Hypogene Speleogenesis and Karst Hydrogeology of Artesian Basins ( Ucrânia 2009 )

Hypogene Speleogenesisand Karst Hydrogeology of Artesian Basins

Edited by Alexander Klimchouk Derek Ford

Ukr

aini

an In

stitu

te o

f Spe

leol

ogy

and

Kar

stol

ogy

Special Paper 1

Hypogene Speleogenesis and Karst Hydrogeology of Artesian Basins Proceedings of the conference held May 13 through 17, 2009 in Chernivtsi, Ukraine

Edited by

Alexander B. Klimchouk and Derek C. Ford

Ukrainian Institute of Speleology and KarstologySpecial Paper 1

Simferopol2009

Ukrainian Institute of Speleology and Karstology, UkraineVernadsky Tavrichesky National University, UkraineFed’kovich Chernivtsy National University, Ukraine

Institute of Geological Sciences, UkraineNational Cave and Karst Research Institute, USA

Karst Water Institute, USASilesian University, Poland

Katowice Section of the Polish Geographic Society, PolandUkrainian Speleological Association, Ukraine

With support of:Union International of Speleology (UIS),

UIS Commission on Karst Hydrogeology and SpeleogenesisInternational Geoscience Program 513

“Global Study of Karst Aquifers and Water Resources” (UNESCO)International Year of Planet Earth (UNESCO-IUGS)

Patronage Committee Bagrov N.V. – Rector of the Vernadsky Tavrichesky National University, corresponding member of the NASUGozhik P.F. – Director of the Institute of Geological Sciences of NASU, corresponding member of NASU Mel'nichuk S.V. – Rector of the Fed'kovich Chertnivtsi National University, corresponding member of NASUShelepnitsky I.O. – Head of the Chernivtsi Province Council Shestopalov V.M. – Academician-Secretary of the Department of Earth Sciences of NASU, academician of NASU

Organizing Committee Klimchouk A.B. – UISK, Ukraine – Chairman Andrash V.V. – Ternopil' Speleo-Club "Podillya"Andreychuk V.N. – University of Silesia, Poland – UISK, UkraineApostoljuk V.A. – UISK – Ternopil' Speleo-Club "Podillya"Koptchinsky A. – Vienna University, AustriaRudenko V.P. – Fed'kovich Chernivtsy National University Ridush B.T. – UISK - Fed'kovich Chernivtsy National UniversitySokhatsky M.P. – UISK – Borshchiv Regional MuseumVakhrushev B.A. – UISK – Vernadsky Tavrichesky National UniversityZimel's J.L. – UISK – Ternopil' Speleo-Club "Podillya"

Scientific CommitteeShestopalov V. (NAS Ukraine) – Chairman Audra Ph. (University of Nice, France)Auler A. (Brazilian Institute for Karst and Caves, Brazil)Andrejchuk V. (University of Silesia, Poland – UISK, Ukraine)Dublyansky Yu. (Institut für Geologie und Paläontologie, Leopold-Franzens-Universität Innsbruck, Austria) Ford D. (McMaster University, Canada)Forti P. (University of Bologna, Italy)Frumkin A. (Jerusalem University, Israel)Kempe S. (University of Darmstadt, Germany)Klimchouk A. (UISK, Ukraine) Lowe D. (British Geological Survey, Nottingham, UK)Osborne A. (University of Sidney, Australia)Palmer A. (University of Oneonta, USA) Veni G. (National Cave and Karst Research Institute, USA)White W. (Pennsylvania State University)

CONTENTS

PRINCIPAL FEATURES OF HYPOGENE SPELEOGENESIS 7Alexander Klimchouk

HYPOGENE CAVE PATTERNS 17Philippe Audra, Ludovic Mocochain, Jean-Yves Bigot, and Jean-Claude Nobécourt

MORPHOLOGICAL INDICATORS OF SPELEOGENESIS: HYPOGENIC SPELEOGENS 23Philippe Audra, Ludovic Mocochain, Jean-Yves Bigot, and Jean-Claude Nobécourt

HYPOGENE CAVES IN DEFORMED (FOLD BELT) STRATA: OBSERVATIONS FROM EASTERN AUSTRALIA AND CENTRAL EUROPE 33R.A.L. Osborne

IDENTIFYING PALEO WATER-ROCK INTERACTION DURING HYDROTHERMAL KARSTIFICATION: A STABLE ISOTOPE APPROACH 45Yuri Dublyansky and Christoph Spötl

MICROORGANISMS AS SPELEOGENETIC AGENTS: GEOCHEMICAL DIVERSITY BUT GEOMICROBIAL UNITY 51P.J.Boston, M.N. Spilde, D.E. Northup, M.D. Curry, L.A. Melim, and L. Rosales-Lagarde

SIDERITE WEATHERING AS A REACTION CAUSING HYPOGENE SPELEOGENESIS: THE EXAMPLE OF THE IBERG/HARZ/GERMANY 59Stephan Kempe

SIMULATING THE DEVELOPMENT OF SOLUTION CONDUITS IN HYPOGENE SETTINGS 61C. Rehrl, S. Birk, and A. B. Klimchouk

EVOLUTION OF CAVES IN POROUS LIMESTONE BY MIXING CORROSION: A MODEL APPROACH 67Wolfgang Dreybrodt, Douchko Romanov , and Georg Kaufmann

SPELEOGENESIS OF MEDITERRANEAN KARSTS: A MODELLING APPROACH BASED ON REALISTIC FRACTURE NETWORKS 75Antoine Lafare, Hervé Jourde, Véronique Leonardi, Séverin Pistre, andNathalie Dörfliger

GIANT COLLAPSE STRUCTURES FORMED BY HYPOGENIC KARSTIFICATION: THE OBRUKS OF THE CENTRAL ANATOLIA, TURKEY 83C. Serdar Bayari, N. Nur Ozyurt, and Emrah Pekkans

ON THE ROLE OF HYPOGENE SPELEOGENESIS IN SHAPING THE COASTAL ENDOKARST OF SOUTHERN MALLORCA (WESTERN MEDITERRANEAN) 91Joaquín Ginés, Angel Ginés, Joan J. Fornós, Antoni Merino and Francesc Gràcia

HYPOGENE CAVES IN THE APENNINES (ITALY) 101Sandro Galdenzi

STEGBACHGRABEN, A MINERALIZED HYPOGENE CAVE IN THE GROSSARL VALLEY, AUSTRIA 117Yuri Dublyansky, Christoph Spötl, and Christoph Steinbauer

HYPOGENE CAVES IN AUSTRIA 121Lukas Plan, Christoph Spötl, Rudolf Pavuza, Yuri Dublyansky

KRAUSHÖHLE: THE FIRST SULPHURIC ACID CAVE IN THE EASTERN ALPS (STYRIA, AUSTRIA) 129Lukas Plan, Jo De Waele, Philippe Audra, Antonio Rossi, and Christoph Spötl

HYDROTHERMAL ORIGIN OF ZADLAŠKA JAMA, AN ANCIENT ALPINE CAVE IN THE JULIAN ALPS, SLOVENIA 131Martin Knez and Tadej Slabe

ACTIVE HYPOGENE SPELEOGENESIS AND THE GROUNDWATER SYSTEMS AROUND THE EDGES OF ANTICLINAL RIDGES 137Amos Frumkin

SEISMIC-SAG STRUCTURAL SYSTEMS IN TERTIARY CARBONATE ROCKS BENEATH SOUTHEASTERN FLORIDA, USA: EVIDENCE FOR HYPOGENIC SPELEOGENESIS? 151Kevin J. Cunningham and Cameron Walker

HYPOGENE SPELEOGENESIS IN THE PIEDMONT CRIMEA RANGE 159A.B. Klimchouk, E.I. Tymokhina and G.N. Amelichev

STYLES OF HYPOGENE CAVE DEVELOPMENT IN ANCIENT CARBONATE AREAS OVERLYING NON-PERMEABLE ROCKS IN BRAZIL AND THE INFLUENCE OF COMPETING MECHANISMS AND LATER MODIFYING PROCESSES 173Augusto S. Auler

MORPHOLOGY AND GENESIS OF THE MAIN ORE BODY AT NANISIVIK ZINC/LEAD MINE, BAFFIN ISLAND, CANADA: AN OUTSTANDING EXAMPLE OF PARAGENETIC DISSOLUTION OF CARBONATE BEDROCKS WITH PENE-CONTEMPORANEOUS PRECIPITATION OF SULFIDES AND GANGUE MINERALS IN A HYPOGENE SETTING 181Derek Ford

THE INFLUENCE OF HYPOGENE AND EPIGENE SPELEOGENESIS IN THE EVOLUTION OF THE VAZANTE KARST MINAS GERAIS STATE, BRAZIL 193Cristian Bittencourt, Augusto Sarreiro Auler, José Manoel dos Reis Neto, Vanio de Bessa and Marcus Vinícios Andrade Silva

HYPOGENIC ASCENDING SPELEOGENESIS IN THE KRAKÓW-CZĘSTOCHOWA UPLAND (POLAND) – EVIDENCE IN CAVE MORPHOLOGY AND SURFACE RELIEF 201Andrzej Tyc

EVIDENCE FROM CERNA VALLEY CAVES (SW ROMANIA) FOR SULFURIC ACID SPELEOGENESIS: A MINERALOGICAL AND STABLE ISOTOPE STUDY 209Bogdan P. Onac, Jonathan Sumrall, Jonathan Wynn, Tudor Tamas, Veronica Dărmiceanu and Cristina Cizmaş

THE POSSIBILITY OF REVERSE FLOW PIRACY IN CAVES OF THE APPALACHIAN MOUNTAIN BELT 211Ira D. Sasowsky

KARSTOGENESIS AT THE PRUT RIVER VALLEY (WESTERN UKRAINE, PRUT AREA) 213Viacheslav Andreychouk and Bogdan Ridush

ZOLOUSHKA CAVE: HYPOGENE SPELEOGENESIS OR REVERSE WATER THROUGHFLOW? 221V. Коrzhyk

EPIGENE AND HYPOGENE CAVES IN THE NEOGENE GYPSUM OF THE PONIDZIE AREA (NIECKA NIDZIAŃSKA REGION), POLAND 223Jan Urban, Viacheslav Andreychouk, and Andrzej Kasza

PETRALONA CAVE: MORPHOLOGICAL ANALYSIS AND A NEW PERSPECTIVE ON ITS SPELEOGENESIS 233Georgios Lazaridis

HYPOGENE SPELEOGENESIS IN MAINLAND NORWAY AND SVALBARD? 241Stein-Erik Lauritzen

VILLA LUZ PARK CAVES: SPELEOGENESIS BASED ON CURRENT STRATIGRAPHIC AND MORPHOLOGIC EVIDENCE 245Laura Rosales-Lagarde, Penelope J. Boston, Andrew Campbell, and Mike Pullin

HYPOGENE KARSTIFICATION IN SAUDI ARABIA (LAYLA LAKE SINKHOLES, AIN HEETH CAVE) 247Stephan Kempe, Heiko Dirks, and Ingo Bauer

HYPOGENE KARSTIFICATION IN JORDAN (BERGISH/AL-DAHER CAVE, UWAIYED CAVE, BEER AL-MALABEH SINKHOLE) 253Stephan Kempe, Ahmad Al-Malabeh, and Horst-Volker Henschel

ASSESSING THE RELIABILITY OF 2D RESISTIVITY IMAGING TO MAP A DEEP AQUIFER IN CARBONATE ROCKS IN THE IRAQI KURDISTAN REGION 257Bakhtiar K. Aziz and Ezzaden N. Baban

FEATURES OF GEOLOGICAL CONDITIONS OF THE ORDINSKAYA UNDERWATER CAVE, FORE-URALS, RUSSIA 267Pavel Sivinskih

ОСОБЕННОСТИ ГИПОГЕННОГО СПЕЛЕОГЕНЕЗА ГОРНО-СКЛАДЧАТОЙ ОБЛАСТИ ЗАПАДНОГО КАВКАЗА 271Б.А.Вахрушев

ГЛУБИННОЕ СТРОЕНИЕ ГИДРОГЕОСФЕРЫ: МОДЕЛЬ ВЕРТИКАЛЬНОЙ ЗОНАЛЬНОСТИ 277В.Н. Катаев

РОЛЬ КАРСТА В ФОРМИРОВАНИИ СОЛЕНЫХ ВОД И РАССОЛОВ ОЛЕНЁКСКОГО БАССЕЙНА 287Александр Кононов, Сергей Алексеев, и Сергей Сухов

193HYPOGENE SPELEOGENESIS AND KARST HYDROGEOLOGY OF ARTESIAN BASINS

Ukrainian Institute of Speleology and Karstology, Special Paper 1, 2009

INTRODUCTIONThe city of Vazante lies in the northwest region of

the state of Minas Gerais (Figure 1),in an area of tropical continental climate characterized by rainy summers and dry winters. The average annual temperature is 21.6 °C and average annual rainfall is about 1470 mm, of which 90% is concentrated between the months of October and March.

The region is an interesting example because it allows a comprehensive direct access to the karstic system in several situations, both in the contemporary vadose zone via dozens of dry caves and below the vadose zone via underground tunnels developed for zinc ore extraction. The Vazante mine exploits the largest Brazilian zinc deposit, with a production of 380 thousand tons/year of zinc concentrate. The zinc mineralization (willemite and hemimorphyte) is located in a shear zone oriented in a northeast direction that cuts across a sequence of carbonate and pellitic rocks belonging to the Neo-Proterozoic Vazante Group. The Vazante underground mine probably ranks among the most complex in the world regarding its hydrogeology and

associated geotechnical problems. This complexity arises primarily due to the fact that its galleries are developed in carbonates with a high degree of karstification.

Significant voids intercepted by the underground mine at depths of up to 250 meters below the regional base level determined by the Santa Catarina River are not consistent with “classic” epigenic karstification models, which imply dissolution driven by meteoric water recharged on the surface. A borehole survey to explore deeper levels of mineralization reported voids at depths of up to 600 meters below the regional base level. These data motivated the investigation of the problem from the perspective of models that consider the migration of ascending fluids unrelated to precipitation and the movement of surface and subsurface water.

GEOLOGY, GEOMORPHOLOGY AND HYDROGEOLOGY

The local geology comprises four distinct units: Morro do Calcario Formation: metadolomites, metadolarenites, •

stromatolitic metadolomites and breccias.

THE INFLUENCE OF HYPOGENE AND EPIGENE SPELEOGENESIS IN THE EVOLUTION OF THE VAZANTE KARST MINAS GERAIS STATE, BRAZIL

Cristian Bittencourt1, Augusto Sarreiro Auler2, José Manoel dos Reis Neto3, Vanio de Bessa4 and Marcus Vinícios Andrade Silva5

1, 4, 5 Votorantim Metais Zinco SA. Rodovia LMG 706 Km65, 38780-000, Vazante, Minas Gerais, Brazil, [email protected], [email protected], [email protected] Instituto do Carste. Rua Kepler 385/04, Belo Horizonte, Minas Gerais, 30360-240, Brazil, [email protected] Universidade Federal do Paraná. Departamento de Geologia. LAMIR. Centro Politécnico, Jardim das Américas, Caixa Postal 19062, 81531-980. Curitiba, Paraná, Brazil, [email protected]

ABSTRACTThe advanced state of karstification in the metadolomites of the Neoproterozoic Vazante Group has resulted in several

geotechnical and hydrogeological problems in an underground zinc mine located in the city of Vazante, state of Minas Gerais, central Brazil, that have prompted detailed hydrogeological studies. The continuity of karstification at depths below the regional base level suggests that hypogenic karstification, driven by migration of fluids from below due to hydrostatic pressure or other sources of energy may be a major player in the area. In this work several tools were used to understand the mechanisms of karstification in the area, focusing on the relationship between karstification and the location of ore bodies.

The influence of both epigene and hypogene processes appears in the Vazante karstic evolution and has a relationship with the cave size. The study demonstrates that the size of voids decreases with depth. The largest cavities (greater than 15 meters) occur above the regional base level. This region is represented by the vadose zone, where epigenic karst processes predominate. Below this elevation, up to 250 meters in depth, a combination of epigene and hypogene processes occurs and the diameter of voids tends to decrease, being usually less than 10 meters. Below 250 meters, the phenomena of karstification are strictly hypogenic and the diameter of voids is limited to less than 5 meters.

194

Bittencourt, Auler, Reis Neto, Bessa and Silva

HYPOGENE SPELEOGENESIS AND KARST HYDROGEOLOGY OF ARTESIAN BASINS


Poço Verde Formation: Green to purple slates and marls with • layers of pink dolomite.

Serra do Garrote Formation: carbonaceous phyllites and quartz • phyllites.

The Geologic Map (Figure 1) shows the location and geometric setting of these formations, all dipping NW.

Geomorphologically, the region can be described as an elongated depression with nearly 60 km of flat relief on the metadolomites surrounded by hilly relief on the metapelites, phyllites and metamarbles. The focus of this study is an area covered by an extensive colluvial and alluvial overburden whose thickness varies from a few meters to more than a hundred meters, making recognition and assessment of the karstic processes difficult. This overburden masks a well-developed karstic surface where big pinnacles are common and ruiniform relief has been identified by drilling.

For the mining operation to be able to extract willemite ore, it is essential that the operations occur in an already drained environment. Therefore, dewatering is an integral part of the mining operations. Water table drawdown is achieved by intercepting hydraulically conductive geological structures through galleries, allowing the water to drain to a pumping station located at the base of the mine at a depth

of 300 meters, and then having it pumped to the surface. Water level drawdown in the rocks of the Morro do Calcário and Poço Verde Formations is influenced by the existence of nine hydrogeological systems. From a hydrogeological point of view, the ore body is an aquitard slowing the underground flow, in spite of the fact that it is located in a fault zone, as observed by FRASA (1990) who described it as an impermeable seal. The schematic cross-section (Figure 2) shows the spatial relationship between these systems and the resulting heterogeneity of the aquifers systems.

KARSTIC FEATURES

Shallow KarstificationField work was directed towards studying caves

and voids, with detailed analysis of the underground morphological features. The Instituto do Carste (Brazilian Karst Research Institute) promoted an exchange of information with the Ukrainian Institute of Speleology and Karstology that facilitated scientific analysis of some major Brazilians caves which potentially displayed hypogene characteristics. Four caves in the region of Vazante were visited, all displaying morphological features generated by hypogene karstification processes, such as feeders, rising

wall channels, rising chains of ceiling cupolas and cupolas (Figure 3).

Two caves (Lapa Nova and Lapa Nova II) are related to the mineralized body (aquitard) and are located in the upper footwall aquifer. These caves are very close to each other although their conduits do not have any lateral physical connection at present. Both caves display a 3D maze pattern (Figure 6). The distal northwestern portion of the caves is located approximately 100 m from the mineralized (willemite) zone and in this sector it is possible to observe a large feeder connected with a master passage, which shows morphological characteristics indicative of the genesis by ascending flow, including associated rising wall channels, ceiling half-tubes, and domes. The flow at this level is from northwest to southeast,in the direction of the Santa Catarina River, the present regional base level.

Deep KarstificationA statistical analysis of

approximately 300,000 meters of boreholes has been performed in order to obtain data about the depth control of karstification. With respect to the relationship

Figure 1. Location and simplified geological context. Modified from DARDENNE, 2000. (1) Paracatu Formation (carbon phyllite with quartzite); (2) Serra do Landim Formation (chlorite phyllite); (3) Serra da Lapa Formation (marlstones, quartzites and dolomites); (4) Serra do Velosinho member (carbonaceous marlstones and shales); (5) Morro do Calcário Formation (stromatolitic bioherms, breccias, metadolomites with algal lamination and marstones); (6) Serra do Garrote Formation (carbonaceous slates and marlstones); (7) Pb.

195




between the presence of voids and the lithological types, the borehole data show that 53% of the voids occur in association with hydrothermal breccias (vicinity of the mineralized body-aquitard), 30% in pink metadolomite (hangwall) and 7% associated with gray metadolomite (upper footwall). The analysis also demonstrates that the size of voids decreases with depth (Figure 4). Down to a depth of approximately 150 meters (to an elevation of 600 m above sea level), voids with diameters greater than 15 meters are not uncommon. Up to 300 meters from surface (elevation 450 m), the diameter of voids tend to decrease, being usually less than 10 meters. Below 450 m, the diameter of voids is restricted to less than 5 meters.

The morphology of the cavities can be described as elongated features, with predominantly vertical development, mainly controlled by structures trending northwest and by the banding of the rock. It is common to observe features of rising flow morphologic suite as defined by KLIMCHOUK (2007). Among them the more frequent are cupolas, vertical tubes, rising wall channels, rising chain of cupolas, and outlets,.

GENESIS OF KARSTIFICATIONIPT (2004) correlated groundwater routes and

karstification depth in the area with the model of groundwater circulation in karst aquifers proposed by WORTHINGTON (1991) that considers the flow depth to be a function of catchment length, dip and strike; it postulates a maximum depth of 170 m (425 m elevation) for the area. However, field data and boreholes show the development of voids below this elevation.

The dissolutional morphological features observed in the caves and in the underground mine show that they are generated thorough karstification by rising flow. In all studied caves, the morphology of conduits indicates genesis by ascending flow but, when a resistant layer is reached, the conduit development follows the dip direction (from NW to SE) until the confining bed is breached and conduits continue at a new upper level. This characteristic is evident in the Lapa Nova Cave, where the master passages have developed preferentially in layers of gray dolomite. The layer that divides the two levels of the cave is a massive pink dolomite with high resistance to flow.

Figure 2. Schematic cross-section illustrating the hydrogeologic systems.

196




Figure 3. Examples of morphological features generated by hypogene speleogenesis as identified in Vazante caves: A = rising chains of ceiling cupolas; B = side feeder with rising wall channels. C = cupola viewed from below; D = feeder; E, F = side feeders; G = outlet with connecting ceiling channel; H = ceiling channel in epigenic speleothem.

197




In both Lapa Nova and Lapa Nova II caves, located near the mineralization, the main feeders are situated in the portion nearest to the mineralized body, as can be seen in Figure 6. At least nine caves in the Vazante region display this behaviour, which suggests that their genesis has been influenced by willemite mineralization. According KLIMCHOUK (2007) the condition of confinement is an essential element for development of hypogene speleogenesis, and the mineralized body meets this requirement. At greater depth (elevation 100 m), when the mineralized body disappears, there is connection between the hangingwall and upper footwall aquifers. The difference in hydraulic properties between the two permits groundwater flow from the hangingwall to the upper footwall through the breccia pores, dissolving them and forming the voids currently observed in the underground mine. Figure 7 show a schematic cross-section illustrating this model.

The activity of epigenic karst processes is also observed in the region. All visited caves are presently in the vadose zone, and display characteristics of later epigenic overprinting such as recent sediment filling and surface water invasion.

The influence of epigene and hypogene processes is also illustrated in schematic cross-section in Figure 7. The largest cavities occur above the regional base level, in the vadose zone where epigenic karst processes predominate. However, we have to bear in mind that at least some of these cavities are likely to be hypogenic in origin, relict with regard to the current vadose conditions. Below this elevation, down to 250 meters in depth, a combination of epigene and hypogene processes occurs, previously analysed by IPT (2004) with the groundwater circulation model of WORTHINGTON (1991). This region corresponds to the epikarst described by FRASA (1991) as a weathered mantle. Below the elevation

Figure 4. Relationship between size and depth of occurrence of cavities.

Figure 5. Examples of morphological features generated by hypogene speleogenesis as identified in Vazante underground mine: A = vertical tubes; B = vertical passage formed by ascending flow. When a resistant layer is reached (phyllite in this case) the conduit develops following the dip direction; C = outlet; D = outlets viewed from below; E, F = outlets in cupolas and domepits; G = cupola and rising wall channels viewed from below.

198




Figure 6. Spatial relationship between the caves (Lapa Nova and Lapa Nova II) and the ore body. The light-grey spots locate the main feeders.

Figure 7. Model for the Vazante karstic system. The graph on the right side relates size versus depth of occurrence of cavities.

199




450 meters, the phenomena of karstification are strictly hypogenic.

At greater depths (below 450 m) hypogene processes alone are responsible for the generation of voids. Following surface denudation, these voids will tend to become shallower in relation to the surface. At elevations around 450 meters (still 250 meters below the regional base level), hypogene features become subject to phreatic (local ground water system) processes. In this phase both hypogene and epigene phenomena coexist, which tends to accelerate the development of caves due to mixing with more aggressive meteoric water. The karst springs, Poço Verde, Poço das Piranhas e Sucuri, are features associated with this system. After reaching the vadose zone, the caves will be subject only to epigenic overprint. Table 1 summarizes the information presented.

ACKNOWLEDGEMENTSThe authors thanks to Votorantim Metais for permission

to use information from the Vazante underground mine and borehole data; to Ukrainian Institute of Speleology and Karstology and Dr. Alexander B. Klimchouk for the important exchange of information about Vazante hypogenic caves.

REFERENCES

Dardenne, M. 2000. The Brasilia Fold Belt Tectonic Evolution of South America International Geological Congress, Rio de Janeiro, Brazil, 231-263 pp.

Frasa Ingenieros Consultores. 1990. Estudio Hidrogeologico-Minero en la Mina Subterránea de Morro da Usina, Vazante, Mina Gerais. Vazante, Votorantim Metais, Relatório Interno, 159 pp.

IPT. 2004. Levantamento Geológico-Estrutural nos Entornos da Mina de Zinco da Votorantim Metais – Unidade Vazante, no Município de Vazante, MG, como Subsídio aos Estudos Hidrogeológicos. Vazante, Votorantim Metais, Relatório Interno, 56 pp.

Klimchouk, A.B. 2007. Hypogene Speleogenesis: Hydrogeologycal and Morphogenetic Perspective. Special Paper 1, National Cave and Karst Research Institute, Carlsbad, NM, 106 pp.

Worthington, S.R.H. 1991. Karst Hydrogeology in the Canadian Rocky Mountains. Hamilton, Ontario, (Ph.D. thesis - McMaster University). 380 pp.

Table 1 Summary of the three depth regions influenced by different flow systems.

Date post:	02-Aug-2016
Category:	Documents
Upload:	marcus-vinicios-andrade-silva
View:	219 times
Download:	3 times

Hypogene Speleogenesis and Karst Hydrogeology of Artesian Basins ( Ucrânia 2009 )

Documents