4 resultados para PHOSPHATE ROCKS
Resumo:
Algarve Province, Southern Portugal, corresponds in part to a meso-cenozoic basin running along the coast from Cabo S. Vicente to beyond Spanish border. Structurally it is a big monocline plunging southwards much deformed mainly by two East-West longitudinal flexures. Lithostratigraphical and chronostratigraphical studies dealt specially with Jurassic formations. This and the geological mapping of the post-Hercynian sedimentary formations allow us to define the following units: Triassic-Lower Liassic Arenitos de Silves (Silves sandstones sensu P. Choffat, pro parte) - At their base the Silves sandstones (0-150m) are represented mainly by cross-bedded red sandstones. This unit is Upper Triassic (Keuper) in age, on the evidence of some Brachiopoda. Complexo margo-carbonatado de Silves (Silves marl-limestone complex=Silves sandstones sensu P. Choffat, pro parte) (80-200m) overlies the preceding, it may be reported to the Upper Triassic-Hettangian. It consists of a thick pelite-marl-dolomite-limestone series with many intercalations of greenstones. Since no fossils were found it is not possible to conclude whether it is still Hettangian or if it does correspond, in the whole or in part, already to the Sinemurian. Liassic Dolomitos e calcários dolomíticos de Espiche (Espiche dolomite-rocks and dolomitic-limestones) - The usually massive and finely crystalline or saccharoidal dolomites and dolomitic-limestones are the toughest strata of the Algarve margin giving rise to several hills. Its thickness attains in certain points 60 metres at least. Based on geometry and on lithological similarities with the carbonated complex of the northern basin of Tagus river (Peniche, São Pedro de Muel, Quiaios), this formation can be accepted as Sinemurian in age. As it happens with the carbonated complex, here also the first dolomite beds are non-isochronal throughout the region; upper time-limit of the dolomitic facies is either Lower Carixian, Lower Toarcian or even Lower Dogger. The dolomitization is secondary but not much later than sedimentation. However, between Cabo S. Vicente-Vila do Bispo there is evidence of an even later secondary dolomitization related to the regional fault complex. Calcário dolomítico com nódulos de silex da praia de Belixe (Belixe beach dolomitic-limestone with silex nodules) (50-55m) - Ascribed to Lower or Middle Carixian on the basis of Platypleuroceras sp., Metaderoceras sp. nov. and M. gr. Venarense. Calcário cristalino compacto com Protogrammoceras, Fuciniceras e ? Argutarpites de Belixe (Belixe compact crystalline limestone with Protogrammoceras, Fuciniceras and ? Argutarpites) (30m) - Ascribed to Lower Domerian. Middle and Upper Domerian are indicated but by a single specimen of ? Argutarpites. Calcários margosos e margas com Dactylioceras semicelatum e Harpoceratídeos de Armação Nova (Armação Nova marly limestones and marls with D. semicelatum and Harpoceratidae) (25m) -Ascribed to Lower Toarcian. Middle and Upper Toarcian formations are not known in the Algarve. Dogger Calcários oolíticos, c. corálicos, c. pisolíticos, c. calciclásticos, c. dolomíticos e dolomitos de Almadena (Almadena oolitic-limestones, coral-reef-limestones, pisolite-limestones, limeclastic-limestones, dolomitic-limestones and dolomite-rocks) (more than 50 metres), with lagoonal facies. Ascribed to Aalenian-Bathonian-? Callovian. Margas acinzentadas e calcários detríticos com Zoophycos da praia de Mareta (Mareta beach greyish marls and detritical limestones with Zoophycos) (40m) - Pelagic transreef facies with Upper Bajocian and Bathonian ammonites. Calcários margosos e margas da praia de Mareta (Mareta beach pelagic marly-limestones and marls) (110m) - Ascribed to the Callovian on its ammonites. Malm Near Cabo S. Vicente and Sagres the first Upper Jurassic level consists of a yellowish-brown nodular, compact, locally phosphated and ferruginous, sometimes conglomeratic, marly limestone (0,35-1,50m) containing a rich macrofauna, which includes: 1) Callovian forms unknown at Lower Oxfordian; 2) Upper Callovian forms that still survived in Lower and Middle Oxfordian; 3) Lower Oxfordian forms (Mariae and Cordatum Zones); 4) Lower and Middle Oxfordian forms (Mariae to Plicatilis Zone); 5) Middle Oxfordian forms (plicatilis Zone), and some ones appearing in Middle Oxfordian. This condensed deposit is therefore dated from Middle Oxfordian (Plicatilis Zone). The other Upper Jurassic lithostratigraphical units were also mapped but their detailed study is not presented in this work. Correlations between lithostratigraphical and chronostratigraphical scales from P. Choffat, J. Pratsch, C. Palain and from the author are stated. Further correlations are attempted between zonc scales of Carixian-Lower Toarcian and Upper Bajocian-Middle Oxfordian of France, Spain (Asturias, Iberian and Betic Chains), Argel (Orania) and Portugal (northern Tagus basin and Algarve). The study of pyritous fossil assemblages common in Upper Bathonian-Lower Callovian marly levels of the praia da Mareta seems to suggest that these sediments were deposited in a bay or in an almost closed coastal re-entrance virtually without deep water circulation. Although such conditions may occur at any depth one may suppose that these ones actually correspond to an infralittoral neritic environment. The thaphocoenosis collected there are almost entirely composed of nektonic (ammonites, Belemnites) and planktonic (Bositra) faunas. The sedentary (crinoids, brachiopods) or free (sea-urchins, gastropods) epibenthonic forms are very scarce; endobenthonic forms are not known. The palaeontological study of all Nautiloids and Ammonoids of the Liassic and Dogger is presented (except Kosmoceratidae and Perisphinctaceae). Among the thirty one taxa dealt with, one is new (Metaderoceras sp. nov.) and the great majority of the others has been identified for the first time in Algarve. Some others have never been reported before in Portuguese formations. The evolution, during Jurassic times, of the sedimentary basins of the Portuguese plate margin is described. The absence of Cephalopods in the very extensive marly and dolomitic limestones, partly marine, suggests that, during Lower Liassic, palaeogeography underwent no great changes. Dolomitic-limestone with silex nodules from Cabo S. Vicente contain the first ammonites recorded at the base of the Middle Liassic. This facies, although very common in Tethys, is unknown north of the Tagus. The faunal assemblage has a mediterranean to submediterranean character. Comparisons between faunal assemblage" from Algarve with the ones known north of the Tagus show that communications between Boreal Europe and Tethys, virtually non-existent during Lower and Middle Carixian, became very easy during Lower Domerian. In earlier Pliensbachian times two distinct seas were adjacent to the Iberian plate. One, an epicontinental sea with a tethyan fauna, extended southwards from the Meseta margin. Another, was a boreal sea; during its transgressive episodes boreal faunas attained into the basin north of the Tagus. During Middle Carixian and Lower Domerian, owing to simultaneous transgressions, these two seas joined together allowing faunal exchanges along the epicontinental areas which limited the emerging hercynian chains belts. During Liassic, the Algarve belonged undoubtedly to the tethyan submediterranean province. The area north of the Tagus, on the contrary, was a complex realm where subboreal and tethyan affinities alternatively prevailed. In the Algarve the first Middle Jurassic deposits do frequently show lateral thickness reductions as well as unconformities contemporaneous with other generalized disturbances on the sedimentation processes in other parts of Europe. By this time, near Sagres, a barrier reef developed separating lagoonal or ante-reef facies from the transreef pelagic zone. The presence of tethyan fauna, the abundance of Phylloceratidae and the absence of boreal forms allow us to consider the Algarve basin as a submediterranean province. The presence of Callovian pelagic fossiliferous formations in the Loulé area shows that during Middle Jurassic the marl-limestone transreef sedimentation was not confined to the western Algarve. They would extend eastwards where they only can be seen in the core of some anticlines. This is due to the progressive sinking of the meso-cenozoic formations as we proceed towards the South of the Sagres-Algoz-Querença flexure. In the whole of the Peninsule, and as for the Middle Callovian, an important regression can be clearly recognized on the evidence of an erosion surface which strikes obliquely the Middle and Upper Callovian strata. The geographic boundaries of the different faunal provinces are not changed by the presence of many Kosmoceratidae in the phosphate nodules since they are but a minority in comparison with the tethyan forms. An abstract model can be constructed showing that in Western Europe the Kosmoceratidae may have migrated South and westwards through a channel of the sea that linked Paris basin to Poitou and Aquitaine. By migrating between the Iberian meseta and the Armorican massif this fauna reached northern Tagus basin at the beginning of Upper Callovian (Athleta Zone); this south and southwest bound migration would have proceeded, allowing such forms to reach Algarve basin only in latest Callovian times (Lamberti Zone). This migration means that during Middle Jurassic a widely spread North Atlantic sea would exist, flooding the western part of Portugal up to the Poitou.
Resumo:
The Middle and Upper Jurassique limestones investigated were sub-divided into nine microfacies (MF) types. The firsts four represent Bathonian sediments with shallow water characteristics typical for carbonate platforms. They are comparable with Wilson's facies zones 6 to 8. Reef and reef debris, near-shore clastic-dominated limestones are not present. These MF-types are reiterated several times without cyclicity. The vertical development of the differentiated facies units indicates a close interfingering. The microfacies data are typical of inter to shallow subtidal environments; both authigenous quartz and low faunal and floral diversity of several layers point to temporary restricted conditions. The occurrence of Dictyoconus cayeuxi LUCAS and Callovian ammonites from the above lying strata argue for a Bathonian age. The MF-types 5-9 (Oxfordian-Kimmeridgian) show completely different sedimentation conditions. Fully marine nearshore recifal limestones alternate with pelagic sediments formed at deeper shelf areas. The pelagic micritic limestones of Oxfordian age are characterized by allodapic intercalations whereas the Oxfordian/Kimmeridgian limestones with tuberolithic fabrics often show intensive silifications. Only initial patch reef growth-stages were reached during the development of the Oxfordian and Kimmeridgian shallow water limestones.
Resumo:
A malária é reconhecida como uma das principais forças selectivas a actuar na história recente no genoma humano. Inúmeros polimorfismos genéticos têm sido descritos como protectores contra a gravidade da malária, como o alelo HbS (designado de traço falciforme) e o alelo G6PD A- (associado à deficiência de G6PD). Mais recentemente, também a deficiência de PK foi associada com a protecção contra a malária. Evidências desta associação foram obtidas em estudos com modelos de roedor e estudos in vitro utilizando GV humanos deficientes em PK. Até à data, não foram obtidos dados em populações humanas que revelem esta associação: ainda não foi identificada uma variante de PK com uma prevalência elevada em regiões endémicas de malária e não foram identificadas marcas de selecção na região do gene que codifica para a PK (gene PKLR). Além disso, os mecanismos subjacentes à protecção contra a malária por deficiências enzimáticas dos GV não estão bem esclarecidos. Assim, os objectivos do presente estudo foram: investigar os polimorfismos genéticos humanos com associação com a malária em Cabo Verde; pesquisar marcas de selecção da malária na região do gene PKLR em populações Africanas; determinar a frequência da deficiência em PK e identificar uma eventual variante da enzima que possa estar sob selecção positiva em regiões endémicas de malária; avaliar o efeito das duas deficiências enzimáticas (PK e G6PD) na invasão e maturação do parasita em culturas in vitro de Plasmodium usando GV normais e deficientes; e analisar o perfil proteómico de GV infectados e não infectados, normais e com deficiência (em PK e G6PD), bem como de parasitas isolados de GV tanto deficientes como normais. Em Cabo Verde (área epidémica), não foram identificadas marcas de selecção pela malária, através da análise dos vários polimorfismos. No entanto, quando a análise foi realizada em dois países endémicos (Angola e Moçambique), foram detectadas várias marcas de selecção: a genotipagem de microssatélites (STRs) e polimorfismos de base única (SNPs) localizados na vizinhança do gene PKLR revelou uma diferenciação consideravelmente maior entre as populações Africana e Europeia (Portuguesa), do que a diferenciação determinada aquando da utilização de marcadores genéticos neutros. Além disso, uma região genómica de maior amplitude apresentou um Desequilíbrio de Ligação (LD) significativo no grupo de malária não grave (e não no grupo de malária grave), sugerindo que a malária poderá estar a exercer pressão selectiva sobre a região do genoma humano que envolve o gene PKLR. No estudo que incidiu na determinação da prevalência da deficiência de PK no continente Africano (realizado em Moçambique), esta revelou-se elevada - 4,1% - sendo o valor mais elevado descrito até ao momento a nível mundial para esta enzimopatia. Na pesquisa de mutações que pudessem estar na causa deste fenótipo (baixa actividade de PK), foi identificada uma mutação não sinónima 829G>A (277Glu>Lys), significativamente associada à baixa actividade enzimática. Esta mutação foi também identificada em Angola, São Tomé e Príncipe e Guiné Equatorial, onde a frequência de portadores heterozigóticos foi entre 2,6 e 6,7% (valores que se encontram entre os mais elevados descritos globalmente para mutações associadas à deficiência em PK). Não foi possível concluir acerca da associação entre a deficiência de PK e o grau de severidade da malária e da associação entre o alelo 829A e a mesma, devido ao baixo número de amostras. Os resultados dos ensaios de invasão/maturação do parasita sugeriram que, nos GV com deficiência de PK ou G6PD, a invasão (onde está envolvida a membrana do GV hospedeiro e o complexo apical do parasita) é mais relevante para a eventual protecção contra a malária do que a maturação. Os resultados da análise proteómica revelaram respostas diferentes por parte do parasita nas duas condições de crescimento (GV com deficiência de PK e GV com deficiência de G6PD). Esta resposta parece ser proporcional à gravidade da deficiência enzimática. Nos parasitas que cresceram em GV deficientes em G6PD (provenientes de um indivíduo assintomático), a principal alteração observada (relativamente às condições normais) foi o aumento do número de proteínas de choque térmico e chaperones, mostrando que os parasitas responderam às condições de stress oxidativo, aumentando a expressão de moléculas de protecção. Nos parasitas que cresceram em condições de deficit de PK (GV de indivíduo com crises hemolíticas regulares, dependente de transfusões sanguíneas), houve alteração da expressão de um maior número de proteínas (relativamente ao observado em condições normais), em que a maioria apresentou uma repressão da expressão. Os processos biológicos mais representados nesta resposta do parasita foram a digestão da hemoglobina e a troca de proteínas entre hospedeiro e parasita/remodelação da superfície do GV. Além disso, uma elevada percentagem destas proteínas com expressão alterada está relacionada com as fendas de Maurer, que desempenham um papel importante na patologia da infecção malárica. É colocada a hipótese de que a protecção contra a malária em GV deficientes em PK está relacionada com o processo de remodelação da membrana dos GV pelo parasita, o que pode condicionar a invasão por novos parasitas e a própria virulência da malária. Os resultados da análise do proteoma dos GV contribuirão para confirmar esta hipótese.
Resumo:
All life forms need to monitor carbon and energy availability to survive and this is especially true for plants which must integrate unavoidable environmental conditions with metabolism for cellular homeostasis maintenance. Sugars, in the heart of metabolism, are now recognized as crucial signaling molecules that translate those conditions. One such signal is trehalose 6- phosphate (T6P), a phosphorylated dimer of glucose molecules which levels correlate well with those of sucrose (Suc). Central integrators of stress and energy regulation include the conserved plant Snf1-related kinase1 (SnRK1) which respond to low cellular energy levels by up-regulating energy conserving and catabolic metabolism and down-regulating energy consuming processes. In 2009 T6P was shown to inhibit SnRK1. The in vitro inhibition of SnRK1 by T6P was confirmed in vivo through the observation that genes normally induced by SnRK1 were repressed by T6P and vice-versa, promoting growth processes. These observations provided a model for the regulation of growth by sugar.(...)