Magmatic fluids in the Breccia-hosted epithermal Au-Ag deposit of Rosia Montana, Romania

The breccia-hosted epithermal Au-Ag deposit of Rosia Montana is located 7 kin northeast of Abrud, in the northern part of the South Apuseni Mountains, Romania. Estimated total reserves of 214.91 million metric toils (Mt) of ore at 1.46 g/t An and 6.9 g/t Ag (10.1 Moz of An and 47.6 Moz of Ag) make Rosia Montana one of the largest gold deposits in Europe. At this location, Miocene calc-alkaline magmatic and hydrothermal activity was associated with local extensional tectonics within a strike-slip regime related to the indentation of the Adriatic microplate into the European plate during the Carpathian orogenesis. The host rocks of the magmatic complex consist of pre-Mesozoic metamorphosed continental crust covered by Cretaceous turbiditic sediment (flysch). Magmatic activity at Rosia Montana and its surroundings occurred in several pulses and lasted about 7 m.y, Rosia Montana is a breccia-hosted epithermal system related to strong phreatomagmatic activity due to the shallow emplacement of the Montana dacite. The Montana dacite intruded Miocene volcaniclastic material (volcaniclastic breccias) and crops out at Cetate and Carnic Hills. Current mining is focused primarily on the Cetate open pit, which was mapped in detail, leading to the recognition of three distinct breccia bodies: the dacite breccia with a dominantly hydrothermal matrix, the gray polymict breccia with a greater proportion of sand-sized matrix support, and the black polymict breccia, which reached to the surface, contains carbonized tree trunks and has a dominantly barren elastic matrix. The hydrothermal alteration is pervasive. Adularia alteration with a phyllic overprint is ubiquitous; silicification and argillic alteration occur locally. Mineralization consists of quartz, adularia, carbonates (commonly Mn-rich), pyrite, Fe-poor sphalerite, galena, chalcopyrite, tetrahedrite, and native gold and occurs as disseminations, as well as in veins and filling vugs within the Montana dacite and the different breccias. The age of mineralization (12.85 +/- 0.07 Ma) was determined by Ar-40- Ar-39 dating on hydrothermal adularia crystals from vugs in the dacite breccia in the Cetate open pit. Microthermometric measurements of fluid inclusions in quartz phenocrysts from the Montana dacite revealed two fluid types that are absent from the hydrothermal breccia and must have been trapped at depth prior to dacite dome emplacement: brine inclusions (32-55 -wt % NaCl equiv, homogenizing at T-h > 460 degrees C) and intermediate density fluids (4.9-15.6 wt % NaCl equiv, T, between 345 degrees-430 degrees C). Secondary aqueous fluid inclusion assemblages in the phenocrysts have salinities of 0.2 to 2.2 wt percent NaCl equiv and T-h of 200 degrees to 280 degrees C. Fluid inclusion assemblages in hydrothermal quartz from breccias and veins have salinities of 0.2 to 3.4 wt percent NaCl equiv and T-h, from 200 degrees to 270 degrees C. The oxygen isotope composition of several zones of an ore-related epithermal quartz crystal indicate a very constant delta O-18 of 4.5 to 5.0 per mil for the mineralizing fluid, despite significant salinity and temperature variation over time. Following microthermometry, selected fluid inclusion assemblages were analyzed by laser ablation-inductively coupled-plasma mass spectrometry (LA-ICMS). Despite systematic differences in salinity between phenocryst-hosted fluids trapped at depth and fluids from quartz in the epithermal breccias, all fluids have overlapping major and trace cation ratios, including identical Na/K/Rb/Sr/Cs/Ba. Consistent with the constant near-magmatic oxygen isotope composition of the hydrothermal fluids, these data strongly indicate a common magmatic component of these chemically conservative solutes in all fluids. Cu, Pb, Zn, and Mn show variations in concentration relative to the relatively non-reactive alkalis, reflecting the precipitation of sulfide minerals together with An in the epithermal breccia, and possibly of Cu in an inferred subjacent porphyry environment. The magmatic-hydrothermal processes responsible for epithermal Au-Ag mineralization at Rosia Montana are, however, not directly related to the formation of the spatially associated porphyry Cu-Au deposit of Rosia Poieni, which occurred lout 3 m.y. later.

Geology of the Cerro-Quema Au-Cu deposit (Azuero Peninsula, Panama)

The Cerro Quema district, located on the Azuero Peninsula, Panama, is part of a large regional hydrothermal system controlled by regional faults striking broadly E-W, developed within the Río Quema Formation. This formation is composed of volcanic, sedimentary and volcano-sedimentary rocks indicating a submarine depositional environment, corresponding to the fore-arc basin of a CretaceousPaleogene volcanic arc. The structures observed in the area and their tectono-stratigraphic relationship with the surrounding formations suggest a compressive and/or transpressive tectonic regime, at least during Late CretaceousOligocene times. The igneous rocks of the Río Quema Formation plot within the calc-alkaline field with trace and rare earth element (REE) patterns of volcanic arc affinity. This volcanic arc developed on the Caribbean large igneous province during subduction of the Farallon Plate. Mineralization consists of disseminations of pyrite and enargite as well as a stockwork of pyrite and barite with minor sphalerite, galena and chalcopyrite, hosted by a subaqueous dacitic lava dome of the Río Quema Formation. Gold is present as submicroscopic grains and associated with pyrite as invisible gold. A hydrothermal alteration pattern with a core of advanced argillic alteration (vuggy silica with alunite, dickite, pyrite and enargite) and an outer zone of argillic alteration (kaolinite, smectite and illite) has been observed. Supergene oxidation overprinted the hydrothermal alteration resulting in a thick cap of residual silica and iron oxides. The ore minerals, the alteration pattern and the tectono-volcanic environment of Cerro Quema are consistent with a high sulfidation epithermal system developed in the Azuero peninsula during pre-Oligocene times.

Mineral zoning and geochemistry of epithermal polymetallic Zn-Pb-Ag-Cu-Bi mineralization at Cerro de Pasco, Peru

The large Cerro de Pasco Cordilleran base metal deposit in central Peru is located on the eastern margin of a middle Miocene diatreme-dome complex and comprises two mineralization stages. The first stage consists of a large pyrite-quartz body replacing Lower Mesozoic Pucara carbonate rocks and, to a lesser extent, diatreme breccia. This body is composed of pyrite with pyrrhotite inclusions, quartz, and black and red chalcedony (containing hypogene hematite). At the contact with the pyrite-quartz body, the diatreme breccia is altered to pyrite-quartz-sericite-pyrite. This body was, in part, replaced by pipelike pyrrhotite bodies zoned outward to carbonate-replacement Zn-Pb ores hearing Fe-rich sphalerite (up to 24 mol % Fes). The second mineralization stage is partly superimposed on the first and consists of zoned east-west-trending Cu-Ag-(Au-Zn-Pb) enargite-pyrite veins hosted in the diatreme breccia in the western part of the deposit and well-zoned Zn-Pb-(Bi-Ag-Cu) carbonate-replacement orebodies; in both cases, sphalerite is Fe poor and the inner parts of the orebodies show typically advanced argillic alteration assemblages, including aluminum phosphate Sulfate (APS) minerals. The zoned enargite-pyrite veins display mineral zoning, from a core of enargite-pyrite +/- alunite with traces of Au, through an intermediate zone of tennantite, chalcopyrite, and Bi minerals to a poorly developed Outer zone hearing sphalerite-galena +/- kaolinite. The carbonate-hosted replacement ores are controlled along N 35 degrees E, N 90 degrees E, N 120 degrees E, and N 170 degrees E faults. They form well-zoned upward-flaring pipelike orebodies with a core of famatinite-pyrite and alunite, an intermediate zone with tetrahedrite-pyrite, chalcopyrite, matildite, cuprobismutite, emplectite, and other Bi minerals accompanied by APS minerals, kaolinite, and dickite, and an outer zone composed of Fe-poor sphalerite (in the range of 0.05-3.5 mol % Fes) and galena. The outermost zone consists of hematite, magnetite, and Fe-Mn-Zn-Ca-Mg carbonates. Most of the second-stage carbonate-replacement orebodies plunge between 25 degrees and 60 degrees to the west, suggesting that the hydrothermal fluids ascended from deeper levels and that no lateral feeding from the veins to the carbonate-replacement orebodies took place. In the Venencocha and Santa Rosa areas, located 2.5 km northwest of the Cerro de Pasco open pit and in the southern part of the deposit, respectively, advanced argillic altered dacitic domes and oxidized veins with advanced argillic alteration halos occur. The latter veins are possibly the oxidized equivalent of the second-stage enargite-pyrite veins located in the western part of the deposit. The alteration assemblage quartz-muscovite-pyrite associated with the pyrite-quartz body suggests that the first stage precipitated at slightly, acidic fin. The sulfide mineral assemblages define an evolutionary path close to the pyrite-pyrrhotite boundary and are characteristic of low-sulfidation states; they suggest that the oxidizing slightly acidic hydrothermal fluid was buffered by phyllite, shale, and carbonate host rock. However, the presence in the pyrite-quartz body of hematite within quartz suggests that, locally, the fluids were less buffered by the host rock. The mineral assemblages of the second mineralization stage are characteristic of high- to intermediate-sulfidation states. High-sulfidation states and oxidizing conditions were achieved and maintained in the cores of the second-stage orebodies, even in those replacing carbonate rocks. The observation that, in places, second-stage mineral assemblages are found in the inner and outer zones is explained in terms of the hydrothermal fluid advancing and waning. Microthermometric data from fluid inclusions in quartz indicate that the different ores of the first mineralization stage formed at similar temperatures and moderate salinities (200 degrees-275 degrees C and 0.2-6.8 wt % NaCl equiv in the pyrite-quartz body; 192 degrees-250 degrees C and 1.1-4.3 wt % NaCl equiv in the pyrrhotite bodies; and 183 degrees-212 degrees C and 3.2-4.0 wt % NaCl equiv in the Zn-Pb ores). These values are similar to those obtained for fluid inclusions in quartz and sphalerite from the second-stage ores (187 degrees-293 degrees C and 0.2-5.2 wt % NaCl equiv in the enargite-pyrite veins: 178 degrees-265 degrees C and 0.2-7.5 wt % NaCl equiv in quartz of carbonate-replacement orebodies; 168 degrees-999 degrees C and 3-11.8 wt % NaCl equiv in sphalerite of carbonate-replacement orebodies; and 245 degrees-261 degrees C and 3.2-7.7 wt % NaCl equiv in quartz from Venencocha). Oxygen and hydrogen isotope compositions oil kaolinite from carbonate-replacement orebodies (delta(18)O = 5.3-11.5%o, delta D = -82 to -114%o) and on alunite from the Venencocha and Santa Rosa areas (delta(18)O = 1.9-6.9%o, delta D = -56 to -73%o). Oxygen isotope compositions of quartz from the first and second stages have 6180 values from 9.1 to 1.7.8 per mil. Calculated fluids in equilibrium with kaolinite have delta(18)O values of 2.0 to 8.2 and delta D values of -69 to -97 per mil; values in equilibrium with alunite are -1.4 to -6.4 and -62 to -79 per mil. Sulfur isotope compositions of sulfides from both stages have a narrow range of delta(34)S values, between -3.7 and +4.2 per mil; values for sulfates from the second stage are between 4.2 and 31.2 per mil. These results define two mixing trends for the ore-forming fluids. The first trend reflects mixing between a moderately saline (similar to 10 wt % NaCl equiv) magmatic end member that had degassed (as indicated by the low delta D values) and meteoric water. The second mixing indicates condensation of magmatic vapor with HCl and SO(2) into meteoric water, which formed alunite. The hydrothermal system at Cerro de Pasco was emplaced at a shallow depth (similar to 500 m) in the epithermal and upper part of a porphyry environment. The similar temperatures and salinities obtained for the first stage and second stages, together with the stable isotope data, indicate that both stages are linked and represent successive stages of epithermal polymetallic mineralization in the upper part of a porphyry system.

Structural, metamorphic and geochronological relations between the Zanskar Shear Zone and the Miyar Shear Zone (NW Indian Himalaya): Evidence for two distinct tectonic structures and implications for the evolution of the High Himalayan Crystalline of Zanskar

The geologic structures and metamorphic zonation of the northwestern Indian Himalaya contrast significantly with those in the central and eastern parts of the range, where the high-grade metamorphic rocks of the High Himalayan Crystalline (HHC) thrust southward over the weakly metamorphosed sediments of the Lesser Himalaya along the Main Central Thrust (MCT). Indeed, the hanging wall of the MCT in the NW Himalaya mainly consists of the greenschist facies metasediments of the Chamba zone, whereas HHC high-grade rocks are exposed more internally in the range as a large-scale dome called the Gianbul dome. This Gianbul dome is bounded by two oppositely directed shear zones, the NE-dipping Zanskar Shear Zone (ZSZ) on the northern flank and the SW-dipping Miyar Shear Zone (MSZ) on the southern limb. Current models for the emplacement of the HHC in NW India as a dome structure differ mainly in terms of the roles played by both the ZSZ and the MSZ during the tectonothermal evolution of the HHC. In both the channel flow model and wedge extrusion model, the ZSZ acts as a backstop normal fault along which the high-grade metamorphic rocks of the HHC of Zanskar are exhumed. In contrast, the recently proposed tectonic wedging model argues that the ZSZ and the MSZ correspond to one single detachment system that operates as a subhorizontal backthrust off of the MCT. Thus, the kinematic evolution of the two shear zones, the ZSZ and the MSZ, and their structural, metamorphic and chronological relations appear to be diagnostic features for discriminating the different models. In this paper, structural, metamorphic and geochronological data demonstrate that the MSZ and the ZSZ experienced two distinct kinematic evolutions. As such, the data presented in this paper rule out the hypothesis that the MSZ and the ZSZ constitute one single detachment system, as postulated by the tectonic wedging model. Structural, metamorphic and geochronological data are used to present an alternative tectonic model for the large-scale doming in the NW Indian Himalaya involving early NE-directed tectonics, weakness in the upper crust, reduced erosion at the orogenic front and rapid exhumation along both the ZSZ and the MSZ.

Secretory IgA: an actor of the interplay between the commensal flora and the intestinal immune system?

In the gastro-intestinal tract,Peyers patches have been describedas a major inductive site for mucosalsecretory IgA (SIgA) responses directedagainst pathogens. The classicalview is that SIgAserves as the firstline of defense against microorganismsby agglutining potential invadersand faciliting their clearance byperistaltic and mucociliary movements,a mechanism called immuneexclusion. Our laboratory has shownthat SIgA is not only able to be"retrotransported" into Peyers patchesvia the associated M cells, but also todeliver sizeable cargos in the form ofSIgA-based immune complexes, resultingin the onset of non-inflammatorytype of responses. Such a novelfunction raises the question of thepossible role of mucosal SIgA in theinterplay with commensal bacteriaand the contribution of the antibody inbacterial homeostasis. To address thisquestion, Lactobacillus rhamnosus(LPR) was administered into a mouseligated loop comprising a Peyerspatch, in association or not with SIgA.The fate of fluorescently labelled bacteriawas followed by laser scanningconfocal microscopy at different incubationtimes. After 2 hours of incubationin the loop, LPR bacteria arefound more abundantly in thesubepithelial dome (SED) regionwhen they are coated with SIgA thanLPR administered alone despite theyare absent from neighboring villi.Herein, it is shown that this mechanismof entry involves M cells inPeyers pathes. After their sampling byM cells, bacteria are engulfed by thedendritic cells of the subjacent SEDregion. Interestingly, LPR bacteriaare found coated by the endogenousnatural SIgA present in mice intestinalsecretions, confirming the requirementof SIgA for this type of entry.The subsequent effect on the maturationof dendritic cells after interactionwith LPR was investigated in vitroin presence or not of SIgA by measuringthe expression of CD40, CD80and CD86 surface markers with flowcytometry analyses. Results show thatDCs respond in the same way in presenceof SIgA than with LPR bacteriaalone, indicating that SIgA does notmodulate the interaction betweenDCs and bacteria in this context. Thiswork gives new evidences about theinvolvement of SIgA in the mechanismby which the intestinal immunesystem permanently checks the contentof the intestine.

Predicting chick body mass by artificial intelligence-based models

The objective of this work was to develop, validate, and compare 190 artificial intelligence-based models for predicting the body mass of chicks from 2 to 21 days of age subjected to different duration and intensities of thermal challenge. The experiment was conducted inside four climate-controlled wind tunnels using 210 chicks. A database containing 840 datasets (from 2 to 21-day-old chicks) - with the variables dry-bulb air temperature, duration of thermal stress (days), chick age (days), and the daily body mass of chicks - was used for network training, validation, and tests of models based on artificial neural networks (ANNs) and neuro-fuzzy networks (NFNs). The ANNs were most accurate in predicting the body mass of chicks from 2 to 21 days of age after they were subjected to the input variables, and they showed an R² of 0.9993 and a standard error of 4.62 g. The ANNs enable the simulation of different scenarios, which can assist in managerial decision-making, and they can be embedded in the heating control systems.

Eficiência de filtros de areia pressurizados na remoção de diferentes tamanhos de partículas da água de irrigação

Resumo:O objetivo deste trabalho foi avaliar a eficiência de filtros de areia com diferentes granulometrias na remoção de diferentes tamanhos de partículas da água de irrigação, bem como a perda de pressão em função da taxa de filtração e da granulometria de areia do leito filtrante. Os ensaios foram realizados com três filtros de um mesmo modelo comercial, testados com diferentes combinações de granulometrias de areia (areia fina, 0,55 mm; média, 0,77 mm; e grossa, 1,04 mm de diâmetro) e taxas de filtração (20, 40, 60 e 75 m3m-2 h-1), e repetidos em três ciclos de filtração de 4 horas (C1, C2 e C3, realizados em 3 dias consecutivos). O filtro de areia avaliado é efetivo na remoção de partículas a partir do tamanho de areia fina (>60 μm). Nesta faixa de remoção de partículas, a influência da taxa de filtração aumenta com a diminuição do tamanho de partícula na água. O aumento na taxa de filtração, associado à diminuição da granulometria de areia, aumenta a eficiência de remoção, mas acentua a perda de pressão com o tempo, o que diminui a remoção das partículas menores ao longo dos ciclos de filtração.

Peripheral exudative hemorrhagic chorioretinopathy: polypoidal choroidal vasculopathy and hemodynamic modifications.

PURPOSE: To investigate choroidal vascular abnormalities in peripheral exudative hemorrhagic chorioretinopathy, using dynamic ultrawide-field fluorescein angiography (FA) and indocyanine green angiography (ICGA).¦DESIGN: Prospective observational case series.¦METHODS: This institutional study comprised a consecutive series of 40 patients (48 eyes) with peripheral exudative hemorrhagic chorioretinopathy. Choroidal vascular abnormalities were assessed with dynamic ultrawide-field (150-degree) FA and ICGA, using the Staurenghi 230 SLO Retina Lens and the Heidelberg scanning laser ophthalmoscope. The main outcome measures were morphologic descriptions of structural vascular abnormalities and choroidal hemodynamics (comparison with 30 normal eyes).¦RESULTS: The peripheral mass lesions were highly exudative and hemorrhagic, and usually associated with a pigment epithelium detachment. FA revealed nonspecific alterations corresponding to the visible fundoscopic changes (window defects, blockage, staining), but no neovascular membrane. However, despite frequent masking, ICGA showed hyperfluorescent polyp-like structures in the choroid of the lesion area in 33 eyes (69%) and an abnormal choroidal vascular network in 24 eyes (50%). The abnormal choroidal vascular network filled in the arterial or early venous phase, while the polyp-like structures filled some seconds later. Optical coherence tomography revealed the typical dome-shaped elevation of the pigment epithelium over the vascular polyps. Peripheral choriocapillaris closure was observed as well as dilated shunting vessels.¦CONCLUSION: Peripheral exudative hemorrhagic chorioretinopathy shares many characteristics (polyp-like choroidal telangiectases, abnormal choroidal vascular networks, exudative and hemorrhagic presentation) with polypoidal choroidal vasculopathy. Clarification of the precise role of these abnormalities requires further studies.

Événements et déformations tardi-métamorphiques dans le segment Ossola-Ticino (Val Vigezzo-Centovalli, Italie-Suisse)

RESUME: Une zone tectonique large et complexe, connue sous le nom de ligne des Centovalli, traverse le secteur des Alpes Centrales compris entre Domodossola et Locarno. Cette région, formée par le Val Vigezzo et la vallée des Centovalli, constitue la terminaison méridionale du dôme Lepontin et représente une portion de la zone des racines des nappes alpines. Elle fait partie d’une grande et complexe zone de cisaillement, en partie associée à des phénomènes hydrothermaux d’âge alpin (<20 Ma), qui comprend le système tectonique Insubrien et celui du Simplon. Le Val Vigezzo et les Centovalli constituent un vrai carrefour entre les principaux accidents tectoniques des Alpes ainsi qu'une zone de juxtaposition du socle Sudalpin avec la zone des racines de l’Austroalpin et du Pennique. Les phases de déformation et les structures géologiques qui peuvent être étudiées s'étalent sur une période comprise entre environ 35 Ma et l'actuel. L’étude détaillée de terrain a mis en évidence la présence de nombreuses roches et structures de déformation de type ductile et cassant tels que des mylonites, des cataclasites, des pseudotachylites, des kakirites, des failles minéralisées, des gouges de faille et des plis. Sur le terrain on a pu distinguer au moins quatre générations de plis liés aux différentes phases de déformation. Le nombre et la complexité de ces structures indiquent une histoire très compliquée, selon plusieurs étapes distinctes, parfois liées, voire même superposées. Une partie de ces structures de déformation affectent aussi les dépôts sédimentaires d’âge quaternaire, notamment des limons et des sables lacustres. Ces sédiments constituent les restes d'un bassin lacustre attribué à l'époque interglaciaire Riss/Würm (éemien, 67.000-120.000 ans) et ils affleurent dans la partie centrale de la zone étudiée, à l'Est de la plaine de Santa Maria Maggiore. Ces sédiments montrent en leur sein toute une série de structures de déformation tels que des plans de faille inverses, des structures conjuguées de raccourcissement et des véritables plis. Ces failles et ces plis représenteraient les évidences de surface d’une déformation probablement active en époque quaternaire. Une autre formation rocheuse a retenu tout notre attention; il s'agit d'un corps de brèches péridotitiques monogéniques qui affleure en discontinuité le long du versant méridional et le long du fond de la vallée Vigezzo sur environ 20 km. Ces brèches se posent indifféremment sur le socle (unités Finero, Orselina) ou sur les sédiments lacustres. Elles sont traversées par des plans de failles qui développent des véritables stries de faille et des gouges de faille; l’orientation de ces plans est la même que celle affectant les failles à gouges du socle. La genèse de cette brèche est liée à l'altération et au modelage glacier (rock-glaciers) d'une brèche tectonique originelle qui borde la partie externe du Corps de Finero. Les structures de déformation de cette brèche, pareillement à celles des sédiments lacustres, ont été considérées comme les évidences de surface d'une tectonique quaternaire active dans la région. La dernière phase de déformation cassante qui affecte cette région peut donc être considérée comme active en époque quaternaire. Une vue d’ensemble de la région étudiée nous permet de reconnaître à l’échelle régionale une zone de cisaillement complexe orientée E-W, parallèlement à l’axe de la vallée Centovalli-Val Vigezzo. Les données de terrain, indiquent que cette zone de cisaillement débute sous conditions ductiles et évolue en plusieurs étapes jusqu’à des conditions de failles cassantes de surface. La reconstruction de l'évolution géodynamique de la région a permis de définir trois étapes distinctes qui marquent le passage, de ce secteur de socle cristallin, de conditions P-T profondes à des conditions de surface. Dans ce contexte, on a reconnu trois phases principales de déformation à l’échelle régionale qui caractérisent ces trois étapes. La phase la plus ancienne est constituée par des mylonites en faciès amphibolite, associées à des mouvements de cisaillement dextre, qui sont ensuite remplacés par des mylonites en faciès schistes verts et des plis rétrovergentes liés au rétrocharriage des nappes alpines. Une deuxième étape est identifiée par le développement d’une phase hydrothermale liée à un système de failles extensives et décrochantes dextres à direction principale E-W, NE-SW et NW-SE. Leur caractérisation minéralogique a permis la mise en évidence des phases cristallines de néoformation liées à cet événement constituées par : K-feldspath (microcline), chlorites (Fe+Mg), épidotes, prehnite, zéolites (laumontite), sphène, calcite. Dans ce contexte, pour obtenir une meilleure caractérisation de cet événement hydrothermal on a utilisé des géothermomètres sur chlorites, sensible aussi à la pression et a la a(H2O), qui ont donné des valeurs descendantes comprises entre 450-200°C. Les derniers mouvements sont mis en évidence par le développement d’une série de plans majeurs de failles à gouge, qui forment une structure en sigmoïdes d’épaisseur kilométrique reconnaissable à l’échelle de la vallée et caractérisée par des mouvements transpressifs avec une composante décrochante dextre toujours importante. Cette phase de déformation forme un système conjugué de failles avec direction moyenne E-W qui coupent la zone des racines des nappes alpines, la zone du Canavese et le corps ultramafique de Finero. Ce système se déroule de manière subparallèle à l'axe de la vallée le long de plusieurs dizaines de kilomètres. Une analyse complète et détaillée des gouges de faille par XRD a montré que la fraction argileuse (<2 µm) de ces gouges contient une partie de néoformation très importante constituée par, des illites, des chlorites et des interstratifiés de type illite/smectite ou chlorite/smectite. Des datations avec méthode K-Ar sur ces illites ont donné des valeurs comprises entre 12 et 4 Ma qui représentent l'âge de cette dernière déformation cassante. L'application de la méthode de la cristallinité de l'illite (C.I.) a permis d'évaluer les conditions thermiques qui caractérisent le déroulement de cette dernière phase tectonique qui se produit sous conditions de température caractéristiques de l'anchizone et de la diagenèse. L'ensemble des structures de déformation qu'on vient de décrire s'insère parfaitement dans le contexte de convergence oblique entre la plaque adriatique et celle européenne qui à produit l'orogène alpin. On peut considérer les structures tectoniques du Val Vigezzo-Centovalli comme l'expression d'une zone majeure de cisaillement "Simplo-Insubrienne". L'empilement structural et les structures tectoniques affleurantes dans la région sont le résultat de l'interaction entre un régime tectonique transpressif et un régime transtensif. Ces deux champs de tension sont antagonistes entre eux mais sont reliés, de toute façon, à une seule phase décrochante dextre principale, due à une convergence oblique entre deux plaques. À l'échelle de l'évolution géodynamique on peut distinguer différentes étapes au cours desquelles les structures de ces deux régimes tectoniques interagissent en manière différente. En accord avec les données géophysiques et les reconstructions paléodynamiques prises dans la littérature on considère que la ligne Rhône-Simplon-Centovalli représente l'évidence de surface de la suture majeure profonde entre la plaque Adriatique et celle Européenne. Les vitesses de soulèvement qui ont été calculées dans cette étude pour cette région des Alpes donnent une valeur moyenne de 0.8 mm/a qui est tout à fait comparable avec les données proposées par la littérature sur cette zone. La zone Val Vigezzo-Centovalli peut être donc considérée comme un carrefour géologique où se croisent différentes phases tectoniques qui représentent les évidences de surface d'une suture profonde majeure entre deux plaques dans un contexte de collision continentale. ABSTRACT: A wide and complex tectonic zone known as Centovalli line, crosses the Central Alps sector between Domodossola and Locarno. This area, formed by the Vigezzo Valley and Centovalli valley, constitutes the southernmost termination of the Lepontin dome and represents a portion of the alpine nappes root zone. It belongs to a large and complex shear-zone, partly associated with hydrothermal phenomena of alpine age (<20 My), which includes the Insubric Line and the Simplon fault zone. Vigezzo Valley and Centovalli constitute a real crossroads between the mains alpines tectonics lines as well as a zone of juxtaposition of the Southalpine basement with the Austroalpin and Pennique root zone. The deformation phases and the geological structures that can be studied between approximately 35 My and the present. The detailed field study showed the presence of many brittle and ductile deformation structures and fault rocks such as mylonites, cataclasites, pseudotachylites, kakirites, mineralized faults, fault gouges and folds. In the field we could distinguish at least four folds generations related to the various deformation phases. The number and the complexity of these structures indicate a very complicated history, comprising several different stages, that sometimes are related and even superimposed. Part of these deformation structures affect also the sedimentary deposits of quaternary age, in particular the silts and sands lake deposit. These sediments constitute the remainders of a lake basin ascribed to the interglacial Riss/Würm (Eemien, 67.000-120.000 years) and outcroping in the central part of the studied area, in the Eastern part of Santa Maria Maggiore plain. These sediments show a whole series of deformation structures such as inverse fault planes, combined shortening structures and true folds. These faults and folds would represent the surface evidence of a probably active tectonic deformation in quaternary time. Another rock formation attracted all our attention. It is a body of monogenic peridotite breccia which outcrops in discontinuity along the southernmost slope and the bottom of the Vigezzo valley on approximately 20 km. This breccia lies indifferently on the basement (Finero and Orselina units) or on the lake sediments. They are crossed by fault planes which developed slikenside and fault gouges whose orientation is the same of the faults gouges in the alpine basement. This breccia results from the weathering and the surface modelling of an original tectonic breccia which borders the external part of Finero peridotite body. This breccia deformation structures, like those of the lake sediments, were regarded as the surface interaction of active quaternary tectonics in the area. So the last brittle deformation phases which affects this area seems to be actives in quaternary time. Theoverall picture of the studied area on a regional scale enables us to point out a complex shear-zone directed E-W, parallel to the axis of the Centovalli and Vigezzo Valley. The field analysis indicates that this shear-zone began under ductile conditions and evolved in several stages to brittle faulting under surface conditions. The analysis of the geodynamic evolution of the area allows to define three different stages which mark the transition of this alpine basement root zone, from deep P-T conditions to P-T surface conditions. In this context on regional scale three principal deformation phases, which characterize these three stages can be distinguished. The oldest phase consisted of the amphibolitie facies mylonites, associated to dextral strikeslip movements. They are then replaced by green-schists facies mylonites and backfolds related to the backthrusting of the alpines nappes. A second episode is caracterized by the development of an hydrothermal phase bound to an extensive fault and dextral strike-slip fault system, with E-W, NW-SE and SE-NW principal directionsThe principal neoformed mineral phases related to this event are: K-feldspar (microcline), chlorites (Fe+Mg), epidotes prehnite, zéolites (laumontite), sphene and calcite. In this context, to obtain a better characterization of this hydrothermal event, we have used an chlorite geothermometer, sensitive also to the pressure and has the a(H2O), which gave downward values ranging between 450-200°C. The last movements are caracterized by the development of important gouge fault plans, which form a sigmoid structure of kilometric thickness which is recognizable at the valley scale, and is characterized by transpressive movements always with a significant dextral strike-slip component. This deformation phase forms a combined faults system with an average E-W direction, which cuts trough the alpine root zone, the Canavese zone and the Finero ultramafic body. This fault system takes place subparallel to the axis of the valley over several tens of kilometers. A complete and detailed XRD analysis of the gouges fault showed that the clay fraction (<2µm) contains a very significant neo-formation of illite, chlorites and mixed layered clays such as illite/smectite or chlorite/smectite. The K-Ar datings of the illite fraction <2µm gave values ranging between 12 and 4 My and the illite fraction <0.2µm gave more recents values until to 2,4-0 My.This values represent the age of this last brittle deformation. The application of the illite crystallinity method (C.I.) allowed evaluating the thermal conditions which characterize this tectonic phase that occured under temperature conditions of the anchizone and diagenesis. The whole set of deformation structures which we just described, perfectly fit the context of oblique convergence between the Adriatic and the European plate that produced the alpine orogen. We can regard the Vigezzo valley and Centovalli tectonic structures as the expression of a major "Simplo-Insubric" shear-zone. Structural stacking and tectonic structures that outcrop in the studied area, are the result of the interaction between a transpressive and a transtensve tectonic phases. These two tension fields are antagonistic but they are also connected, in any event, with only one principal dextral strike-slip movement, caused by an oblique convergence between two plates. On the geodynamic evolution scale we can distinguish various stages during which these two tectonic structures fields interact in various ways. In agreement with the geophysical data and the paleodynamic recostructions taken in the literature we considers that the Rhone-Simplon-Centovalli line are the surface feature of the major collision between the Adriatique and the European plate at depth. The uplift speeds we calculated in this study for this Alpine area give an average value of 0.8 mm/a, which is in good agreement with the data suggested by the literature on this zone. TheVigezzo Valley and Centovalli zone can therefore be regarded as a geological crossroad where various tectonic phases are superimposed. They represent the evidences of a major and deeper suture between two plates in a continental collision context.

Molecular mechanisms of follicular associated epithelium differentiation

Les muqueuses respiratoires, genitales et digestives sont continuellement exposées aux antigènes de l?alimentation, à la flore intestinale et aux pathogènes. Cela implique une activité immunologique intense et finement régulée dans ces tissus. On admet que la modulation de ces réponses immunitaires muqueuses s?effectue dans des organes sentinels spécifiques appelés o-MALT (organized mucosal associated lymphoid tissues). Ces processus de modulation et la biologie de ces sites immuno-inducteurs sont peu connus. Ceci est pourtant d?une grande relevance si l?on veut faire un design rationnel de drogues et de vaccins muqueux. Dans l?intestin grèle, ces organes sont composés de follicules multiples et sont appelés plaques de Peyer. Ils sont constitués de follicules enrichis en cellules B comprenant ou non un centre germinatif, de regions interfolliculaires comprenant des cellules T, et d?une région en d ome riche en cellules dendritiques, cellules B naives et cellules T CD4+, surmontée par un epithelium specialisé, le FAE (epithelium associé aux follicules). Le FAE contient des cellules M spécialisées dans le transport de macromolécules et micro-organismes de la lumière intestinale au tissu lymphoide sous-jacent. Ce transport des antigènes est une condition obligatoire pour induire une réponse immunitaire. Les cellules du FAE, outre les cellules M, expriment un programme de différenciation distinct de celui des cellules associées aux villosités. Ceci est characterisé par une baisse des fonctions digestives et de défenses, et l?expression constitutive des chimiokines: CCL20 et CCL25. Le but de l?étude présentée ici est de rechercher les facteurs cellulaires et/ou moléculaire responsables de cette différenciation. Certaines études ont démontré l?importance du contact entre le compartiment mésenchymateux et l?épithelium pour la morphogenèse de ce dernier. En particulier, les molécules de la matrice extracellulaire peuvent activer des gènes clefs qui, à leur tour, vont controler l?adhésion et la differenciation cellulaire. Dans l?intestin, les cellules mésenchymateuses différencient en myofibroblastes qui participent à l?élaboration de la matrice extracellulaire. Dans cette étude, nous avons décrit les différences d?expression de molécules de la matrices sous le FAE et les villosités. Nous avons également montré une absence de myofibroblastes sous le FAE. Suite à plusieurs évidences expérimentales, certains ont proposé une influence des composés présents dans la lumière sur la différenciation et/ou la maturation des plaques de Peyer. La chimiokine CCL20, capable de recruter des cellules initiatrices de la réponse immunitaire, constitue notre seul marqueur positif de FAE. Nous avons pu montrer que la flagelline, un composé du flagelle bactérien, était capable d?induire l?expression de CCL20 in vitro et in vivo. Cet effet n?est pas limité aux cellules du FAE mais est observé sur l?ensemble de l?épithelium intestinal. Molecular mechanisms of FAE differenciation. La signalement induit par la lymphotoxine ß est critique pour l?organogenèse des plaques de Peyer, car des souris déficientes pour cette molécules ou son récepteur n?ont ni plaque de Peyer, ni la plupart des ganglions lymphatiques. Nous avons obtenus plusieurs évidences que la lymphotoxine ß était impliquée dans la régulation du gène CCL20 in vitro et in vivo.<br/><br/>Mucosal surfaces of the respiratory, genital and digestive systems are exposed to food antigens, normal bacterial flora and oral pathogens. This justifies an intense and tuned immunological activity in mucosal tissues. The modulation of immune responses in the mucosa is thought to occur in specific sentinel sites, the organized mucosa associated lymphoid tissues (o-MALT). This immune modulation and the biology of these immune-inductive sites are poorly understood but highly important and relevant in the case of drugs and vaccines design. In the small intestine, these organs (gut associated lymphoid tissue : GALT) consists of single or multiple lymphoid follicles, the so-called Peyer?s patches (PP), with typical B cell-enriched follicles and germinal centers, inter-follicular T cell areas, and a dome region enriched in dendritic cells, naive B cells, and CD4+ T cells under a specialized follicle associated epithelium (FAE). To trigger protective immunity, antigens have to cross the mucosal epithelial barrier. This is achieved by the specialized epithelial M cells of the FAE that are able to take up and transport macromolecules and microorganisms from the environment into the underlying organized lymphoid tissue. The ontogeny of M cells remains controversial: some data are in favor of a distinct cell lineage, while others provide evidence for the conversion of differentiated enterocytes into M cells. In this study we mapped the proliferative, M cells and apoptotic compartments along the FAE. Enterocytes acquire transient M cell features as they leave the crypt and regain enterocyte properties as they move towards the apoptotic compartment at the apex of the FAE, favouring the hypothesis of a plastic phenotype. The follicle-associated epithelium (FAE) is found exclusively over lymphoid follicles in mucosal tissues, including Peyer?s patches. The enterocytes over Peyer?s patches express a distinct phenotype when compared to the villi enterocytes, characterized by the down regulation of digestive and defense functions and the constitutive expression of chemokines, i.e. CCL20 and CCL25. The purpose of this study was to investigate and identify the potential cells and/or molecules instructing FAE differentiation. Contact between the epithelial and the mesenchymal cell compartment is required for gut morphogenesis. Extracellular matrix molecules (ECM) can activate key regulatory genes which in turn control cell adhesion and differentiation. In the gut, mesenchymal cells differentiate into myofibroblats that participate to the elaboration of ECM. We have described a differential expression of extracellular matrix components under the FAE, correlating with the absence of subepithelial myofibroblats. Molecular mechanisms of FAE differenciation. Different studies proposed an influence of the luminal compartment in the differentiation and/or the maturation of PP. CCL20, a chemokine able to recruit cells that initiate adaptive immunity constitutes our first positive FAE molecular marker. We have shown that CCL20 gene expression is inducible in vitro and in vivo in intestinal epithelium by flagellin, a component of bacterial flagella. This effect was not restricted to the FAE. Lymphotoxin ß (LTß) signaling is critical for PPs organogenesis as LT deficient mice as well as LTß-receptor-/- mice lack PPs and most of the lymph nodes (LN). The continuous signaling via LTßR-expressing cells appears necessary for the maintenance throughout the life of PP architecture. We obtained in vitro and in vivo evidence that LTß signalling is involved in CCL20 gene expression.

A fruticultura como alternativa para a produção familiar no âmbito do Pronaf nos municípios de Campos dos Goytacazes e São Francisco do Itabapoana - RJ

O trabalho analisa a importância do cultivo de frutas como alternativa para o aumento de renda da agricultura familiar, no contexto dos financiamentos concedidos pelo PRONAF. Os resultados evidenciaram que o recurso financeiro foi a variável que mais limitou a escolha dos agricultores. Maracujá, goiaba e pinha foram identificadas como as melhores alternativas econômicas para os produtores familiares da região. A análise permitiu concluir que a concessão do crédito, pelo PRONAF, contribui para a melhor utilização dos recursos, para a obtenção de maior renda, bem como para a geração de empregos.

Estimativa dos níveis ótimos e econômicos de irrigação no mamoeiro (Carica papaya L.) cultivar Golden nas condições do norte do Espírito Santo

Objetivou-se, no presente trabalho, identificar os níveis ótimos de irrigação e adubação nitrogenada que propiciem a máxima produtividade física e econômica da cultivar de mamoeiro Golden. Na identificação dos níveis ótimos, utilizou-se a função de produção. O estudo experimental foi conduzido na fazenda Caliman Agrícola S.A., no município de Linhares-ES. Utilizou-se o delineamento estatístico experimental em blocos casualizados, com esquema fatorial 5x4, em parcelas subdivididas, sendo cinco lâminas de irrigação (0,5; 0,7; 0,9; 1,1 e 1,3 da evapotranspiração de referência), com turno de rega diário, e quatro doses de sulfato de amônio (90; 188; 288 e 377 kg ha-1mês-1). A estimativa da produtividade (t ha-1), em função da lâmina total de água aplicada, obteve ajuste estatístico significativo (p < 0,05) ao modelo de segunda ordem. A máxima produtividade econômica foi igual a 94,83 t ha-1, com lâmina máxima de 1.546,5 mm. A receita líquida operacional dos mercados interno e externo foi de 313,19 e 929,57 R$ ha-1 mês-1, respectivamente.

Geology of the Cerro-Quema Au-Cu deposit (Azuero Peninsula, Panama)

The Cerro Quema district, located on the Azuero Peninsula, Panama, is part of a large regional hydrothermal system controlled by regional faults striking broadly E-W, developed within the Río Quema Formation. This formation is composed of volcanic, sedimentary and volcano-sedimentary rocks indicating a submarine depositional environment, corresponding to the fore-arc basin of a Cretaceous-Paleogene volcanic arc. The structures observed in the area and their tectono-stratigraphic relationship with the surrounding formations suggest a compressive and/or transpressive tectonic regime, at least during Late Cretaceous-Oligocene times. The igneous rocks of the Río Quema Formation plot within the calc-alkaline field with trace and rare earth element (REE) patterns of volcanic arc affinity. This volcanic arc developed on the Caribbean large igneous province during subduction of the Farallon Plate. Mineralization consists of disseminations of pyrite and enargite as well as a stockwork of pyrite and barite with minor sphalerite, galena and chalcopyrite, hosted by a subaqueous dacitic lava dome of the Río Quema Formation. Gold is present as submicroscopic grains and associated with pyrite as invisible gold. A hydrothermal alteration pattern with a core of advanced argillic alteration (vuggy silica with alunite, dickite, pyrite and enargite) and an outer zone of argillic alteration (kaolinite, smectite and illite) has been observed. Supergene oxidation overprinted the hydrothermal alteration resulting in a thick cap of residual silica and iron oxides. The ore minerals, the alteration pattern and the tectono-volcanic environment of Cerro Quema are consistent with a high sulfidation epithermal system developed in the Azuero peninsula during pre-Oligocene times.

INCENTIVOS À PRODUÇÃO DE FRUTAS E AS MUDANÇAS NA AGRICULTURA DA REGIÃO NORTE DO ESTADO DO RIO DE JANEIRO

A economia agrícola da região Norte Fluminense é, historicamente, dependente da atividade sucroalcooleira. Na tentativa de reduzir tal dependência, vêm sendo adotados incentivos ao desenvolvimento da fruticultura na região, particularmente através do “Programa Frutificar”. O presente trabalho visa a avaliar os impactos desse programa, sob a óticade sua contribuição para elevar a produção de frutas e diversificar a agricultura regional. A análise foi efetuada mediante o emprego do modelo , shift-sharede taxas geométricas de crescimento, e do Índice de Diversificação. De mão dessas análises, pode-se concluir que foi constatada a redução da área agrícola da região, particularmente associada à queda nas áreas cultivadas com cana-deaçúcar, arroz, milho e feijão. Por outro lado, no período sob estímulo do “Programa Frutificar”, verificouse aumento do cultivo das fruteiras: abacaxi, banana e coco-da-baía. Esta constatação é um indicativo da contribuição da fruticultura como fator de diversificação da economia agrícola regional. Cabe ressaltar que a economia da região Norte Fluminense é ainda fortemente dependente do setor sucroalcooleiro.

Molluscan radiations and landscape evolution in Miocene Amazonia

This PhD study aims to exploit the rich archive provided by the Miocene mollusc fauna of the Pebas Formation and other inland Miocene Amazonian formations to reconstruct landscape evolution and biotic development in lowland Amazonia during the Neogene. Over 160 samples from more than 70 Pebas Formation outcrops mostly collected by the author were processed for this study. Additional samples were collected in Andean areas of Colombia and Venezuela and further material from other northwestern South American basins was studied in museums. Pebas Formation samples and well log data made available by Occidental Peru from three wells in the Marañon Basin in Peru were also investigated. During this study four genera and 74 species from the Pebas Formation have been described and a further 13 species have been introduced in open nomenclature, and several species were reported for the first time. The number of mollusc species attributed to the Pebas fauna has increased from around 50 to 156. The Pebas fauna is characterised as aquatic, endemic and extinct, and is a typical representative of a long-lived lake fauna. Fluvial taxa are not common, (marginal) marine taxa are rare. An additional molluscan fauna from the Miocene Solimões Formation of Brazil, containing 13 fresh water species was also described. The newly documented fauna was used to improve biostratigraphic framework of Miocene Amazonian deposits. Twelve mollusc zones were introduced, the upper eleven of which cover a time interval of approximately seven million years covered previously by only three pollen zones. An age model calculated for the borehole data indicates that the Pebas Formation was deposited between c. 24 and 11 Ma. The areal distribution of the outcropping mollusc zones uncovered a broad dome structure, termed here the Iquitos-Araracuara anteclise in the study area. The structure appears to have influenced river courses and also contributed to edaphic heterogeneity that may have been in part responsible for the current high biodiversity in the study area. The Pebas system was a huge system (> one million km2) dominated by relatively shallow lakes, but also containing swamps and rivers. The system was fed by rivers draining the emergent Andes in the west and lowlands and cratons to the east. The Pebas system was located at sea level and was open to marine settings through a northern portal running through the Llanos Basin and East Venezuela Basin towards the Caribbean. Cyclical baselevel changes possibly related to Mylankhovitch cycles, have been documented in depositional sequences of the Pebas Formation. The composition of the Pebasian mollusc fauna implies that the system was mostly a fresh water system. Such an interpretation is matched by strontium isotope ratios as well as very negative δ18O ratios found in the shells, but is at odds with oligohaline and mesohaline ichnofacies found in the same strata. The mollusc fauna of the Pebas Formation diversified through most of the existence of the lake system. The diversification was mostly the result of in-situ cladogenesis. The success of some of the Pebasian endemic clades is explained by adaptation to fresh water, low oxygen, common unconsolidated lake bottoms (soup grounds) as well as high predation intensity. Maximum diversity was reached at the base of the late Middle to early Late Miocene Grimsdalea pollen zone, some 13 Ma. At the time some 85 species co-occurred, 67 of which are considered as Pebasian endemics. A subsequent drop in species richness coincides with indications of elevated salinities, although a causal relation still needs to be established. Apparently the Pebas fauna went (almost) entirely extinct with the replacement of the lake system into a fluvio-tidal system during the Early Late Miocene, some 11 Ma.