleontological, geochemical and sedimentary proxies were used. Through these proxies it was possible to infer which processes are associated with the carbonate dissolution during this period. The micropaleontological proxies of area density (ρA), dissolution resistent species (ERD and BDI) and fragmentation index (IF), were able to identify the beginning of the dissolution events, while the proxies of grain size variation, calcium carbonate content in different size fractions, benthic/planktonic ratio (B/P) and size normalized weight (SBW) were related with the dissolution peak. The proxies based in cocoliths (CEX\'), Broecker/Clark Index and Chiu/Broecker Index presented inconclusive results. It was observed that during the three dissolution events there was an increase in the contribution of the water mass of southern origin (more corrosive to the carbonate) in the region, indicated from the variation of δ13C in benthic foraminifera. This increase also coincided with the increase in the contribution of non-carbonate sediment (continental input indicator -IAC, Fe/Ca and Ti/Ca). The paleoproductivity proxies (based in cocoliths - PP, RN, and G. bulloides/G. ruber ratio) did not indicate an increase in primary productivity during dissolution events, therefore productivity was not considered as one of the processes that led to dissolution in this study. The depths at which these sediment cores are found (∼2000 m) also eliminate the possibility that the dissolution occurred as a function of the variation of the position of the lysocline, even if considering that it was ∼1000 m shallower during the last glacial period. In this way, we believe that the dissolution events are related to an increased southern-sourced water mass more corrosive to the carbonate during MIS 5d, 5b and 4, which implies the reorganization of the water masses in the region and a reduction in the strength of AMOC during these periods.

Coral reefs are threatened in Florida and worldwide. Successful resource management requires rapid identification of anthropogenic sources of stress before they affect the reef community. I tested a multi-scale approach for assessing reef condition at seven reefs within the Florida Keys National Marine Sanctuary and Biscayne National Park between 2001 and 2003. I examined multiple environmental parameters to identify potential sources of stress. I utilized the Atlantic and Gulf Rapid Reef Assessment Biotic Reef Index to assess benthic community structure and an indicator species of Foraminifera (Amphistegina gibbosa) to determine if environmental conditions were suitable for calcareous organisms that host algal endosymbionts. Small tissue samples were extracted from colonies of Montastraea annularis species complex to assay a suite of cellular biomarkers to elucidate possible mechanisms of the coral stress response. I monitored regeneration rates of the resultant lesions to determine if the coral colonies were capable of recovering from damage. Multivariate data analyses indicated that corals at all study sites were experiencing stress with different degrees of response and decline. On reefs with coarse grain sediments that are adjacent to an intact mangrove shoreline, the Cellular Diagnostic System indicated that corals were responding to a xenobiotic stress but appeared to be compensating as evidenced by consistently high lesion regeneration rates, a high percentage of healed lesions, low coral mortality and high abundances of A. gibbosa. On reefs with silt-sized sediments adjacent to developed coastlines, corals also were responding to xenobiotic stresses, but were negatively affected as evidenced by low regeneration rates, a low percentage of healed lesions, high coral mortality, and low abundances of A. gibbosa. Corals at an 18 m offshore site exhibited abnormally low biomarker levels and some died during the study, indicating that sampled colonies were incapable of upregulating necessary protective proteins. Further research will be required to determine stressor sources. This study demonstrates that a multiple-indicator approach, spanning scales from cellular to community, can provide marine resource managers with data linking decline of coral populations to specific environmental conditions and events, thereby providing potential for early detection of stressors allowing for preventive management.

The foraminiferal population of Yaquina Bay was investigated to attempt a correlation of seasonal changes in the hydrography with observed changes in the faunal distribution patterns. The results are based on data from two spatial surveys conducted in July 1966, and late February and March, 1967. The hydrography of Yaquina Bay undergoes seasonal changes closely paralleling the seasonal precipitation pattern. Except for short-term variations, the estuarine system is partly-mixed during the period of maximum river discharge (November to May) and wellmixed from June through October. Coastal upwelling (high salinity, low temperature) has a marked influence on the hydrography of the lower bay during the summer; maximum salinities and temperatures prevail in the upper reaches of the estuary during late summer and fall. Species associations were determined by the Fager-McConnaughey correlation coefficient method; similar assemblages were found for both summer and winter surveys. A marine biofacies fauna, dominated by Elphidium microgranulosum and E. frigidum, occupies the main estuary channel for about five miles upstream. The distributional patterns of the living fauna show evidence of a stronger marine influence during the summer, corresponding to a similar pattern in the hydrography. In the lower bay, the Elphidium fauna is displaced laterally by an assemblage characterized by Trochammina charlottensis and Elphidium incertum in the middle intertidal zone. This assemblages in turn gives way to an Ammobaculites exiguus -Miliammina fusca fauna in the upper intertidal area. The Elphidium assemblage gives way to a Miliammina fauna in the upstream direction. Trochammina inflata, T. macrescens, Miliammina fusca, Jadamminina polystoma, Haplophragmoides sp., H. hancocki and Siphotrochammina lobata are the principal species found in the marine marsh. Zones of environmental similarity were defined by the index of affinity association analysis. Living and total faunas of both winter and summer surveys were considered separately; several sample groups were defined in each case. Index of affinity data can also be used to provide an index of the marine influence on the foraminiferal population of the estuary. Species diversity or the average number of species/sample, ranges from 22 in the marine biofacies zone to six on the lower bay tideflats. An intermediate value (l0/sample)was found for the marine marsh. Highest standing crops were found in the marshes (summer) and on the tideflats adjacent to the lower bay channel, averaging 40 and 42/cm² respectively. Lowest values (1 to 2 cm²) were found in the middle to upper intertidal areas of the lower bay during the summer. The distribution of the total fauna is quite similar to that of the living population. Highest average values (175/cm³) are again found in the marine marsh and in the marine biofacies zone (70 to 80/cm³). Lowest values occur on the lower bay intertidal areas (3 to 9/cm³). In general, the percentage representation of agglutinated species in the total fauna increases with distance upstream in the channel and with distance laterally from the channel axis. Faunas of some marsh stations are composed entirely of agglutinated species. The percentage of calcareous hyaline species shows an inverse relation to that of the agglutinated fauna, increasing in importance with approach to marine conditions. Porcelaneous and planktonic species are generally minor constituents in the total fauna and are restricted to the marine biofacies as it is developed in the estuary. Foraminifer-ostracod ratios are extremely variable in the environments sampled in Yaquina Bay. Smooth-valved species are characteristic of the marine marsh and inner bay environments; valve ornamentation tends to increase with approach to marine conditions. Thecamoebians are present in low numbers throughout the estuary. In general however, the number of species and population size increases in the upstream direction. / Graduation date: 1968

Graduation date: 1952

Two drilled cores were collected from the Jhuoshuei River delta for this study, which is focused on the analyses of sedimentological, statistical analysis, AMS C14 dating and paleoenvironment interpretation based on the benthic foraminiferal fossils. Foraminiferal shell do not exist between 30000 and 12000 yr B.P., indicating the environment of this sections might be terrestrial. Between 12000 and 8000 yr B.P., the southern core do not have traces of foraminifera, suggesting the deposition site was terrestrial. The northern core contains the benthic foraminiferal shell between 12000 and 9000 yr B.P. The foraminiferal assemblage indicates the sedimentation might be a inner shelf like enviroment. An estuarine like environment was suggested between 9000 and 8000 yr B.P.. Between 8000 and 6000 yr B.P., foraminiferal cluster analysis indicates a middle to inner shelf environment at the southern core site; a inner shelf at the northern core. From 6000 to 3000 yr B.P., foraminiferal cluster analysis indicates a inner shelf at the south core while northern core foraminifera became fewer and the environment gradually changing to terrestrial facies. From 3000 yr B.P. upwards, foraminiferal cluster analysis indicates a shallower inner shelf at the southern core. From 2000 yr B.P. to today, the southern core changed to terrestrial.

The surface sediments off Southwestern Taiwan were collected during three different cruises in May 2009, November 2009, and March 2010, respectively. The concentrations of chlorophyll-a and phaeopigment, as well as benthic foraminifera species, were analyzed. The results show that the concentration of chlorophyll-a decreases with the distance from the shore, and the concentration of chlorophyll-a also decreases with increasing water depth. The concentration of phaeopigment seems to have no significant relationship with the water depth. The relationships between the concentrations of benthic foraminifera, chlorophyll-a, and phaeopigment are also not significant. Because samples were collected from different water depths on the continental shelf, slope and in a canyon, the oceangraphic setting therefore may be one of the main factors which influences the distribution pattern of benthic foraminifera. According to the EOF analysis, the water depth in sampling sites plays a very important role in terms of the distribution of living benthic foraminifera in this study. The distribution do not show significant difference between collecting seasons. Finally, the concentrations of the chlorophyll-a and phaeopigment decrease drastically in a downcore record. Quinqueloculina spp., an epifaunal foraminifer, shows a significant peak concentration in the depth of 5-6 cm downcore. Bioturbation probably was responsible for this change.

The Region of Western Pacific Warm Pool (WPWP) is closely related to Global climate system. Previous studies indicate that the region of WPWP is affected by Walker circulation (WC) and Hadley cell (HC). WPWP expands when WC becomes stronger or when HC becomes weaker, and contracts when WC becomes weaker or when HC becomes stronger. In this study, records derived from core ODP1115B, including stable oxygen and carbon isotopes are used to reconstruct the long-term hydrological variations of WPWP over the past 2.2 Ma. We compared two species of foraminifera: Neogloboquadrina dutertrei and Globigerinoides sacculifer, for the reconstruction of differences between surface water and oceanic subsurface water. We try to find out the relationships between the thermocline depth in southern WPWP, the region of WPWP, HC and WC. However, our records indicate that the depth of thermocline in southern WPWP may be effected by the region of WPWP and the hydrology of southern WPWP. According to the Paleothermometry records of ODP806, ODP847, ODP1115 and MD063018, we can explain the relationship between WC, HC and the region of WPWP. Before 1.8 Ma, southern WPWP may not be affected by weak WC. During 1.8~1.2 Ma, WC becomes stronger and effect the region of WPWP. At the period of 1.2~0.9 Ma, southward migration of WPWP enhanced the influence of WC on the region of south WPWP and the depth of thermocline, then weakened HC in the southern hemisphere. After 0.9 Ma, the variation of hydrology in southern WPWP may be affected by stronge WC, not HC. We suggest that the influence of HC in southern WPWP is resulted in the southern region of WPWP.

The objective for this study was to provide the insight into the link between benthic foraminiferal assemblages and the surrounding environment. Stained sediment samples were collected from the continental shelf and slope off the southwest Taiwan, including the Kao-ping Submarine Canyon. In addition to faunal census, total organic carbon (TOC), carbonate, and coarse fraction of the sediments were also measured. Nevertheless, the downcore record of the excess 210Pb from selected sites offers the constraint for stratigraphy time frame for discussion. The benthic foraminiferal assemblages were analyzed by statistics. Clusters analysis shows that all species present in this study could be divided into two groupings. One is those distributed in outer shelf and the other is those found in the inner shelf of the southwest Taiwan. Different from previous studies, the spatial distribution of stained benthic foraminifera seems not to be related with TOC contents in the sediment and water depth. Both the diversity index and Eqitability show that sites inside of the canyon have lower values. The higher Living/Total ratios and lower dead tests at the head of Kao-ping Submarine Canyon than adjacent area might be the effect of migration. Furthermore, the species within the canyon are similar to the southern and northern continental shelf. These findings indicate that the spatial distribution of benthic forams within canyon might be the effect of transport, which could result from the complex interaction between tides and currents. Augmented with the profiles of excess 210Pb, the temporal variation of benthic foraminifera was revealed. Generally there is a progressive decrease in the abundance of Ammonia sp.. It is possible that the diminishing trend was caused by the increase of anthropogenic activity for the last 30 years.