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Speleology in Kazakhstan

Shakalov on 04 Jul, 2018
Hello everyone!   I pleased to invite you to the official site of Central Asian Karstic-Speleological commission ("Kaspeko")   There, we regularly publish reports about our expeditions, articles and reports on speleotopics, lecture course for instructors, photos etc. ...

New publications on hypogene speleogenesis

Klimchouk on 26 Mar, 2012
Dear Colleagues, This is to draw your attention to several recent publications added to KarstBase, relevant to hypogenic karst/speleogenesis: Corrosion of limestone tablets in sulfidic ground-water: measurements and speleogenetic implications Galdenzi,

The deepest terrestrial animal

Klimchouk on 23 Feb, 2012
A recent publication of Spanish researchers describes the biology of Krubera Cave, including the deepest terrestrial animal ever found: Jordana, Rafael; Baquero, Enrique; Reboleira, Sofía and Sendra, Alberto. ...

Caves - landscapes without light

akop on 05 Feb, 2012
Exhibition dedicated to caves is taking place in the Vienna Natural History Museum   The exhibition at the Natural History Museum presents the surprising variety of caves and cave formations such as stalactites and various crystals. ...

Did you know?

That fountain is a free-flowing well or spring [16]. see also artesian well; spring, artesian.?

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Featured articles from Cave & Karst Science Journals
Chemistry and Karst, White, William B.
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Featured articles from other Geoscience Journals
Karst environment, Culver D.C.
Mushroom Speleothems: Stromatolites That Formed in the Absence of Phototrophs, Bontognali, Tomaso R.R.; D’Angeli Ilenia M.; Tisato, Nicola; Vasconcelos, Crisogono; Bernasconi, Stefano M.; Gonzales, Esteban R. G.; De Waele, Jo
Calculating flux to predict future cave radon concentrations, Rowberry, Matt; Marti, Xavi; Frontera, Carlos; Van De Wiel, Marco; Briestensky, Milos
Microbial mediation of complex subterranean mineral structures, Tirato, Nicola; Torriano, Stefano F.F;, Monteux, Sylvain; Sauro, Francesco; De Waele, Jo; Lavagna, Maria Luisa; D’Angeli, Ilenia Maria; Chailloux, Daniel; Renda, Michel; Eglinton, Timothy I.; Bontognali, Tomaso Renzo Rezio
Evidence of a plate-wide tectonic pressure pulse provided by extensometric monitoring in the Balkan Mountains (Bulgaria), Briestensky, Milos; Rowberry, Matt; Stemberk, Josef; Stefanov, Petar; Vozar, Jozef; Sebela, Stanka; Petro, Lubomir; Bella, Pavel; Gaal, Ludovit; Ormukov, Cholponbek;
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Your search for reactivation (Keyword) returned 18 results for the whole karstbase:
Showing 1 to 15 of 18
Le palokarst littoral de Provence (Estaque, Calanques et zone de Bandol), 1993, Blanc, J. J.
The general features of coastal paleokarst in Provence are describes: suspended gallery sections and drain-pipes cut across by fracturations or fault reactivation. The types of deformations and breaking observed are tilting, stalactite fall, extension fault sealing, reactivation and speleothem shearing, coastal wall and karstic cleft collapse as well as network deformation. The influence of structural environment is represented by overlapping strata, coastal faults and crossed-fault systems. Emphasis has been laid on the tectonic inheritance as well as the geodynamic context. To conclude, the importance of provenal-ligurian rifting mechanisms and the transition to faulted and distorted margin is underlined.

SEDIMENT-HOSTED GOLD MINERALIZATION IN THE RATATOTOK DISTRICT, NORTH SULAWESI, INDONESIA, 1994, Turner S. J. , Flindell P. A. , Hendri D. , Hardjana I. , Lauricella P. F. , Lindsay R. P. , Marpaung B. , White G. P. ,
The Ratatotok district in the Minahasa Regency of North Sulawesi, Indonesia is an area of significant gold mineralisation. Gold has been mined in the district since at least the 1850s, and intensively by the Dutch between 1900 and 1921 with a recorded production of 5,060 kg of gold. Newmont began exploring the district in 1986, and has delineated a major sediment-hosted replacement-style deposit at Mesel, and other smaller deposits in an 8 X 5 km area. A total drill-indicated resource of over 60 metric tonnes of gold ( 2 Moz) is reported for Mesel, and three of the smaller deposits. Approximately 80% of this resource is refractory. Silver grades are usually low (< 10 g/t). The Mesel deposit is similar to many Carlin-type deposits in carbonate hostrocks, alteration, geochemical signature and ore mineralogy, but is distinct in tectonic setting. The discovery of replacement-style mineralisation at Mesel, in an impure limestone within a Tertiary island arc environment, demonstrates that deposits with outward characteristics similar to Carlin-type mineralisation are not restricted to a continental setting. Carbonate sediments in the Ratatotok district were deposited in a Late Miocene restricted basin. Later compressional tectonics caused uplift that resulted in karst development in the limestone and erosion of the adjacent volcanic arc with deposition of a thick epiclastic unit. This was followed by intrusion of shallow level pre-mineral andesite into the sequence. Mineralisation at Mesel, and probably elsewhere in the district, is synchronous with the late-stage reactivation of strike-slip faults. Mineralising fluids at Mesel were focussed along steep structures sympathetic to these faults, and trapped below a relatively impermeable andesite cap rock. Hydrothermal fluids caused decalcification of the silty, more permeable carbonate units with the formation of secondary dolomite, deposition of fine arsenian pyrite, silica veinlets and gold. Volume loss due to decalcification and dolomite formation caused collapse brecciation which enhanced fluid flow and further mineralisation. This locally culminated in total decarbonation and deposition of massive silica. Late-stage stibnite occurs in structural zones within the ore deposit, whereas arsenic (as realgar and orpiment) and mercury (as cinnabar) are concentrated on the periphery. Elsewhere in the Ratatotok district, gold mineralisation is restricted to replacement-style mineralisation in permeable zones along limestone-andesite contacts, open-space-filling quartz-calcite veins and stockworks, and residual quartz-clay breccias. The residual breccias are developed in-situ, and are interpreted to form by dissolution of the wallrock limestone from around pre-existing mineralisation. This has resulted in widespread eluvial gold occurrences

Signification des remplissages des karsts de montagne, quelques cls lusage des splologues, 1995, Audra, P.
This paper is intended to cavers in order to help them identify the most significant mountain karst infillings. Carbonated varves sedimentation occurs during floodings in glacial environment. The varves block the deep parts of the networks. Pebbles sealings show a powerful erosion in the vadose zone, near glacial sinkholes. Gelifract spreadings are indicators of frost and snow action in periglacial environment. Reworked weathered rocks are the most ancient deposits, inherited from tertiary warm phases when karstification occurred under regolith covers. Their clearing is partly simultaneous with cave systems elaboration, in relation to the alpine uplift, during Pliocene. Speleothems are also warm or temperate climate indicators. Crystalline morphology reflects environmental characteristics, while their surface sight could have been smoothed during discharge reactivations. Finally, some infillings could have recorded neotectonic movements: broken speleothems, deformed clastic sediments, etc.

Interprtation morphomtrique et splo_gense : exemple de rseaux karstiques de Basse-Provence (directions de galeries, modle et maillage structural), 1997, Blanc Jeanjoseph, Monteau Raymond
Successive tectonic phases on limestone massifs are at the origin of a fracturation grid with several pattern dimensions, and linear or organized drain directions. Mechanical reactivations are observed from Oligocene until Plio-Quaternary on a former "pyreneo-provenale" structure (Eocene). Statistical analysis of gallery and fracture directions, cave levels and descent stages (overdeepening) show several erosional stages occurring after the formation of the Antevindobonian erosional surface. The active speleogenesis during Oligocene and Miocene was controlled by tectonics in connection with European rifting and mediterranean opening. In Messinian a short and significant lowering of mediterranean base level (and water table) made drastic erosion and created vertical pits. The horizontal cave level dug during the stabilization phase of Pliocene, now perched over underground rivers, shows a new overdeepening because of glacio-eustatic Quaternary oscillations. Compressive or distensive mechanical reactivations (Upper Miocene, Pliocene, Quaternary) modified the drainage and consequently the cave organization: self-piracy, confluence and diffluence. In the endokarst, the drainage inversion can be detected in late Upper continental Miocene and early Messinian (6,5 Ma), in correlation with the tilting and extension of the continental margin. Five caves in Provence are studied: Sabre, Petit Saint-Cassien, Rampins, Planesselve river, and Tete du Cade networks.

The influence of tectonic structures on karst flow patterns in karstified limestones and aquitards in the Jura Mountains, Switzerland, 2000, Herold T. , Jordan P. , Zwahlen F. ,
The development of karst systems is often assumed to be related to tectonic structures, i. e. joints and faults. However, detailed studies report many of these structures to be indifferent ui even obstacles to karst development. The aim of our study is to present a systematic which helps to explain or even predict whether a specific fault or joint, or a class of such structures are permeable (and therefore likely to be widened to karat conduits) or impermeable. Therefore three extended multi-tracer experiments followed by three months of monitoring were performed at some 95 springs and streams in the Eastern Jura fold-and-thrust belt. In addition, detailed mapping of tectonic and hydrogeological structures, including sinkholes and some 600 springs, has been carried out. The study area is characterised by two large anticlines, which have been affected by pre-fold normal faulting and synorogenic folding and thrusting as well as oblique reactivation of pre-existing faults. Hydrogeologically, two karst aquifers can be distinguished, the lower Mid Jurassic Hauptrogenstein (Dogger Limestone) and the upper Late Jurassic Malm Limestone. Both karst aquifers are confined and separated From each other hy impermeable layers. This study has shown that karst development and groundwater circulation is strongly controlled by tectonic structures resulting in specific meso- to macro-scale anisotropies. Fast long distance transport along fold axes in crest and limb at cas of anticlines is found to be related to extension joints resulting from synorogenic folds. Concentrated lateral drainage of water now from anticline limbs is exclusively related to pre-orogenic normal faults, which have been transtensively reactivated during folding. The same structures are also responsible for the significant groundwater exchange between the lower (inner) and upper (outer) aquifer. This water now, through otherwise impermeable layers, which is reported at several places and in both directions, is suspected to take place in porous calcite fault gouges or fault breccias. Transpressively reactivated normal faults and synorogenic reverse faults, on the other band. are found to have no influence on karst development and groundwater circulation. It is proposed that the systematic found in the Weissenstein area, i.e. that karst conduit development is mainly controlled by extensive or transtensive (reactivated) joints and faults, may also be applied to other tectonically influenced karat regions. Transpressive structures have no significant influence on karst system development and may even act as obstacles

Histoire gologique et enregistrement karstique : exemple du massif de Siou Blanc et de ses abords (Var), 2001, Blanc, Jeanjoseph
Presentation about a middle-elevated karst (625-650 m) in a temperate mediterranean climate excaved into an important limestone and dolomitic sequence (500 m to 900 m), from Bathonian to Coniacian. Tectonic and pedological factors induced the deep drainages, dolines and ouvalas alignments, vertical vadose networks. The observations applied to doline fields give a discrimination of several epikarstic morphologies: little conic- shaped dolines, lobate, bucket, circular or elliptical dolines pits, asymetrical-falling dolines, collapsed-dolines, ouvalas elongated along the fault lines and megadolines. These states are the results of various processes from the Upper Miocene to actual time. Suspended and disconnected poljes (Limate, Valbelle) were at the origin induced by paleo-networks with an orientation from East to West, at the Miocene; then, these formations were slightly shifted by the reactivation of the fault displacement (Messinian) in relation to a volcanic event (Evenos). The karstification of Siou Blanc massif and its environments, after the bauxitic paleo-karst (Albian), shows an exceptional polygenic evolution in relation to the dynamic of the mediterranean margins.

Quaternary tectonics: Influence on the structure of two karstic aquifers of Languedoc (France), 2001, Josnin J. Y. ,
Our research focuses on the effect of Quaternary tectonics on the organization of the conduit network of karst ground water flow. In the Languedoc region, the major karstic systems are developed in Malm and Lower Cretaceous platform limestones. Most of these systems are polygenetic, their genesis and evolution having been controlled by fracturing that occurred during major tectonic phases (ante-Senonian, Eocene, Oligocene, Aquitanian, Pliocene). These complex karst systems were reactivated following Messinian eustatic events, under tectonic conditions which are not well-known, particularly those that occurred during the Quaternary. Small scale deformations and a lack of seismic activity make characterization of current tectonics in Mediterranean Languedoc difficult. The presence of vertical offsets, however, demonstrates that there are active faults in the interior of or in proximity to karst systems. In two karst aquifers within the Garden basin, we have observed a correlation between the orientations of active faults and the principal karst conduits. In the Mialet basin, we demonstrate that erosion resulting from post-Miocene uplift (and so changes of boundary conditions) divides the aquifer into smaller, independent units. In the St Chaptes basin, we reconstruct the history of the karst, proposing that tectonic and eustatic events were predominant in the karstification process and that the climatic conditions were only of secondary importance. We also show how the reactivation of faults can lead to the unblocking of abandoned karst conduits, allowing their reintroduction into the active flow system, a phenomenon that can be explained by the combined influence of the present stress field and hydraulic gradients. This work, which represents a preliminary study, leads to hypotheses that we will subsequently validate through different successive modelings

Recent active faults in Belgian Ardenne revealed in Rochefort Karstic network (Namur Province, Belgium), 2001, Vandycke S. , Quinif Y. ,
This paper presents observations of recent faulting activity in the karstic network of the Rochefort Cave (Namur Province, Belgium, Europe). The principal recent tectonic features are bedding planes reactivated as normal faults, neo-formatted normal faults in calcite flowstone, fresh scaling, extensional features, fallen blocks and displacement of karstic tube. The seismotectonic aspect is expanded by the presence of fallen blocks where normally the cavity must be very stable and in equilibrium. Three main N 070degrees fault planes and a minor one affect, at a decimetre scale, the karst features and morphology. The faults are still active because recent fresh scaling and fallen blocks are observable. The breaking of Holocene soda straw stalactites and displacements of artificial features observed since the beginning of the tourist activity, in the last century, also suggest very recent reactivation of these faults. This recent faulting can be correlated to present-day tectonic activity, already evidenced by earthquakes in the neighbouring area. Therefore, karstic caves are favourable sites for the observation and the quantification of recent tectonic activity because they constitute a 3-D framework, protected from erosion. Fault planes with this recent faulting present slickensides. Thus a quantitative analysis in term of stress inversion, with the help of striated faults, has permitted to reconstruct the stress tensor responsible for the brittle deformation. The principal NW-SE extension (sigma(3) horizontal) is nearly perpendicular to that of the present regional stress as illustrated by the analysis of the last strong regional earthquake (Roermond, The Netherlands) in 1992. During the Meso-Cenozoic, the main stress tectonics recorded in this part of the European platform is similar to the present one with a NE-SW direction of extension. The discrepancy between the regional stress field and the local stress in the Rochefort cave can be the result of the inversion of the sigma(2) and sigma(3) axes of the stress ellipsoid due to its symmetry or of a local modification at the ground surface of the crustal stress field as it has been already observed in active zones

Geohazard map of cover-collapse sinkholes in the 'Tournaisis' area, southern Belgium, 2002, Kaufmann O. , Quinif Y. ,
This paper reports the methodology developed to draw up a geohazard map of cover-collapse sinkhole occurrences in the 'Toumaisis' area. In this area, Carboniferous limestones are overlain by a Mesocenozoic cover, mainly consisting of marls, sand and clay. The thickness of this cover ranges from a few meters to more than 100 m. The surficial morphology of the area does not show any karstic evidence except for the occurrence of these collapses. From a paleogeographical point of view, a developed quaternary karst is not conceivable in the area. Recent works suggested that the collapses are set off from reactivated paleokarsts. The paleokarsts studied in the area proved to be the result of a particular weathering of the limestone. The organization of these paleokarsts seems very low and mainly guided by the limestone fracturing. As for most induced sinkholes, the reactivation of these paleokarsts is linked to the lowering of piezometric heads. In most of the area, a thick cover and intensive land use mask potential surface hints of the buried paleokarsts and of the fracturing of the bedrock. Aerial photographs and remote sensing techniques have therefore shown little results in delineating collapse hazard zones up to now. The study of the surficial morphology is also of little help. In order to draw up the geohazard map in such a difficult context, hydrogeological data and geological mapping information could only be used. These informations are based on a limited number of boreholes and piezometers and are thus, only valid on a regional scale. Records of former collapses were also available. These records were of great interest since sinkhole distribution is obviously clustered in the area. Bedrock roof and cover formation floor altitudes were digitized and adapted to produce digital thematic maps. Piezometric heads were imported from a calibrated groundwater model of the aquifer. These data and a digital elevation model of the area were integrated into a geographical information system (GIs) to produce a coherent 3-D description of the area on a regional scale. Parameters such as the dewatering of the limestone and the thickness of the cover formation where sinkholes occurred were then estimated. Density of former collapses was also computed. This showed that zones of high sinkhole occurrence coincide with zones of heavy lowering of piezometric heads. Combining the density of former collapses with the dewatering of the limestone enabled us to delineate zones of low, moderate and high collapse hazard. (C) 2002 Elsevier Science B.V. All rights reserved

Karst processes from the beginning to the end: How can they be dated?, 2003, Bosk, B

Determining the beginning and the end of the life of a karst system is a substantial problem. In contrast to most of living systems development of a karst system can be „frozen“ and then rejuvenated several times (polycyclic and polygenetic nature). The principal problems may include precise definition of the beginning of karstification (e.g. inception in speleogenesis) and the manner of preservation of the products of karstification. Karst evolution is particularly dependent upon the time available for process evolution and on the geographical and geological conditions of the exposure of the rock. The longer the time, the higher the hydraulic gradient
and the larger the amount of solvent water entering the karst system, the more evolved is the karst. In general, stratigraphic discontinuities, i.e. intervals of nondeposition (disconformities and unconformities), directly influence the intensity and extent of karstification. The higher the order of discontinuity under study, the greater will be the problems of dating processes and events. The order of unconformities influences the stratigraphy of the karst through the amount of time available for subaerial processes to operate. The end of karstification can also be viewed from various perspectives. The final end occurs at the moment when the host
rock together with its karst phenomena is completely eroded/denuded. In such cases, nothing remains to be dated. Karst forms of individual evolution stages (cycles) can also be destroyed by erosion, denudation and abrasion without the necessity of the destruction of the whole sequence of karst rocks. Temporary and/or final interruption of the karstification process can be caused by the fossilisation of karst due to loss of its hydrological function. Such fossilisation can be caused by metamorphism, mineralisation,
marine transgressions, burial by continental deposits or volcanic products, tectonic movements, climatic change etc. Known karst records for the 1st and 2nd orders of stratigraphic discontinuity cover only from 5 to 60 % of geological time. The shorter the time available for karstification, the greater is the likelihood that karst phenomena will be preserved in the stratigraphic record. While products of short-lived karstification on shallow carbonate platforms can be preserved by deposition during the immediately succeeding sea-level rise, products of more pronounced karstification can be destroyed by a number of different geomorphic
processes. The longer the duration of subaerial exposure, the more complex are those geomorphic agents.
Owing to the fact that unmetamorphosed or only slightly metamorphosed karst rocks containing karst and caves have occurred since Archean, we can apply a wide range of geochronologic methods. Most established dating methods can be utilised for direct and/or indirect dating of karst and paleokarst. The karst/paleokarst fills are very varied in composition, including a wide range of clastic and chemogenic sediments, products of surface and subsurface volcanism (lava, volcaniclastic materials, tephra), and deepseated
processes (hydrothermal activity, etc). Stages of evolution can also be based on dating correlated sediments that do not fill karst voids directly. The application of individual dating methods depends on their time ranges: the older the subject of study, the more limited is the choice of method. Karst and cave fills are relatively special kinds of geologic materials. The karst environment favours both the preservation of paleontological remains and their destruction. On one hand, karst is well known for its richness of paleontological sites, on the other hand most cave fills are complete sterile, which is true especially for the inner-cave facies. Another
problematic feature of karst records is the reactivation of processes, which can degrade a record by mixing karst fills of different ages.

Paleokarst: cessation and rebirth?, 2003, Osborne, R. A. L.

The transformation of active karst into paleokarst by burial, isolation or cessation of process is not necessarily permanent. Paleokarst structures and landforms can be and are exhumed or reactivated, sometimes on numerous occasions. There is not a great deal of similarity between the localities where exhumation and reactivation of paleokarst has been reported. Exhumation and reactivation however have not been reported in many karsts that are similar to those where they have been reported. Exhumation and reactivation appears to be favoured in four situations: - the margins of sedimentary basins overlying grand unconformities, the axes of anticlines, narrow steeply-dipping impounded karsts and where paleokarst fill contains unstable minerals. Six processes are principally responsible for exhumation and reactivation: - per-ascensum speleogenesis, eustatic sea level changes, paragenesis, high density speleogenesis, glaciation, and large-scale meteoric speleogenesis. On some occasions karst landforms, particularly caves or segments of caves, may survive intact and unfilled for geologically significant periods of time. These may be completely isolated from the surface environment, or become reactivated by entrance formation due to breakdown, surface lowering or headward erosion. The intersection and reactivation of ancient open cavities and of exhumed cavities by “modern” caves may be much more common than is currently recognised. If caves have histories as long and as complex as the karsts in which they are developed then many “modern” caves will be composite features composed of interconnected “modern”, relict and exhumed cavities excavated at different times by different processes. Unravelling these histories is the new challenge facing cave science. It will require caves to be studied in a much more detailed, thorough and systematic manner and will also require the application of new technologies in surveying, analysis and dating

The 'Calamine' of Southwest Sardinia: Geology, Mineralogy, and Stable Isotope Geochemistry of Supergene Zn Mineralization, 2003, Boni M, Gilg Ha, Aversa G, Balassone G,
The mining district of southwest Sardinia, Italy, is one of the classic areas where primary carbonate-hosted Zn-Pb sulfide ores are associated with a relatively thick secondary oxidation zone containing Zn (hydroxy-)carbonates and silicates, the so-called 'calamine,' exploited until the 1970s. The extent of the capping oxidized ore zones, reaching deep below the surface, is generally independent of the present-day water table. The base of the oxidation profile containing nonsulfide Zn minerals in various uplifted blocks in the Iglesiente area can be both elevated above or submerged below the recent water table. The genesis of the ores is therefore considered to be related to fossil, locally reactivated, oxidation phenomena. The mineralogy of the nonsulfide mineralization is generally complex and consists of smithsonite, hydrozincite, and hemimorphite as the main economic minerals, accompanied by iron and manganese oxy-hydroxides and residual clays. This study places the secondary ores in the context of the tectonostratigraphic and climatic evolution of Sardinia and includes a petrographic and mineralogic study of the most abundant minerals, relating the mineralogy of secondary Zn and Pb carbonates to their stable C and O isotope geochemistry and constraining the origin of the oxidizing fluids and the temperature of mineralization. The{delta} 18OVSMOW values of smithsonite are homogeneous, regardless of crystal morphology, position, and mine location (avg. 27.4 {} 0.9{per thousand}). This homogeneity points to a relatively uniform isotopic composition of the oxidation fluid and corresponding formation temperatures of 20{degrees} to 35{degrees}C. Considering the karstic environment of smithsonite formation in southwest Sardinia, this high temperature could be due to heat release during sulfide oxidation. The carbon isotope compositions of secondary Zn carbonates display considerable variations of more than 9 per mil ({delta}13CVPDB from -0.6 to -10.4{per thousand}). This large range indicates participation of variable amounts of reduced organic and marine carbonate carbon during sulfide oxidation. The isotopic variation can be related to a variation in crystal morphologies of smithsonite, reflecting different environments of formation with respect to water table oscillations in karstic environments (upper to lower vadose to epiphreatic). The same range in{delta} 13C isotope values is displayed by the calcite associated with Zn carbonates and by recent speleothems. The most reliable time span for the deposition of bulk calamine ore in southwest Sardinia ranges from middle Eocene to Plio-Pleistocene, although further multiple reactivation of the weathering profiles, peaking within the warm interglacial periods of the Quaternary, cannot be excluded

Cambial growth of Swietenia macrophylla King studied under controlled conditions by high resolution laser measurements, 2003, Dunisch O, Schulte M, Kruse K,
The kinetics of phloem and xylem formation of two-year-old plants of Swietenia macrophylla King (true mahogany) was studied in a model system along the shoot circumference (experiment 1) and along the shoot axis (experiment 2). The radius increment of the shoot was registered by high resolution laser measurements (accuracy: 2 mum) in a spatial resolution of 7.8 to 41.3 mum along the stem circumference and 1.5 mm along the stem axis. The temporal resolution of the measurements was 2 s in experiment 1 and 20 s in experiment 2. The radius increment of the shoot detected by the laser measurements was predominately due to the radial enlargement of the phloem and xylem derivatives. On the phloem side the reinitiation of radial cell enlargement after a cambial dormancy occurred first in sieve tubes with contact to ray parenchyma cells, while on the xylem side the radial cell enlargement of vessels and paratracheal parenchyma was induced almost simultaneously along the shoot circumference. In the phloem and xylem derivatives, which were formed first after the cambial reactivation, radial cell enlargement was induced almost simultaneously along the shoot axis. In more advanced phases of phloem and xylem formation, radial cell enlargement of phloem and xylem derivatives was induced shoot downwards with a rate of approximately 13 mm per min. The mean rate of radial cell enlargement of the phloem and xylem derivatives was 2.26 and 4.37 mum per min, respectively. These findings suggest that the kinetics of cambial growth of tropical tree species differ significantly from kinetics observed in trees from temperate regions. The laser measurements might provide a useful experimental approach for studies of cambial activity in situ

Paleoseismic phenomena in karst terrains in Bulgaria and Morocco, 2003, Angelova Dora, Belfoul M'hamed Alaeddin, Bouzid Sophia, Filahi Mustapha, Faik Farid

During the recent years there has been a growing interest in recording and investigating the effects of paleoseismic events in surface and underground karst in almost all countries. Karst represents a reliable reference marker for understanding the potential seismicity in regions with instrumentally established low to moderate seismicity. The karst errains in Bulgaria and Morocco occupy considerable areas. The disturbances in surface and underground karst had usually been provoked by catastrophic one-act events or by repeatedly activated movements by earthquakes. The catastrophic seismic events had disturbed the naturally interrelated karst ecosystems and were the reason for rejuvenation, reactivation or attenuation of karst processes. The natural surface and underground relief had been partially or entirely destroyed; a new type of relief had been formed; the geological environment had been disturbed; changes occurred in the flowrate and direction of surface and underground karst water; wetlands of the gravitation type had been formed; natural caves, local grabens, rock-falls and landslides collapsed partially or entirely and terrains were subjected to subsidence and destruction; the ecological balance in urbanized territories had been disturbed. The present work considers the different types of paleoseismic phenomena in the karst terrains in Bulgaria and Morocco. Recommendations are given for the protection of these areas.

ORIGIN AND STRUCTURAL AND STRATIGRAPHIC CONTROL OF CAVES, ?TOCAS? AND ROCK SHELTERS OF IPEÚNA AND ITIRAPINA (SP, 2005, Luiz Felipe Brandini Ribeiro, Fabio. R. Souza Cruz, Marli. Carina. Siqueira. Ribeiro, Daniel. Frnç, Oso. Godoy

Focus on this topic, although they usually concentrate on limestone caves; few papers have been written about the speleogenesis of non-limestone caves (pseudokarst) The present paper was designed to describe the structural control of caves and rock shelters in the regions of Itaqueri da Serra, Ipeúna, São Pedro and neighboring areas. The caves in the region have basically been formed in the sandstone of the Botucatu Formation, with rare occurrences in other rocks, with speleogenesis resulting from the percolation of water and ceiling collapse. In this study the following caves were studied: Fazendão, Paredão, Boca do Sapo, and the Abrigo da Glóra (in the Itirapina mountain range), as well as the rock shelters Roncador (Analândia), Santo Urbano (Corumbataí), Rochedo (Itirapina), and Abrigo da Chuva (Itirapina), and the ?tocas? Toca do Ninho, Toca do Bauru, Toca do Morcego (Itirapina). The methodology used was the identification of the faults and fractures, as well as of the orientation of the central passages, and the identification of the speleothems associated with the fractures. The records were made in the form of rosettes and sterograms of the faults. The majority of the caves reveal faults, fractures and large discontinuities (rifled fault planes) with a North-Northeast (N30) orientation; some of the ?tocas? reveal main passages oriented to the West/Northwest (N270-285). These trends were correlated with the lineaments of a regional nature. The regional orientations NE and NNE are controlled by the NE lineament which represents the reactivation of the Areado fault, underlying the basin of the Paraná River. The reactivation may have given rise to this fault; evidence has been found in the basin of the Paraná River and in the region of Analândia and São Carlos. The NW orientation of the larger caves and some of the ?tocas? is linked to stratigraphic control (crossed stratification is common in the area). Some of the caves also have an extension to the northeast, a direction which may be correlated to neotectonic events.

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