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翻译部分(英文原文)Coal facies studies in SpainIsabel Suarez-Ruiz ,*, Amalia JimenezINCAR (CSIC), Ap. Co., 73, 33080, Oviedo, SpainGeology, University of Oviedo, 33005, Oviedo, SpainReceived 1 January 2003; accepted 6 June 2003Abstract:This work is a synthesis of the distribution of the main coal basins and sub-basins in Spain as well as the research carried out on their coal facies. The coal fields are distributed through the Paleozoic (mainly Pennsylvanian), Mesozoic (Cretaceous) and Cenozoic times. Peats also exist in the southeast Spain (Granada area), although these types of deposits are not included in this review. Spanish coal basins are both of a paralic and intramontane type and the coal rank is highly variable, from lignite in the case of the younger coal seams to anthracite for those of Carboniferous age.2004 Elsevier B.V. All rights reserved.Keywords: Spain; Coal; Paleozoic; Mesozoic; Coal basins; Rank; Coal facies1. IntroductionThe analysis of facies in Spanish coal basins has developed since the 1980s, although not many data have been reported. The works are mainly based on stratigraphic and sedimentological studies. In some basins, paleobotanical studies, organic petrology and geochemistry have also contributed significant infor-mation about coal facies. Coal basins and other coal areas in Spain are shown in Fig. 1.2. Synthesis of Spanish coal faciesCoal facies analyses have been mainly performed in the following coal basins:Cenozoic coals:-Mequinenza Basin. Oligocene. Sub-bituminous coals.-As Pontes Basin. Eocene Oligocene. Lignite.-Pyrenees area (Berga, Tremp and Ager zones).-Cretaceous Tertiary (Garumnian). Sub-bituminous coals.Mesozoic coals:-Teruel Basin. Lower and Upper Cretaceous. Sub-bituminous coals. Paleozoic (Carboniferous) coals:-Puertollano Basin. Stephanian. High-volatile bitu-minous coals.-Cantabrian Range. Pennsylvanian (Westphalian and Stephanian). Bituminous and anthracite coals. -Penarroya Belmez Espiel area (Penarroya area).Pennsylvanian (Westphalian). Bituminous and an-thracite coals.There are other small basins and sub-basins of Carboniferous and Cretaceous age located in the Pyrenees range as well as Carboniferous coal fields (Mississippian and Pennsylvanian age) in the south and southwestern parts of Spain, but scarce or no data on their coal facies have been reported.Fig. 1. Coal resources in Spain including exploitable coal basins and other coal areas (data from IGME, 1985).2.1. Cenozoic coalsLignites of Mio Pliocene age are found in Gran-ada (Fig. 1) which are linked with lacustrine facies.These types of facies are also assigned to the Tertiary lignite seams from the Baleares Islands (IGME, 1985). However, the most important and best de-scribed areas containing Tertiary coals are those of the As Pontes and Mequinenza Basins (Fig. 1).2.1.1. As Pontes Basin (Eocene Oligocene age)2.1.1.1. Cabrera et al. (1995). Lignite deposits recorded in the Cenozoic As Pontes strike-slip basin (Northwestern Spain) were formed due to early, favourable, warm humid, tropical subtropical pale-oclimatic conditions which later evolved into slightly drier and cooler conditions. The main features of these lignites resulted from the tectonic evolution of the basin, due to the influence of tectonics on the sedimentation/subsidence rate and on the morphology of the basin. The evolution and distribution of the coal facies in this basin is as follows (from bottom to top of the series):(i) swamp marsh to shallow lacustrine facies.(ii) retroactive expansive swamp marsh sequence and progradational retrogradational sequence.(iii) swamp marsh and alluvial facies.(iv) alluvial swamp marsh facies.Sedimentological, petrological and organic geo-chemical data point to the conclusion that, although the paleoenvironments where peat deposition took place did not undergo dramatic changes, they were affected by distinguishable variations (i.e.,water hydrochemistry and groundwater-level stability), linked mostly to the evolution of the morphology and the water balance of the basin.2.1.1.2. Haggeman et al. (1997). Coal seams from the As Pontes Basin are characterized by the frequent occurrences of bright brown coal layers which are highly degraded compared with the dark coals from the same basin. The formation of these bright layers occurred especially during the early evolution stage and was influenced by water table oscillations. Thus, the origin of these levels are clearly related to the depositional environment in which the conditions became progressively drier and more stable towardsthe top of the coal-bearing series where bright layers are found. These authors established that the defined depositional conditions are of far more relevance to the brightness of the coal seam in the As Pontes Basinthan the variations in plant supply. Another important area containing lignite deposits in Northwestern Spain and near to the As Pontes Basin is the Meirama coal field. This is a limnic basin of Miocene age (IGME, 1985) generated by the activation of preexistent faults at the end of the Alpine Orogeny. The tectonic activity originated grabens in which organic material accumulated giving rise to thick coal seams.2.1.2. Mequinenza Basin (Oligocene age)2.1.2.1. Querol et al. (1996). The Mequinenza Ba-sin is located between the limits of Lerida, Huesca and Zaragoza provinces (Fig. 1). Their coal deposits represent a small proportion of Spains low-rank coal reserves and production. The coal is of great scientific interest due to its high sulphur content, especially organic sulphur. The Mequinenza inner lacustrine facies assemblages, which bear most of the coal deposits, were deposited in subaqueous lacustrine zones under alkaline conditions. In the northeast of Spain (Huesca, Lerida, Gerona and Barcelona provinces, Fig. 1), there are other coal deposits of Tertiary age located in undeformed basins with scarce tectonic activity (IGME, 1985). Coal seams are normally found in a horizontal to subhorizontal position. The coal rank is lignite and no information about the corresponding facies has beenreported. Finally, in the Central Pyrenees area (Berga, Tremp and Ager zones), the Garumnian (Mesozoic Tertiary) sub-bituminous coals are well known. The data avail-able can be summed up as follows.2.1.2.2. Garcia-Valles et al. (1993, 1994). The Garumnian (Cretaceous Tertiary) sediments of the Pyrenees contain coal seams in the Berga, Tremp and Ager zones, some of which are mineable coals (Berga coal field). Garumnian coals show humic composition derived from terrestrial plants. A good diagenetic correlation between mineral matter diagenesis and organic matter maturity is found. Petrographic studies indicate that the coal-forming peat was stored in a predominantly forest moor swamp environment. The specific maceral assemblages suggest a subtropical and damp climate during peat deposition. The paleoenvironments are similar in these three areas, which could originally been part of the same basin.2.2. Mesozoic coals (Cretaceous)Mesozoic coals are mainly of Cretaceous age, and some coal fields also located in the Central Pyrenees as well as the Teruel Coal Basin (Fig. 1) are the most representative areas for coals of this age (Fig. 1). Coals from the Central Pyrenees are characterized by their low rank. They are mainly lignites (IGME, 1985) while those from the Teruel Basin are of lignite sub-bituminous coal rank. Only the coal facies of the Teruel Basin are well known.2.2.1. Teruel Basin (Lower and Upper Cretaceous age)2.2.1.1. Querol et al. (1989, 1992). During the Albian, the Maestrazgo Basin was divided into four sub-basins separated by intrabasin thresholds of NW SE and W E directions. Only two of these, the Castellote and Calanda sub-basins, contain important coal accumulations. The facies character and distribution of the Escucha Formation in these sub-basins seem to have been formed in a delta-estuarinesedimentary environment. Within this depositional system, two subenvironments producing coal accu- mulation can be distinguished:(i) a flood plain, located in the upper delta plain, with a dominant continental influence and mainly occurring in the Calanda sub-basin.(ii) a swamp belt, located in the lower delta plain, with marine influence and mainly belonging to the Castellote sub-basin.Table 1 Spanish coal facies studies (by Suarez-Ruiz, I. and Jimenez, A.) Paleozoic coal basinsAuthorMethodDepositional environment/other commentsAge/areaASTM Reflectancerank(%)Agueda et al.(1991)stratigraphic andsedimentologysequenceProgradation of delta and fan-deltasystems into shallow to deep water.Carboniferous,Westphalian/Cantabrian Rangehvb-anColmenero andPrado (1993)stratigraphic and sedimentologysequences, petrographyForeland, intrathrust and Intramontanebasins. Evolution from fan deltas to marine environments.Carboniferous,Westphalian/Cantabrian Rangehvb-an Piedad-Sanchez et al. (2003a,b)Petrography (maceralnalysis, petrographicindices) organicgeochemistrySwamp environments, vitrinite-rich facies, wet conditions, high water table, humid climate.。Carboniferous,Westphalian/CentralAsturian Coal Basinhvb-an 0.7 2.5Saldana (1994)stratigraphic andsedimentologysequences,petrographyAlluvial fans, delta systemsand shelf sediments.Carboniferous,Westphalian/(Guardo Cervera basin)Cantabrian RangehvbGabaldon andQuesada (1986)stratigraphic andsedimentologysequencesLimnic basin, alochthonouscoals in lacustrine facies.Autochthonous coals in fluviatileflood plain and palustrine zones of the flood plains.Carboniferous, Westphalian/Penarroya- Belmez Espiel.Alvarez-Vazquez(1999)Paleoflora distributionTwo areas of sedimentationwith coals of different rank(Westphalian B) probably L. Bolsovian,(probably Westphalian C).U. Langsettian(Westphalian A)/BasalDuckmantian(Westphalian B).hvb-anMarques (2002)petrology (maceral andmicrolithotype analysis)Very wet paleomire systemsCarboniferous, Westphalian/Penarroya Belmez Espiel.hvb-an 0.60-3.20Wallis (1983, 1985),Wagner (1985,1989),Marques (1987)lithofacies, ppetrography(microlithotype,maceral analysis)Terrestrial, forest swamp;Seam III: relatively dry conditionswith only a thin layer of watercovering the swamp.Carboniferous,hvbStephanian/PuertollanohvbGabaldon andQuesada (1986)StratigraphyLimnic basin, paleomire systemsin marginal zones of the lakeCarboniferous,Stephanian/PuertollanoJimenez et al. (1992,1998, 1999)sequencespetrography, organicgeochemistryEvolution from limno telmaticenvironment to a wet forest swampCarboniferous,Stephanian/PuertollanoHvb 0.60-0.70Mesozoic coal basinsQuerol et al. (1989,1992)geochemistrypetrography.Progradation of delta and fan-deltasystems into shallow to deep waterL. and U.Cretaceous/TeruelSb 0.35-0.55Garcia-Valles et al.1993,1994)maceral andmineral composition,palynologyForest moor swamp underwet subtropical climate.U. Cretaceous Tertiary/CentralPyreneesSb 0.35-0.45Cenozoic coal basinsCabrera et al.(1995)sedimentology, petrology and organic geochemistry Alluvial and swamp marsh under warm, humid, tropical subtropical paleoclimatic conditions which later evolved into slightly drier and cooler conditions.Eocene Oligocene/As Pontes1.Haggeman et al.(1997)organic petrographyand geochemistryThe origin of the bright layers of the As Pontes lignite is mainly related to the depositional environment with dry periods of terrestrial peat forming conditions.Eocene Oligocene/ As Pontes1. 0.31-0.39Querol et al. (1996)petrography,geochemistryand mineralogyLacustrine with relatively high alkalinity. Influence of thepaleohydrology of the depositional framework on the early diagenetic evolution of the precursor peat deposits.Oligocene/MequinenzaSb 0.24-0.29The Escucha formation has been sedimentologically studied by various authors including Pardo (1974, 1979), Ardevol (1983), Salas (1987), Pardo et al. (1987), and others. All these authors agree that this formation is the result of sedimentation in a tide-influenced delta. A synthesis of the depositional environments in Teruel as interpreted by the afore-mentioned authors has been mainly provided by Querol et al. (1992).2.3. Paleozoic (Carboniferous) coals2.3.1. Puertollano Basin (Pennsylvanian, Stephanian age) The Puertollano Basin (province of Ciudad Real) is an area of small size (12 4 km) of (Wagner, 1985) Stephanian B C age. Coal seams in this basin are interstratified with bituminous shales and oil shales and covered by lacustrine limestones of Mio-cene age. The most significant research on the coal facies concerning this basin (Fig. 1) is shown in Table 1.2.3.1.1. Wallis (1983, 1985). Different terrestrial environments have been discerned: coal swamp, la-custrine, delta and fluvial. These all occur in a small area in the Puertollano Basin, and within a relatively short period of time. Detailed analysis shows each facies to be indivisible from the others, one facies being the natural conclusion of the previous one. Hence, the environmental progression from coal seam to coal seam, producing a cyclical succession, can be explained entirely by internal processes, without the need to refer to external tectonic influences.2.3.1.2. Wagner (1985, 1989). Tuff bands intercalated in the lower part of coal seam III fossilised a swamp forest floor with abundant mature Sporangios-trobus remains that are associated with vegetative Bodeodendron (the same lycophyte), the pecopterid fern Scolecopteris and the sphenophytes Asterophyl- lites and Annularia sphenophylloides. There is evidence of the absence of water currents, although the general environment must have been humid in view of the overall lacustrine setting. This is one of the rare examples in Europe and North America (paleoequa-torial belt) where lycophytes continued to be the dominant peat-forming element in the late Stephanian.2.3.1.3. Gabaldo and Quesada (1986). The different coal seams in the Puertollano limnic basin were generated in the marginal zones of the lake in which the paleomires developed.2.3.1.4. Marques (1987). This author investigated the most important exploitable coal seams in this basin, seam numbers 2 and 3, which can reach a thickness of 2.0 and 3.5 m. Based on the distribution of their organic/mineral associations, the author defined different episodes of oxidation/reduction during the deposition of the organic material in a sedimentary environment of lacustrine type. Thus, during the formation of the deeper coal seam (seam number 3), the oxidising conditions which were favoured by a thin and oscillating water table prevailed. This is in agreement with the high detrovitrinite content reported by Jimenez et al. (1999) for seam number 3 and with the conclusions previously established by Wagner (1989).2.3.1.5. Jimenez et al. (1992, 1998, 1999). The detailed petrographic and organic/inorganic geochemistry research carried out on the coal seams of the Puertollano Basin including seam number 1 and 1bis located at the top of the stratigraphic series made it possible to establish differences in the degree of production/preservation of the organic material and in the paleoenvironmental conditions. Moreover, based on the petrographic indices (TPI/GI; VI/GWI), a depositional environment which evolved from limno-telmatic to a wet forest swamp was established for these coal seams.2.3.2. Cantabrian Range (Pennsylvanian, Westphalian and Stephanian age)There are numerous coal basins and sub-basins of different size in the Cantabrian Mountains which mainly are of Westphalian and Stephanian age (Fig. 1). Relating to the coal facies studies on this area the most significant are included in Table 1. A general information related to the coal geology of this zone is that provided by the following authors.2.3.2.1. Agueda et al. (1991). Coal basins in the Cantabrian Range were formed synorogenically during late Carboniferous times. The coal fields formed a single foreland basin in front of the developing mountain chain. As the orogenic front advanced, the basin became progressively deformed. Therefore, the principal coal-bearing sequences are younger in the direction of the orogenic movement. Deposition occurred through the progradation of delta and fan-delta systems into shallow to deep water. Five broad groups of facies can be distinguished:(i) conglomerates of fan-delta origin interbedded with fluvio-delta sandstones and minor marine mudstones.(ii) delta sandstones prograding onto a shallow muddy shelf.(iii) shallow marine mudstones interfingering with limestones and subordinate delta sequences.(iv) bioclastic and algae limestones that form shallow shelf sequences.(v) basinal shales with local turbiditic episodes and olistolites, which record a shallowing upward trend.2.3.2.2. Colmenero and Prado (1993). Coal-bearing successions are Late (Pennsylvanian) Carboniferous in age and their deposition took place in a synorogenic context during the Hercynian activity, mainly in three different time-successive locations:(i) Foreland basins. Most of the coal seams of commercial importance in the foreland basins are located in the delta facies. Coal seams present in fan-delta settings and back-barrier lagoons are of less importance.(ii) Intrathrust basins. Alluvial fan and fan-delta systems deposited under humid climatic conditions.(iii) Intramontane fault-controlled basins. Continental facies associations reflect deposition as alluvial fans in fluvial and lacustrine environments. Peatswamps expanded mainly on the muddy distal fringes of the fans, in interlobate depressions and along lake margins. As regards the basins of predominantly Westphalian age, the largest coal basin located in the Cantabrian Mountains that contains mineable and commercial coal seams is the Central Asturian Coal Basin. It is situated in the central part of Asturias (North Spain, Fig. 1) and shows a thick sedimentary series (6000 m) from the Visean (Mississippian) to Upper Westphalian D (Pennsylvanian) (IGME, 1985). The Carboniferous succession of this basin begins with a transgressive phase up until the Namurian and then starts a regressive phase with transitional paleosedi-mentary environments in which episodes of marine and continental character alternate. The exploitable coal seams are concentrated in the Westphalian sediments and developed in the continental episodes. Recent data from petrographic and geochemical analyses obtained for coals from this basin confirm a variable coal rank, from high volatile bituminous coals to anthracite (Piedad-Sanchez et al., 2003a,b). A paleoenvironmental interpretation shows that the coals which are vitrinite-rich were originated in a swamp system with a high water table and under a humid climate. This is coincident with the maximum point of humidity for the Moscovian period described for the Euroamerican coal basins.For the Palencia area (Fig. 1) the Guardo Barruelo coal fields are also of great importance. According to IGME (1985), this area is divided into the Guardo and La Pernia Barruelo Basins. The stratigraphic series for the Guardo Basin is of Westphalian D age. Their sedimentary facies are of both marine and continental origin and the coal seams were originated in a deltaic environment. For the La Pe
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