The Sorbas Basin. Geological Features
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1 The Basin Geological Features
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3 desplegable INGLES OK copia.qxp 27/5/08 01:43 Página 1 Geological Features and Evolution STRATIGRAPHY OF THE SORBAS BASIN Geological Features and Evolution GEOLOGICAL MAP OF THE SORBAS BASIN 50 m A. UPPER TORTONIAN (around 8 Ma) QUATERNARY Graphic Scalebar Millions of years 1.8 R SIER 10 9 PLIOCENE 5.3 PALAEOGEOGRAPHICAL EVOLUTION OF THE SORBAS BASIN FROM THE UPPER TORTONIAN (8 Ma) TO THE LOWER PLIOCENE (4 Ma) GEOLOGICAL CONTEXT OF THE SORBAS BASIN F LOS Conglomerates and sands AL Bioclastic sands ILL HAM Emerged land 5 Km Shallow platform MESSINIAN Gypsum 5 Marls 4b 4a 4b Fringing reefs 4a Calcarenites 3 Bioclastic limestones 2b 2c 2a Open sea Submarine high Cabo de Gata Platform ALHAMILA Palaeo Deltas BÉDAR Coral reef Open sea Shallow sea ALHAMILA (reefal lagoon) Neogene sediments Neogene volcanic rocks Modified from Montenat, Km Position of geological section Betic Substratum D. UPPER MESSINIAN (evaporitic unit, around 5.5 Ma) GEOLOGICAL SECTION E. UPPER MESSINIAN (around 5.4 Ma) SE Gypsum karst Sierra Alhamilla Río Aguas 2b Reefal limestones 2c Marls, sands and conglomerates Abanicos deltaicos Bédar Semi-arid basin Conglomerates and red sands Open sea Barrier ALHAMILA Palaeo Enclosed lagoon CABRERA 1 Submarine fan Tabernas NW TORTONIAN 7.1 PRE-MIOCENE C. LOWER MESSINIAN (around 6 Ma) Bédar Submarine fan 7a Conglomerates, oolites, patch reefs and stromatolites 7b Sands and muds Almería Conglomerates, sands and muds 7a 7b B. END TORTONIAN-LOWER MESSINIAN (around 7 Ma) Vera RERA CAB A Níjar SIERRA DE GÁDOR 8 A DE RES ILAB Sea Zone Beach/ Barrier island CABRERA ALHAMILA F. PLIOCENO INFERIOR (around 4 Ma) Palaeo CABRERA ALHAMILA Betic Substratum. Metamorphic rocks: phyllites, schists, quartzites, marbles, etc... 5 Km 101
4 THE SORBAS KARST. Origin of the gypsum Geological Features and Evolution Around 5.5 million years ago (in the Messinian) the Mediterranean dried up through closure of its communication with the Atlantic Ocean due to tectonic uplift, and masses of evaporites (gypsum and salt) were deposited in its central and deepest region. The thickness of accumulated salt (mainly sodium chloride) exceed 1500 m in some places. In relation to this phenomenon, important deposits of gypsum (hydrated calcium sulphate) were also deposited in the Basin, which locally exceed 130 m in thickness and that outcrop over an area of nearly 25 square kilometres. Fringing reef Basin Mediterranean Atlantic Normal salinity Situation prior to the deposition of evaporites, with the formation of reefs along the margins and marly-muddy sediments in the basin. 44º Gibraltar 200 Km Spain Morocco 32º 8º 0º Erosion Alborán SEDIMENTARY INTERPRETATION FOR THE SORBAS GYPSUM IN A MEDITERRANEAN CONTEXT A (5.9 Ma bp) Desiccation 8º 16º Salt B C (5.5 Ma bp) Evaporation Gypsum and other salts Evaporite deposits in the centre of the Mediterranean result from this disconnection with the Atlantic, and drying out. Gypsum N Juan C. Braga - José M. Martín Taken from Rouchy, 1980 AEREAL DISTRIBUTION OF MESSINIAN SALT DEPOSITS IN THE MEDITERRANEAN SEA Semi-confined Basin Evaporite deposits in the interior of the Basin. The Basin constitutes an intermontane basin of singular geological interest for the study and understanding of palaeogeographical and palaeoenvironmental changes occurring on the Mediterranean coast during the last 8 million years, and its relationship to the geological evolution of the Betic Cordillera. Eight million years ago (in the Upper Miocene), the configuration of land emerged and submerged beneath the sea along the coastal zone of Almería was similar to present, but not identical: the sea spread across the Basin, dry land today, up to the foothills of the Sierra de los Filabres, in whose margin reefs of fossil corals from this age remain as testament, closely marking the position of the ancient. On the slopes, submarine fans deposited thick and extensive sediments that the rivers stripped out from the emergent relief. The later emergence of Sierra Alhamilla and Sierra Cabrera configured a long and narrow intermontane marine basin between these new relieves, to the south, and Los Filabres, towards the north, where the deposition of marine sediments continued: this is today called the Basin. At the end of the Miocene (around 5,5 million years ago, during the Messinian) an enhanced process of desiccation of the Mediterranean Sea caused the marine Basin to become practically dry, with a very shallow depth subjected to strong evaporation. In these circumstances a package of gypsum almost 100 metres in thickness was deposited: the gypsum. Afterwards, the sea reoccupied its level, continuing the accumulation of marls and detrital sediments above the gypsum, up until, around 3.5 million years ago (in the Pliocene), DISTRIBUTION OF EMERGED LAND AND SEA 6 MILLION YEARS AGO Atlantic Ocean Guadalquivir Basin Almería Mediterranean Sea Juan C. Braga - José M. Martín the progressively retreated until reaching its present position. The final retreat of the sea meant that the marine sediments became exposed to the action of erosive agents. The removal of the upper sedimentary layers left the highly soluble gypsum subjected to the continuous action of water, which progressively dissolved it. Therefore, one of the most important gypsum karst landscapes in the world for its size, worth and beauty started to form. ALHAMILLA Mediterranean Sea Coastline
5 Geological Features and Evolution Juan C. Braga - José M. Martín The Basin constitutes an intermontane basin of singular geological interest for the study and understanding of palaeogeographical and palaeoenvironmental changes occurring on the Mediterranean coast during the last 8 million years, and its relationship to the geological evolution of the Betic Cordillera. Eight million years ago (in the Upper Miocene), the configuration of land emerged and submerged beneath the sea along the coastal zone of Almería was similar to present, but not identical: the sea spread across the Basin, dry land today, up to the foothills of the Sierra de los Filabres, in whose margin reefs of fossil corals from this age remain as testament, closely marking the position of the ancient. On the slopes, submarine fans deposited thick and extensive sediments that the rivers stripped out from the emergent relief. The later emergence of Sierra Alhamilla and Sierra Cabrera configured a long and narrow intermontane marine basin between these new relieves, to the south, and Los Filabres, towards the north, where the deposition of marine sediments continued: this is today called the Basin. At the end of the Miocene (around 5,5 million years ago, during the Messinian) an enhanced process of desiccation of the Mediterranean Sea caused the marine Basin to become practically dry, with a very shallow depth subjected to strong evaporation. In these circumstances a package of gypsum almost 100 metres in thickness was deposited: the gypsum. Afterwards, the sea reoccupied its level, continuing the accumulation of marls and detrital sediments above the gypsum, up until, around 3.5 million years ago (in the Pliocene), DISTRIBUTION OF EMERGED LAND AND SEA 6 MILLION YEARS AGO Atlantic Ocean Guadalquivir Basin Almería Mediterranean Sea the progressively retreated until reaching its present position. The final retreat of the sea meant that the marine sediments became exposed to the action of erosive agents. The removal of the upper sedimentary layers left the highly soluble gypsum subjected to the continuous action of water, which progressively dissolved it. Therefore, one of the most important gypsum karst landscapes in the world for its size, worth and beauty started to form. ALHAMILLA Mediterranean Sea Coastline 99
6 STRATIGRAPHY OF THE SORBAS BASIN 50 m Millions of years QUATERNARY 10 Conglomerates and sands Bioclastic sands 5.3 PLIOCENE 8 Conglomerates, sands and muds 7a 7b 7a Conglomerates, oolites, patch reefs and stromatolites 7b Sands and muds MESSINIAN 6 5 4b 4a Gypsum Marls 4b Fringing reefs 4a Calcarenites 7.1 TORTONIAN 3 2b 2c Bioclastic limestones 2b Reefal limestones 2c Marls, sands and conglomerates PRE-MIOCENE 2a 1 Conglomerates and red sands Betic Substratum. Metamorphic rocks: phyllites, schists, quartzites, marbles, etc...
7 Geological Features and Evolution GEOLOGICAL MAP OF THE SORBAS BASIN GEOLOGICAL CONTEXT OF THE SORBAS BASIN Graphic Scalebar SIERRA DE LOS SIERRA DE GÁDOR Almería ALHAMILLA Vera CABRERA Níjar Cabo de Gata Neogene sediments Modified from Montenat, Km Position of geological section Neogene volcanic rocks Betic Substratum GEOLOGICAL SECTION NW Gypsum karst SE Sierra Alhamilla Río Aguas 5 Km
8 Geological Features and Evolution PALAEOGEOGRAPHICAL EVOLUTION OF THE SORBAS BASIN FROM THE UPPER TORTONIAN (8 Ma) TO THE LOWER PLIOCENE (4 Ma) A. UPPER TORTONIAN (around 8 Ma) B. END TORTONIAN-LOWER MESSINIAN (around 7 Ma) C. LOWER MESSINIAN (around 6 Ma) 5 Km Submarine fan Emerged land Shallow platform Tabernas Submarine fan Submarine high ALHAMILA Bédar Platform Open sea BÉDAR Palaeo Coral reef Deltas Open sea Shallow sea ALHAMILA (reefal lagoon) D. UPPER MESSINIAN (evaporitic unit, around 5.5 Ma) E. UPPER MESSINIAN (around 5.4 Ma) F. PLIOCENO INFERIOR (around 4 Ma) Open Bédar sea Semi-arid basin Barrier CABRERA ALHAMILA Palaeo Enclosed lagoon Abanicos deltaicos ALHAMILA Sea Zone Beach/ Barrier island CABRERA Palaeo ALHAMILA CABRERA 101
9 THE SORBAS KARST. Origin of the gypsum Juan C. Braga - José M. Martín Around 5.5 million years ago (in the Messinian) the Mediterranean dried up through closure of its communication with the Atlantic Ocean due to tectonic uplift, and masses of evaporites (gypsum and salt) were deposited in its central and deepest region. The thickness of accumulated salt (mainly sodium chloride) exceed 1500 m in some places. In relation to this phenomenon, important deposits of gypsum (hydrated calcium sulphate) were also deposited in the Basin, which locally exceed 130 m in thickness and that outcrop over an area of nearly 25 square kilometres. 44º Gibraltar 200 Km Spain Alborán Morocco 32º 8º 0º 8º 16º Salt N Taken from Rouchy, 1980 AEREAL DISTRIBUTION OF MESSINIAN SALT DEPOSITS IN THE MEDITERRANEAN SEA SEDIMENTARY INTERPRETATION FOR THE SORBAS GYPSUM IN A MEDITERRANEAN CONTEXT Basin Mediterranean Atlantic Fringing reef A (5.9 Ma bp) B C (5.5 Ma bp) Normal salinity Erosion Desiccation Evaporation Semi-confined Basin Situation prior to the deposition of evaporites, with the formation of reefs along the margins and marly-muddy sediments in the basin. Gypsum and other salts Evaporite deposits in the centre of the Mediterranean result from this disconnection with the Atlantic, and drying out. Gypsum Evaporite deposits in the interior of the Basin. 102
10 Origin of the gypsum The gypsum deposits in the Basin were not, however, strictly contemporaneous with the deposition of evaporites in the centre of the Mediterranean, but somewhat later. This deposition took place during the reflooding phase of the Mediterranean, upon refilling with new water, presumably coming from the Atlantic and invading a broad semi-restricted depression, that at the time occupied a large part of what today constitutes the Basin. The gypsum was deposited in an evaporitic basin, of restricted character, closed towards the west and separated from the open sea by a submarine barrier located at its most easterly end, created through uplift of the Sierra Cabrera. PALAEOGEOGRAPHY OF THE SORBAS BASIN DURING GYPSUM DEPOSITION (5.5 Ma bp) Open sea BÉDAR BARRIER PALAEOCOASTLINE SEMI-RESTRICTED LAGOON CABRERA ALHAMILLA Semi-restricted basin Evaporation Basement Gypsum precipitation Barrier Open sea 103
11 Origin of the gypsum In detail, the evaporite sequence of consists of banks of gypsum, of up to 20 m thickness, separated by marly-limestone intervals and/or carbonates. The thickness of the gypsum banks diminishes towards the top at the same time as that of the non-evaporitic intervals increases. The latter, at least in the higher part, possess a marine character, in that they incorporate the remains of the calcareous skeletons of marine organisms and record the different episodes of basin inundation. STRATIGRAPHICAL COLUMN OF THE SORBAS EVAPORITE SEQUENCE AND DETAILED STRUCTURE OF THE GYPSUM BANKS WITHIN THE SUCCESSION Mts Taken from Dronkert, 1976 Supercones Field view of the gypsum banks. Supercone In the highest banks of gypsum in the sequence a very spectacular growth structure of arborescent character evidently forms, known as supercones (also called cauliflowers), that are interpreted as resulting from competition between the growth of gypsum and the deposition of contemporaneous muddy sediments Palisades Nucleation Cones Detailed field view of the gypsum supercones. 30 according to Dronkert, Gypsum 10 Marly limestones and/or muds Carbonates Field photograph of the gypsum banks from the upper part of the evaporite sequence. 104
12 Karst: the slow dissolution of the rocks M. Villalobos Rainwater and groundwater are capable of dissolving soluble rocks in a slow process that takes thousands of years. The resultant landscape, known as karst or karstic landscape, is very peculiar. It is characterised by the presence of abundant closed depressions at the surface (dolinas, potholes, etc.) and a complex subterranean drainage system (cavities). FEATURES IN KARST LANDSCAPE 1. Tepuys (Karst en cuarcitas) 2. Pitons, Stacks,Towers (tropical karst) 3. Lapiés/Karren (high mountain karst) 4. Dissolution Dolina 5. Uvala 6. Polje 7. Ponor 8. Collapse dolinas 9. Rock bridge 10. Joint 11. Sinkhole 12. Pothole 13. Chimney 14. Cascade 15. Bedding Plane 16. Pipe 17. Sump 18. Debris cone 19. Gours 20. Fossil Gallery 21. Lake 22. Column 23. Resurgence 24. Dry valley 25. Trop Plein 26. Cave 27. Canyon A B Karstification of gypsum is an infrequent phenomenon in nature.the greater part of known karst are limestones.the karst is the most important gypsum karst in Spain, and one of the four best known examples in Europe. Additionally, it has a very high scientific and didactic value in a world context. Taken from J. L. Saura. C A B C Zone of recharge (photo J. M. Calaforra). Zone of transfer (photo J. M. Calaforra). Flooded Zone (photo J. M. Calaforra). 105
13 How is the gypsum karst of formed? J. M. Calaforra 1. The gypsum is originally covered by other sediments, on top of which the incipient drainage network starts to install itself. 1. THE DRAINAGE NETWORK IS ESTABLISHED Basin Faults 2. THE SURFICIAL DISSOLUTION OF GYPSUM STARTS 2. The drainage network erodes the upper sediments until exposing the gypsum in very localised places where the first dolinas originally start to be dissolved. Basin 3. SUBTERRANEAN DRAINAGE IS INITIATED 3. The gypsum is becoming exposed to a greater extent at the surface through time. A multitude of dolinas develop that favour the entrance of water into the interior. Sierra de losfilabres Basin 4. KARST DEVELOPS 4. The general entrance of water into the gypsum mass promotes its slow dissolution, creating a complex subterranean network of galleries. Basin 106 Sediments beneath the gypsum Gypsum Sediments above the gypsum
14 Landscape and surface features M. Villalobos A multitude of small depressions pepper the surface of the karst. These are the dolinas. They result from the dissolution or collapse of the surface layers of the gypsum. An escarpment cliff delimits the entire southern margin of the gypsum outcrop. The extensive plain, the escarpment cliff and the valley are the most characteristic elements of the surface landscape. Above the gypsum rock an extensive karstic plain is fashioned. Large gypsum blocks tumble down from the cliff covering the marl slope. These are called block falls. The Río Aguas cuts down towards the south into soft marly sediments giving rise to a broad valley. 107
15 Dissolution features: chambers and galleries J. M. Calaforra - M. Villalobos Rainwater penetrates into the rock interior, starting to dissolve the gypsum. Dissolution progressively enlarges the initial channel. The water penetrates through to the lower layers. The initial crystallization features start to form. (Photo J. Les) The water infiltrates, slowly dissolving gypsum rock, generating a complex network of subterranean galleries. Chambers are formed from galleries through the dissolution of the walls, and by the fall of blocks from the walls and roof
16 Dissolution features: chambers and galleries 4 Slowly meanders are excavated, on occasions they are very long. 5 Only the lower section is permanently flooded
17 Crystallization features: speleothems J. M. Calaforra - M. Villalobos Water circulates through the incipient galleries and chambers, infiltrating and dissolving the gypsum rock. Gypsum is saturated in this slow process so that it then precipitates in the form of small crystals. The roof, walls and floors of chambers and galleries are coated with a multitude of gypsum crystals in fanciful designs and colours. Water infiltrates dissolving the gypsum, is saturated and crystallizes in extremely delicate forms.these are the speleothems. It has taken hundreds of thousands of years, millions at times, in order for nature to sculpt them. Respect them, never touch them, and be careful not to damage them by accident. They have an incalculable value, but only here where they were born, they have no value elsewhere. Stalagmites. Columns. Mamelones. Rings. Stalagmite mounds. Curtains. Corals. Balls. 110
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